JPRS ID: 8308 SEISMIC REGIONALIZATION OF EASTERN SIBERIA AND ITS GEOLOGICAL AND GEOPHYSICAL FOUNDATIONS

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6 MARCH i979 ~ F0~10 ~ i OF S
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.7PRS L/8308
6 March 19~9
r
SEISMIC REGIONALIZATIOH OF EASTERN SIBERIA
, AND ITS GEOLOGICAL AND GEOPHYSICAL FOUNDATIONS
t~. S. JOINT PUBLICATIONS RE,SE~ARCH SER~/ICE -
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REPORT OOCUMENTA110N ~~L~E?~* z ~ L ~~?~YNnI ~ Ate~~Wn Na
_ PA~E .TPR.S L 8308
1. 1Nw ~M f~rM~H~ II~OS~t ON~
S~I5MIC R~CI.ONALT.ZATIO~I OP ~ABTERN SIBERIA AND ITS 6 Ma rch 19 79
C~OIACICAL AND GEOPHYSICAI, POUNDATI4NS ~
1. ArVwl.1 f. hA~n,~w~ a~~~aNw, ~.a no
V. P. 5olnnenko editor
?M�+~~t O.s�N:.n� M.~ w~w~w~ /0. n'er~/T~~f/Wer~ Un.~ Ne.
Joiat Publications Research Service
1000 North Glebe Road ~4 c�+a.~,ca �a.,~uc?
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SEYSHI(~iESKOYE RAYONIROYANIYE YQSTOC.~IOY SIBIRI I EGO CEOIACO-CEOPIZICHESKIYE ,
OSNOVY, Novosib~rak, 1971
u cu~ i+oo ..wa
This report contaias a description of the results of many years of complex
seiecwgeolagical, seisaic and geophysical studies of Eastern Siberia aimed
at establishing a baais for mapping its aeismic s~egionalization. The genetic
classification of the residual seissogenic deforuationg of the earth'e crust
and the fundamentals of the paleoseismogeological method--deteraination of
the location and iatensity of powerful earthquakes--are presented. A study
is made of the probleas of predicting earthqualces, the seismic regionalization
~nd the peculiarities of the manifestation of earthquakes under permafrost
conditions.
- 11. o.owa~. A~.r,.i. o..aw�+
US?iR Permaf ros t -
Ea~tern Sibezia Tectonic atress
Seismology Forecasting
Earthquakes
? M~M~/OOM~~ON T~nw~
o co~?n nwic~... 8K 8L 17J '
t.. F..iIwM, ft.u~,.~t f.sr.�y w.. rnw A.o..n :3. M.. 4 3~H
Fot ufficial Use Only. Limited i1NCI.ASSIFIED
_ '~uabQr of Copiea Availsble Fraa JPRS, m. _�.?~,u..+~M,..s., +u. r.,~. -
UNCLASSIFIED I
a" s� w.e..~. � s...... o?rwiu~ so~w 2n ~~-~n
(Irn~t~ MTIi-~SI
~ ON~b~wK ~I C~e~c~
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JPRS L/8308 -
6 March 1979
SEISMIC REGIONALIZATIOH OF EASTERN SIBERIA
AHD ITS GEOLOGICAL AND G~OPHYSICAL FOUNDATIONS
Novosibirsk SEYSM.TCHESKOYE RAYONIROVANIYE VOSTOCHNOY SIBIRI I
EGO GEOI.~GO-GEOFIZICEiESKIYE OSNOVY in Russian 1977 sign~d to
press 21 Nov 77 pp 1-304
- [Book edited by V.P. Solonenko, Izdatel'stvo "Nauka", 1,400 copies~
CONTEiVTS PAGE
FOREiJORD. V. P. Solonenko ~ _
CHAI'TER I. Seismogenic Defor~oatione and the Paleoseiscageological
Method, V. P. Solonenlco 3
CHAPTER II. Structural-Tectonic Regionalization of the Pxecenozoic
Basement, V. V. Nikolaqev, R. A. Kurushin, S. D. Khil'ko,
V. S. Khromoveskikh, M. G. Dem'yanovich, V. M. Zhilkin,
S. V. Lastochkin, A. D. Abalakov 60
CHAPTER III. Basic Characteriatics of the Latest Structure,
Yu. A. Zarin 74
- CNAPTER IV. rtechanism of Latest Tectonic Movements, Yu. A. Zarin 83 -
CHAPTER V. Mechanism of Centers and Tectonic Stress Pield,
L. A. Misharina, N. V. Solonenko 92
CNAPTER VI. Energy Classification of Earthquakea, A. V. Solonenko,
V. M. Kochetkov 106
CHAPTER VII. Strong Earthquakes, V. P. Solonenko, V. S. Khromovskikh,
R. A. Kurushin, S. D. Khil'ico, V. M. Zhilkin,
M. G. Dem'yanovich, S. V. Lastochkin, A. D. Ab~lakov 123
' - a - [I - USSR - E FOdO]
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CONTENT5 (Continued) PeBe
CHAPTBR VIII. Malysis of the Epicentral Pield. Seismic Activiey, 221
S. I. Col~netskiy
CHAPTER IX. Seismic Vulnerability of the Baykal Region, 253
- S. I. Golenetskiy
CNAPIBR X. Earthquake PorecasCing 269
Peculiarities of the Development of the Seismic Procesa
by the Obaervations of Weak Earthquakes (in Connection
with the Search for Diagnoatic Attributes of Strong
Earthquakes), N. S. Borovik 269
Long-Range Forecasting of the Seismic Activity
Rccordi.ng to the Geophysical Data, M. R. Novoselov,
Yu. A. Zorin 280
CHAPTER XI. Neotectonics and Seismotectonics, V. P. Solonenko,
S. D. Khil'ko, M. G. Dem'yanovich, R. A. Kurushin,
_ S. V. Lasmochkin, V. V. Nikolayev, V. S. Khromovskikh 290
CHAPTFR XII. Seismic Regionalization 360
~
Des~ription of Seismic Regions, S. D. Khil'kn,
V. P. Solonenk,o, R. A. Kurushin, V. V. Nikolayev,
V. S. Khormovskikh, M. G. Dan'yanovich, S. V.
' Lastochkin 370 -
Peculiarities of the Seismic Manifestations Under _
Permafrost Conditions, V. P. Solonenko 383
CONCLUSIOti 390
BIBLIOCRAPHY 395
~ -b-
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"PUBLICATION DATA q
Bngliah title ; SEISMIC REGIONALIZATION OF EASTEItN SIBERIA
AND ITS GF4LOGICAL AND CEOPHYSICAL
POUNDATIONS
Russian title ; SEYSMICHESKOYE RAYONIROVANIYE VOSTOCHNOY
SIBIRI I EGO GEOLOGO-CEOPIZICHESKIYE
OSNOVY
Author (s) ;
Editor (s) ; V. P. Solonenko
Publishing Houae ; Izdatel'stvo "Nauka"
Place oF Publication . Novosibirsk
Date of Publication . 1977 ~
Signed to press : 21 Nov 77
Copiea � 1,000 ~
_ COPYRICHT . Izdatel'stvo "Nauka", 1977
-c-
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,
Mnotation _
[Text] A description is presented of the reav].ts of many
years of conplex eeiamogeological, seismic and geophysical
studies of Eaatern Siberia aimed at eatablishing a baais _
for mapping ita aeiamic regionali~.ation. The genetic
classificatioa di the residual seiamogenic deformations of
- the earth's crust and the fundamentals of the paleoseismo-
geological method--deternination of the location snd
intensity of po~nerful earthquakea--are presented. A study
is made of the problems of predicting earthquakes, the
seismic regionalization and the peculiarities of thQ
manifestation of eartbquakes under permafrost conditiona.
The book is designed for a broad class of specialists in
the fields of seismogeology, seismology, regional geo-
- physics and engineering geology. It can be used by the
design organizations.
Foreword
' 'i~he latest official map of the seismic regionalization of Eastern Siberia
was compiled in 1962 (V. Solonenko, 1963a, 1968a). Since that time broad -
data have been accumulated which directly a~r indirectly reveal the condi-
tion4 of the laanifestation of earthquakes in Eastern Siberia, primarily in
its most seismically active part the Baykal rift zone.
In order to establish the geological and Reophysical basis for Che seismic
regionalization, a comprehensive analysis was c~ade of the seismological,
Reophysical and geolo~ical data. It derwnstrated that it is far from
always possible from this group of data to obtain a unique or close to F
_ actual estlmate of the possible seismicity level of on~ region or another.
Therefore in the proposed paper cer[sin contradictions are unavoidable, -
the elimination of which will become possible after many years of instru- -
ment observations.
1
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t4oreover, the seismic evenCs in 1962-1Q75 confirm the seismic regionaliza-
tion map of 1962: iC did not reqt~ire Cheoreeical reworking, that is, the
' effectiveness of the procedural principles on which it was based the
joint ana~ysis of Che seismological, geophysical, aeismogeological and
paleoseismogeological daCa was confirmPd.
This paper was written, on th~ one hsnd, ae a secCion of the All-tsnion
theme of Seismic Regionalization of Che Te~ritory of the USS?t, and, on the
other hand, as a developTnent of the theme of 5eismic Regionalization on
Paleoseismogeological Principles,l which was entrusted to the Institute
of the Earth's Crust by the 5Cate CommiCCee of the Council of Ministers of
the USSR on Science and Engineering in 1958. Accordingly, a special section
has been set aside in the monograph on the paleoseismogeological method
which must not be c~nsidered as an inde x of Che basic role of this method
in seismic regionalization. The ob~ective solution of this complex problem
is possible only on the basis of complex seismological, seismogeological
and geuphyaical data not contradicting, but reinforcing erich other. There-
fore, not only seismogeologisCs, but also co-workers from all of the
t~lboratories of the ~eophysica division of the InstiCute of the Earth's
Crust p.~rticipated in this work: the Seismogeology Divisi~n (V. P. Solonenko,
5. D. Khil'ko, V. S. Khromovskikh, R. A. Kurushin, V. V. NiKOlayev,
_ M. G. De~'yanovich, S. V. Lastochkin), Regional Seismicity (S. I. Golonetskiy),
Seismology (V. M. Kochetkov, L. A. Misharina, A. V. Solonenko), Geophysical
Studi~s ~f the Earth's Crust (Yu. A. Zorin, M. R.Novo~selova}, and Engineer-
- ing Seismology (0. V. Pavlov, N. Ye. Zarubin). In addition to the mentioned
reponsible executive agents, the work was also participated in by
A. D. Abalakov, N. S. Borovik, K. I. Bukina, I.. G. Yevstigneyeva,
V. M. Zhilkin, L. R. Leont'yeva, G. Ye. Myl'nikova, i'. A. Novomeyskaya,
A. D. Sarapulov, R. :i. Semenov, N. V. Solonenko, V. I. Tatarnikova,
A. A. Tret'yak, Ye. V. Fomina and A. V. Chipizubov. The earthquake magni-
~udes were redetermined by V. V. Kislovskaya (the ~Institute of Earth
Physics of the USSR Academy of Sciences).
1
Not only the seismic region3lization of Eustrrn 5lberia on paleoseismo-
geological principles was investigated, but ~lso a test of the applicability
oE the paleoseismogE~logical method under the conditions of compression of
the earth's crust. The latter was done in the example o� the Greater
Caucasus where special studies were made in 1970-1972, the results of
which are especially discussed.
2
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CNAPTER I. SEISMOGENIC DEFORMATIONS AND THE PALEOSEISMOGEOLOGICAL METHOD
~ "Experience is the ultimate basie~for knowing�the world."
Roger Bgcon. OPUS MAJUS
In practice, the moat irnportant result of seismological research is
determination of the location a.nd possible recurrence rate of powerful,
especially maximal earthquakes.
~ne prediction of the exact time of an earthquake, its location and intensity
could have inestimable significance. However, the solution of this problem,
if it will ever in general be aolved, is a matter of the indefinite future.
An earthquake is a geological proceas. Based an ti~e physics of earthquakes
and on changes in the earth's crust in connection with them, that is, on
the consequences oi aeismogenic processes and not the cause of them, with-
out taking into acc:ount the noncommensurable nature of the geological and
human time scales, it is possible easily to accept ~ahat one likes as reality.
The causes of strong earthquakes are in general unl:nown to us. It is
possible to make assump tions about them which are more or less substantiated
by the geophysical data. The system on which almost all seismological
r
developments are based, the fracture-earthquake, is decapitated. In reality,
this is only the consequence of deep processes which cause a stressed state
in large volumes of the earth's crust or the tops of the upper mantle in
the earth's crust, and discharge of the basic part (but not all) of the
accumulated excess energy takes place by movement o� the blocks of the
- earth's crust, primarily, the most contrasted, along the fractures but
far from exclusively along them.
Seismostatisticalinstrument data widely used in recent years for various
~ types of forecasts (the recurrence rate of earthquakes, se~smic activity,
maximum earthqua'.;es, seismic vulnerability, and so on), havin~ unquestioned
high significance, frequently do not provide reliable solutions to the
problems. Being objective from the beginning, when processing these data,
in order to agree with macroseismic statistics, they must be sub3ected to
subjective sorting (for example, aftershocks,groups, earthquake swarms,
and so on must be excluded from the processing). Here, especially for the
3
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liighly active regions,it is usually imposaible Co eay where the afCershock~
en~ nnd the normal seismic rePimen is esCnh].isheci.
As to what the normal aeismic Ye~imen is--this is also unknown. Tt would be
pos~ible to use this term Ca refer Co the combination of frequency and
energy class of the earthquakea which would make it possible to obtain the
true recurrence rate oE powerful earth~uakes and their maximum intensity on ~
the recurrence raCe graphs. However, for this purpose it is necessary Co have -
reliable seismostatistica]. data available for the intracontinental seismic
regions for no lesa than 500 to 600 years and even for the moat seismically
active zone, no less thAn 150 to 400 years. -
Moreover, the complex paleoseismogeological and seismological studies in the
Baykal rif t zone demonstrated Chat Che "normal" seismic regimen is ouly an
episode in the activity of the specific 3eismogenic sCructure. It usually
. develops wiCh respect to the following stages: 1) (nonmandatory) fore-
' shocks; 2) powerful earthquakes; 3) active seismic activity (aftershocks);
~i) clecrease in seismic ,activity; 5) prolonged (a minimum of ten and sometimes
hundreds of yeara) calm; 6) degeneration of seismic activity; 7) short-term
(yenrs, perhaps the first decadea) calm; 8) first or second stages again.
Tl~e "normal" seismic regimen is possible only for part of the time interval
oE the siaCh stag~ 3nd the duration of the stages (with the exception of
- the second. short-t~:rm one) is known only approximately or it is unknown.
Ther~fore the determination of the recurrence rate of powerful earthquakes,
ro say nothing of their unper Ievel, by the short-term instrument observa-
tions for specific se~.smogenic morphostructures is a hopeless matter.l If
for the regions with significant seismostatistical data for hundreds of years.
- an~ even for one or two thousand years the seismological methods can give
a more or less correct estimate of the practically important seismicity -
parameters, in order Co estimate the seismic danger of previously uninhabited
' and seismically (instrumentwise) uninvestigated territories, the seismogeo- ~
logical methods are the most important. The history of their development -
is prolonged, but we cannot dwell on it here.
_ The most po~ular at the present time are the histor.ical-structural method
(Gorshkov, I949; Belousov, 1954; Petrushevslciy, 1955, 1957), seismotectonic
(~ubin, 1950, 1953, 1960), tectonophysical (Gzovski~, 1957, 1963;
~iovskiy, et al., 1953, 1960, 1973) and paleosPismogeological methods
(rlorensov, 1960b; Solonenko, V., 1959, 1962b, 1963a, b, 1966, 1970a, b,
1973 a-c). Each of these areas is a comoonent part of a united seismo-
geological or, more correctly, geological and geophysical method of
~ lIn a significant seismogenic zone with respect to area (tens to hundreds
_ of tl~ousands of square ki?ometers) with many more or less like seismogenic
morphostructures, naturally averaging of the seismic regimen takes place,
a:~d by the recurrence rate graphs it is possible to obtain a more or less
correct idea of the recurrence rate of the powerful earthquakes (but not
their upper level) for the zone as a whole.
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precliceing ttie locntion, intensity and recurrence rate uf powerf.ul earth- -
qunkea, and each liAS iCs advantagea and disadvantages.
The historical-strucCural method which ia fruitful when analyzing the ~;lobal
or regional lawa of seismic manifestations during seismic regionalization
frequently encounters inaurmountable difficulties, which one of the founders
of Che method notes: "During the experimenCs clearly defined restricCions
= were discovered with respecC to the posaibilities of the historical-
structural analysis for purposes of seismic regionalization. It was estab~
lished that it is poseible to find relaCions between seismicity and geologi-
cal peculiarities only in a generali~ed form" (Petrushevskiy, 1976, p 69).
The possibilities of Che seismotectonic method are essentially limiCed to
seismostatistics. In order to forecas C the force of the shocks, "extrapola-
tion of the recorded seismicity from one zone to another, neighboring,
like zone" is required (C,ubin, 1971, p 11). For proper estimation of t~e
~ maximum possible earthquake intensity, reliable seismostatistical data are needed
for hundreds of years. The laCest atudies (partially using the paeloseismo-
geological method) indicate that for a specific seismically dangerous area, -
even in the most seismically active zones, a long time is needed to accumu-
1te the energy far earthquakes of the highe3t force for these zones, 110 -
years at tturoto, 140 years at Kanto (Sassa, 1951; Sigimura, 1968), 150 years
in the Anatolian fault zone (Ambraseys, 1970), 400 years in Alaska
_ (Hansen, et al., 1966; Plafker, 1968). The information for these time
intervals (they nnist, of course, be taken as average, provisional data)
can be obtai~zed ~nly for individual ancient cultural centers, and at that
with significarit gaps during the social-political upheavals, pandemics and
other disasters, and they dr~ not encompass the uninhabited or sparsely
inhabited a~e~s, r;~ey are m~ager for the territories where religious -
pre~udices prev~nte~ the accumulation of data (for example, in the lands
of the Buddhist :�fachayanalamaists).
The tectonophysical method initially was of interest in that it offered the
possibility of predicting earthquakea or narrowly local zone~. One of the
most important elements of the method analysis of the quantitative
expression of vertical movements of the earCh's crust originally gave
_ hopeful results (Ca.ovskiy, et al., 1958), but on being used in ad~acent
regions, serious difficulties occurred (Gzovskiy, et al., 1960), and when
trying to use it to explain the regional seismicit~, the author
(Gzovskiy, 1963) came into contradiction with the actual data (~'lorensov,
et a1.,1964).
On accumulation of data by repeated geodetic observations and the results
of a detailed structural analysis of the seismic dislocations, it was E
discovered more and raore clearly that the signs of vertical and horizontal _
movements of the earth's crust in the active areas frequently change
(Solonenko, V., 1973a). In Japan at Cape riuroto, the history of sudden
uplifts during disastrous earthquakes and systematic subsidences between
_ them has been traced for several centuries. In Alaska, between disastrous
5
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earthqu~tkes subsidence of. up Co 11 mm per year takes place, and the
instanCgneous heaving duttn~ r,~e eaxthquake not only has compensated for
this subsidence, Uut in the last 2500 yeara it has resulted in uplift at _
an average rate on the order of 10 mm/year (Piafker, 1968'..
It is no accident that in their ~latest paper, M. V. G~avskiy and -
A. A. Nikonov (1973) give a very careful estimate�of the possibilities of
determining the seismicity levels with respect to the rates and the gradients
of the raCes of movement the most imporCant function of the tecCono-
physical method: "The relaCions of seismicity to tectonic movements -
reflect only the mosC general statistical laws, and Chey cannot be sufficienC
for engineering estimates of seismic danger" (p 54). The ef.fort to improve
- the method as a result of using data on mountain shocks and the: 3solation of
~ four types of movements with respect to seismicity does not change the
situation. The stresses causing mounCain and seismic shocks cannot have a
functional relation their naCure is entirely difFerent. The types of
movements, ~udging by the direction of the effective external active forces
indicaCed on the diagrams in the quoted article (Gzovskiy, Nikonov,
i973, p 5) are a few of the possible ones in nature, and the fourth type
of movement teleseismic which can cause an earthquake tens and -
hundreds of kilometers from the point of seismogpnic movement appears quite
doubtful.l
Detailed seismogeological studies in areas where it is possible to compile
a tiistory of the development of the latest geological processes, for example,
active tectonics in the l~test volcanism (ACTIVE TECTONICS..., 1966) or ~
to discover the migration of modern tectonic ~rocesses (SEISMOTECTOtd~CS..., -
1968) indicate that the geodynamic fields changed significantly already in
the Holocer.e. At the same time, esL-imation of the possible seismic activity
_ without discovering the evolution of the seismotectonic processes with
respect to rates and gradients of movements generalizing the results of -
the mnvzments of the earth's crust at~least~for the t~leogene-Quaternary time
(29 million to 30 mi~lion years) appears to be less and less substantiated.
After the firsr enthusiasm for the method, on discovery uf its obvious
defic.ienci~s, many specia].ists in the field of seismic regionalization -
have Ueen inclined to re,ject it decisively as was previously done. How~ver, _
under defined conditions the m~thod can be used successfully to compare the
expected level of seismic activity and probable recurrence rate of earth- _
quakes in individual areas of the seismogeologically united zone with -
stable seismotectonic conditions, sometimes for a qualitative comparison
of the potential activity of the adjacent areas and for the solution of
other problems. However, it does not follow to expect more from this
1The authors even present specific examples of three such earthquakes .
in the Garr?skaya and the Northern Tyan'~shan' zones, which can only arouse ~
_ suspicion: in such highly seismic zones, using the data over a large -
.1rea, if desired,it is possible to establish the most improbaUle "correla--
t~ons."
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m~thod thgn it csn giv~, It is nn ~ccident that R. A1len, P. 5. Maand,
_ P". Richter end n. !4, ttordquint, underta}~in~y 29 yes~rs of seismogec~lop,ical
and Keisa~ological etudtes in 5outhern C~lifornie, r~rrived ~t ~nelo~vue~
~ cQnclueions to ours vith ree~peck to e~tid~ting the rst~s of v~xtical
~ dtsplncetnent4 !or inolation of the active ~tructurea: "Jt i~ much simpler
= :~nd mor~ r~ali~tic td m.~p the faulta th~n~,~lv~s thr~n to try to cslculr~t~
thc rateH of v~eticgl di~plaeemenc in the ~~alo~ical p4xt or to meagur~
~ euch di~place~aents at the present ticae" (Allen~ et al., 1965).
'Che conclu~ione of thin representativQ grour af Americ~n seismologints
a~d nn_iamoqeologists uith reapect tu ~rtimating the nignificanc~ of th~ -
tracture tQ~coni~s for determining the eeisai+c potential alRO ageee with
r,urA: "7Ch~ mo~t in?porca~nt prablem rem,ain~ the problem of vhether the
r,ones of hiy,h relief de[or~aatiun c~n be predicted only on the b~sia of
the ~vcatione of ~he 'ar.tive'~~ult xon~n,,, Tne anssier r~m.ainn emph4tically
'y~rs'; tn :~ct, e~1 of the ba~tic seiamic ~ctivlty v~~ ~con~entraepd in th~
r~r~na of r~bundant fQrmation of f~ulta in thc Quaternary period,"
:~ll of the enumerqted selamo~eoloqicQl taethudn fail~ed to offer thc
pu~t~ibt~ity of estim,~ting gei~mic danger. of previounly uninvegtigat~d
- r~~,;ionq, decermin~tio� of th~ uppex level of the s~tRmic activity of
~neclfir Ket~mo~enic ~structures, obteining d~t~ on the ~ocstton of the
epiCenct'el zoneR and th~ recur:ence rate of the ~aost po~erful earthquake~
nnd algv evalution of the seismicity of the epecific nrea~. This Pep ia
eesencl~lly fil~ed by the pel~oeeis~opeo~.oqicel method.
Th~~ pal~�osc~ismo~;eoloKicAl method Wag che l.o~ieal r~esult of studying the
~eocc~ct~nics, sei~mogeoloy,y and qeological eon~equences ~f ,strontt (~arce 9
an~! hiKh~~r, M~b.S) earchquakes. The neceR4lty for e~timating the seirsmic
dan~rr of uninhabited or spqrsely populated territories of P.astern Siberia
for s~hich there were no s4l.~stati~~ deta served ae the direct reason for
i[rs developaent.
7he paleo~eisnwqeolQ~icql raethod ueQ in ptactice used for the fir:c time
when correctinq the mockup of the seismic reqionalizaciAn map of Eastern
Siberi~ compilnd in 1956 r~t the Ineti[ute of Eerth PhynicR. Tt~~e AocY.up of
chr m~p did noc differ theoreticelly~ fran the ~eisr~ic reqionalization ~ap
uf 1947-~952 co~spiled under the direccion of G. P. Gozshkov, for, as befqre,
it w:ia ~ua~piled on the basis of thP sei~ca~tatie[ical method.
BaRed on the d9ta aith reepect co the latest tectonicg, seis~nicitv and
the first information on paleqseismodisloca[ions, N. A. Florenaov, ~
A. A. Tr~sY.ov and Y, P. Solonenk~ propo~ed an increaae in the extent of the
zone of hi~h-fotc~ earthquake~ by 90Q ~.u to th~ norti~cest snd by 400 icsb
tn rh~ Mnqt (Plorenso~. et at,, 196~1), anC ~ nev ?a.ap vas compiled in 19h0
(So1~~nenY.o, V,~ et al.. 1960b). 7'tie subse~uen[ ~eisfai~ events ~nd broad
xpeci~~i seiRmnlop,ical, seismogeQloy;ical end geaphyRical s[udiea confirssed
the ob)ectiveness of the p$leoseiea+oyeologicel method.
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'~he conviction ~f the netAmologiste and ~ei~aa geolo~ist~ th~t the reRidual
d~forrnativn of thc earth's crus[ during stronP e~arthquakee ia ~ rare
phennmpnon nnd fault~ c.~n reach the eurface only in the rag~ of shallas~r~
farua c~r~rthqvnY.rn (then onlr in exc~ptianr~l chne~) pr~v~nt~rd rrcognit inn
of tf~c pr~leo~~i~snnq~oldpical ~nethod for a l~~g tia~. No~ev~r, the ~x~mina-
tivn of poweeful earthquekee (r?ith fi;6. S) in varioue higl~ly seismically
active areaR of the world reliably refuted this idea, tt~oreover, whQn
ntudyl.np, the plei~tucei~nal r,onps of alfloRt all very prn+erful and disgstrous
pArthqu~k~s vith cru~tel renter~, palen~eismr~disl~c~tian.g a~re invgriably
diqcaverc~ (see, fot exan?ple, SQ1anQnkn, V., 1962b, 1963n, b, 197b~, b;
ACTiV~ TF,CTOKICS..., 1966; S~I5MOT~CTO:i1C5 196B; Kopp, et al., 1964;
Y,uchay, 1911, 1972; ?tifonov, 1971; Allen, Qt al.~ 1965; Ar~b r~seys, et al.,
1969; ~uchstein, et A1., 19h7; qureehi, S~dig, 1967; Plafker, e[ al., 1971;
Natenv-Yum, et r~l., 1971; ?chaler~ko, et ~1., 1914a, b; and so on).
Tt~e regidual deforaiationrs of the earth's crust rand the ground are v~ried.
'i'hey nre deeply interrelated, but for cor?va.nien~ce of discussing the saaterial
and uain~ them with respect to the degree of relation ca the seissaic procese,
sre ~ubdlvided the resLdual deforaaationn Lnto seismatectonic, gravitation~l- -
seismocectQnic s~nsi eei~mogravitational (Solonen1cA, 1972a, b; Solonenkn, V., -
197'l, b, 19~3~-c).
' The xeisnotectonic deformation~ are c~nnected With [he tectonic saovements
qf the earch's cruRt. Nith respect to theit gene[ic qttributee, encompassed
area, awrphostruccural saorphaaculptucal expressiong, they are divided into
regional~ r,onal and lo~al.
Hefiional 5eigmvgenic Deforiaation~ of the Earth's Crust
uhen examining the pleistoceism Zones of disastrous earthquakes in the -
!'AnKol ian-Saykal seiswir. bel[, s+e arrived at the conclusiAn that the taove-
c?cnt~ of the earth'B crust are not limited to the zones next to the f~ults,
but ch~y encompasA si~nificant areas, at leaet. the sections of appearance
of ~fterRhockR (SolonenY.o, V., et al., 1969), and in the case of crustal
centers, they c~n ~ncompass areas up to tens of thousands and saaetimes -
hundre~fe of thoua~nds of squat~e kilrnaeters. The area ~ of the residual ~
deforc~itivns of the earth'$ crust iQ ap;~ror.imately defined by the folloving
~nrmula as ~ funcciQn of the magnitwde of the earthquake (M)1
1E S ~(0.99 � 0.07) M- 3.6 (1) -
~Tii~ maxic~ volue is for broad ciarine seisaic areas encosapassing the sea
- f~oor r~nd the island ~rchipelagos, and ti+e ~ainirrum value. for n.arrosr
c~onttnennl Refa~ic belts of activate~! nlatforaas.
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- At the present tie~ aur concept nf regianal deformati~n of the earth's
cru~t durinq poaerful earthquakes has receiv~d instrument Canfirmation. `
Nith respect to the mgreographic ~nd gpodetic (repeated l~velin~ and
triangul~,tidn) data, for the Chilean earthqtui~c~s oE 1960 (the prin~ipal
Rhock on 22 N,~y, 1t~$.4) vertical (to 3-5.7 meterg) and hcrrizontal ~o+vements
- o~ the enrth'n crust were establiehed aver an are~ of 130,0~0 km2 (Plnfker,
Snvage, 1970).
During the Alaskan ~erthquake nf 27 ?i~rch 1964 (N+~6.6), the upliftg, sub-
~ gidenceB and buckling of l~rge blocke of the earth's crust cook pl~ce aver
~n area of about 100,b~4 km2 (9t~Q-g64)X(25~-44~J km) from the Aleutian
Trench to the int~rnal parts of the Ala~kan ridge. The vertical displace-
cr~nts on th~ dry lend were from -4 to +10 merQrs= and at the bvttow of the
eea to +15 meters or uwre; the horizontal displac~~ne~te were up to 3 m~tera
(H~nsen, et al., 196b; plafker, 1969).
_ It i~ poesible that the ~aovemente of che earth's crust encomp~as still
~re~ter area~. A reaROn for thie assumption can be the eventg vhich occurred
in 7rnnsbaykal afccr the Nuya earthquake. Th~ Eirst reports that Water
h~d apppnred in the Torey a dry lacustrel basins after the tluyskiy [NuyaJ
earth~uake s~zre received in the fall of 1957 (before the Cobi-Altay earth-
quakc). Lle did not attach any significance tn this report, for the lakes
~re 750 to 800 km froc~ the epicenter. Houever, che lakes quickly gprkTad,
and in 10 yeara the area reached ~17.5 km2 (the depth of lake yun-Tor~ya `
- r~ached .9 metera, Barun-Toreya~ to 3.7 meters). The area of a n~~e.r
uf 1~kes increased not only in the southern part ~f ?ransbayY.al, but als~?
in :~orthern Mongolia where a lake 16 km l~ng appe~red, nnd the drea of the
Khukh-:iur Lake increased hy several titaes; the L'ldzya River chan~ed its
dirQCtion and flowed from Hongolia to the USSR to the TorevB basin8. ~
- The aajority of researchers of the yexre-loug complex expe+dition studying
tiiis excraordinary event arrived at the conclusion [hat it is connected with
_ the posrerful earthquakes of 1957-1958 ahich occurred t.n Hongolie end the
_ Bayk,~l rift zone aitb 1~6, :.4, a.6, 6.9, 7 and 6.5. "fhe move:aenc$ (of
!.he edreh's crust) are of a differentiated nature, for the scale of the
subsidences ir~ the variaus lacuetrine basins i~ different"(ftarinov, 1973,
p 79).
The enorm~us epicen[ral distances, of course, provide a basi+~ for doubting
she relat:on of such gign:ficant movem~nte of the earth'g crust, but
exact coi~~~idencc of thea~ in time vith the poverful e.3rthquakes in !~tongolia
arui the a~ykal rift zone and the ebsence of any relation eo the other
causeA at least force che question to bQ stated of the possibility of
movementa of Lhe earth's crust ower areas on the order of a million square
kilrmeter,;. Is t}..s not the cause of the solidarity of the aoi+erful earth-
q~~.~kes in the Mongolian-Baykal seismic belt CSolonenko, V., 1974)?
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Mon~olian Pe4ple'~ Renublic B~ykal Fift Zone
Kyakht~ 6~'ebr~~ry 1957, tt=6 y Muyg~ 27/June 1957, M=7.9
C,obi-Altay 4 becember 1957, M=$.6 + Nyukzha 5 1Antt~ry 1958, H+~6.5
~~yr~n-T~ngr~n~ko;~~ ~ April 1958, M=7 Ole~.m~ 14 5eptember 1956, Mi6.5
Mogodekdye S Janu~ry 19b7= M~7-3/4 Tae-Yuryakhskoye 18 January 1957 M~7.
Urtil recently ch~e re~ional ~eismugenic movementg of the earth'g crugt vere
nnt uged tn di~cover the disaetrous asp~ct~ di the past, glthough effnrts
t+ere aadC td expl~in the formatit~n of t~rrdces by them (Plafker, 1968;
5igimura, 196$). tlo~+ever, ahen expandin~ the greas encrnnpas~ed by the _
~eiRraogeological gtudie~ there i~ such a possibili~:�, especially in th~
marine ~eismic rc~ions.
Ina~much ~s Che a~ov~rnentg of the earth's cruet frequently hav~ diEfer~nt
em~litude and sign next to each other, thev can introduce significant
disr.urbances into the normal evolutionary eeriee, of the relief. The simul-
taneous variation in relief of different types (transgressive and regLesgive)
cnn indieate its seismogenic nature. ihe problem still lies in exact dating -
of th~~e chan~pg.
Ttie r.onr~l seismoqenic defore~etions are o~uvements oE seisaagenic morpho-
- Ktructures. A classical example of them is the disp~acanent of the mountain E,_
~?roup nf Curban-Bogdo of Gobi Altay during the earthquake of 4 December 1957
(force 12~ M~8.6, center depth 18+8, most orobable 22-25 1~a). For the Eirst
tirae in the hietory of seismogeology the possibility vas offe~red to a[udy
the mnveaient during the course of the earthqueke of r~ large aarphostructure
in a"clos~d gystem" ac the sarie cirae as the ~eistaogenic structures oE
other strong earthquaY.ee eicher are highly complex or they do not have
clear boundaries. and a~ost frequently they are covered with sea and ocean
Water. -
During the Cobi-Altay earthquake the mountain massif (275X30 kra, absolute
1ltitude to 4,p00 meters), similarly to an ic~breaker during laceral
coahression of the ice~ rose and shifted to the east ([he apparent ampli-
tudes of the di~placQments to 10 and 8.8 meters; true, as a result of
bendin~ defornations, appreciably losier). Ptany explicit and latenc
eler,ents nf the mechanisw of deformation of the c~orphostructure and seisca-
genic cw rphosculptures of the Cobi Altay appeared (Solonenko, V., 1959,
1960.z, 1963a; 5olonenkn, V., et al., 1968; Solonenko, 1965, 1966).
A~ysten ot faulcs nnd other residual deEormations of the earch's crust
vas forned vith :~n overall length of about 85~ km. All of the kno~m and
sorae of che previoufily unknwin types of dislocations in the structural
peoloRy occurrcd: gr~vitational-seismotectonic s+edge vich vertical dis-
~lacer~enc acapl:tude to 328 meters, stripping of the mountain peaks, and so
on.
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_ UurinE; the Muy s ~~rthqueke on 27 lune 1957 (force 10-11, ~i=~.9, th~
depth nf center 22 km) twn aeismc~g~nic morphnstructureg were shift~d: the
Namarnkit embryonic depreeaion oE the Baykal type ~nd the E�~ult-block upiift
of the Udo~;an and Bouthern ttuya ridges. Durinp the parthquake, th~~
ba~ in dropped 5 to 6 meters and aas shi~ted to the southwe~t; the
Udokan ridge ~hifted in the nppogite direction 1 to 1.2 met~rs, and it
uplifted 1 to 1.5 m~ters, and it aas eimulteneously overthrust on the
depree~ion with r~gpect to the gtrike-slip thrust fault. The vi~ible move-
_ m~nt along the f~ults nGCUrred over an exCent c~f 140 km (90 km~ to the e~st
and 50 km to the west of the instrumentally dptermined ppicenter), ~nd the
extent of the rt~yg system of the fault itself connected vith the earth-
qu~ke of 27 June 1g57, 35 km. Oscillations of the aalls of th~ old Eaults
occurred over the reciaining extent (Solonenko, V., 1965).
The principel residual defornint~ong for thi~ type of aeismog~nic morpho-
gtru~cur~s are concpntrated Within the limitg of the moet actf.ve part of
_ the morphostructural system in the embryonic depressinn~ and in the lee~s
nctively developed fault-block unlifts they are concentrated in the Lone of
f:~~~lts d~limiting them on the depression side (Solonenko, V., 1965; -
ACI'IVE T~CTO:rtcs 1966).
'fhe presented examples of the aonal dislocations i~dicate that when discover-
ing their paleoseismogenic analogs it is necessary first of all for the
geologisC to dismiss the cenonical postulates of the handbooks on structural
analysis. Por example, a reliable sign of different age of the structures
ig considered to be geodynamic difference in type. In reality, during
disaxtreus earthquakes any type of structure occurs simult~neougly. The
incomps~tible defora~ations are mutually trensitional; for example, an over-
chruRc can quickly turn into a poverful tensile fracture or fault (Solonenko,
V., 1960a,1963b).
In the case of paleoseismogeological reconstructions of posrerful zonal -
seismotectonic phenomena, one of the knotty problems is stratification of
the zonal deformations ahich will permit determination of the recurrence
rate of strong earthquakes, the "viability" of the seismogenic structure,
and so on. Por this purpo~e, geological, hiseorical-archaelogical, ~
dendrochronological and radiocarbon methods can be used.
The loc~l seisnatectonic deformations are direct signs of che residual -
tectonic deformations of the earth's crust intt~e epicentral zones of poaer-
ful earthquakes. Hi[h reapect to scale, cy~e s~nd structure of residual
defora~ationa vhich are visible on the earth's surface, the fora~ation of
- vhich is not explainable by any other causes except seismic, the locacion
.~nd intensity of the earthquake, preseismostatistical for the Riven region,
is detecmin~d.
Thc first standard acale for deterr.~ining the intensity of an earthquake
Wns established empirically (Solonenko, V., 1962a) ahen studying the powrer-
ful ~nd disastr~us earthqunkes in the 'tongolian Baykal seismic belt.
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Then~ with the eccumulation of daCa on modern seismodislocatione, it became -
poseible to give a general formula for the approximate c~lculaeion of the
m~gnitude of the earthquake with respect to the ~xt~nt (I) of the seiamo-
disloc~tion zone:
_ lg L~ :(1.01 � 0.02) M- 6.1$.1
- 'The scale of the seismndislocgtinns d~pends not only on the m~gnitude and
the intensity of the earthquakeg, but also on their depth and mechaniam oE
the center, the geological etructure of the epicentral zone and other cgusea,
as a reault of which it can be different for earthquakes with identical
pnergy characterigCic.
The extent of the aonea of seismogenic faults formed during modern earth-
quakes fluctuates from hundreds of ineters (for '~i>,A.S). The maximum eatab-
lished amplitude of vertical dieplacement is from tens of centimetera to
10 to 12 metere, eometimes more, and horizontal displacement, to 8.85 meters.
Nhen studying the paleoseismodislocationa, it has been necessary more than
once to deal with significantly greater amplitudes of the displacements by
zomparison With the ones obaerved in the epicentral zones of modern earth-
quakes Which can be explained differently, but tWO cases are most probable.
1. Paleoseismodislocation tias occurred not in the case of one but in the
case of several earthquakea that have taken place close together in time,
and it expresses the total effect of the displacements.
2. After the main shock, the movement of the Walls of the fault continues
during the aftershock activity and, possibly, even after that,
If the aeismodislocation is repreaented by a seisaw tectonic scarp~ When
determining the amplitude of the displacement it i~ necessary to be
especially careful, for on steep alopea the covering deposits or part of _
the old fault breaks away, and the clastic material can be absorbed by
the fracture at the foot of the scarp. The illusion is created of a very
large vertical displacement. _
1The correction factor of +O.C~2 is of geological significance. It is equal ~
to 0 for faults, strike-slip faults, strike-slip thrustfaults (With a
subordinate shift component), maximal for ehifts, minimal for upthros+ faults
and A~is~i~ zones with snecial. types of stresses (for near vertical position
of the major axis of the stress ellipsoid). If the shift component for the
valls of the fault is simultaneously directed in opposite directions, then
this preventa the development of faults, and their magnitude turns out to be
less than usual (aithin the limits of un to tvice as ~uch With equal magni- .
tude of the differently directed shifts).
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In ehe cese of bldck typp seismogenic etructures the area of the atgri~~ea
per.t t~~na houndr.rl hy thr. fnul t~ rencheg 250 to 30~ km2.
_ P~rt of the eeismologista and geologi.at~ atill adhere to the old idea ttiat
the eeismoQenic fracture deformaCions ~ncomp~sa only the cover beda,
nlthnugh thig also contradicrg numero~es known fa~ts. There i~ gctually
little daCa oti the behavior of aeismodislocatione at depth, but thp exiat-
_ ing obgervgCions more indicate an increase in diaplacemenC amplitudee with
depth and not damping of the dieplacements. Thus, in the case of the Idzu
earthquake on 25(26) November 1930 (M!7) g shift with an ar~plitude nf 0.7
meters tooic place nn the eurface, gnd at a depth of 160 meters (in a tunnel
on the Tokyo-Kobde railroad) it became a sCrike-slip fau1C with horizontal
displacement of 2.4 meters and vertical displacemenC of 0.6 meters. _
In ~.he case of the Cobi-Altay earChquake where it was possible to study the
ehift surfacea in the cnver rock and bed rock, ~he amplitude of ChQ residual
deformations apparent in the aurface horizons turned out to be half or -
less than half the true displacement ampliCude at depth.
The Eact of prolonged exietence on Che steep slopes of the rock of the
seismotectonic Crenches is an index of deep occurrence of the joints
Only in the case of constant absorption of the clastic material by the ~
~oints is it poseible �or them to remain in the relief (see below).
We have already given attention (Solonenko, V., 1913a) to the hypertrophy
of seismodislocations at the bottomB and on the undervater slopes of large
bodies of water. For example, during the Kanto earth~~iake on 1 September 1923,
the relarive displacemente of the bottom of the Aay c�f Sagimi reached
-400 and +250 meters, and Within the limits of up to 1170 meters (to -720
and '.�450)1 although in the case of like earthquakes (H=8.3) on the dry land,
the scale of the displacement does not exceed the first tens of inetera and
only rare structures of special type gravitational-seismotectonic wedges
(see beloW) approach the aubaqual deformations with respect to their amrli-
tude.
In the case of the force 10 Central Baykal earthquake on 29(30) August 1959,
the bottom oE Baykal dropped 10 to 15 meters (Solonenko, V., Treskov, 1960)~
and on the dry land in the ~aykal region the same earthquakes (M=6 3/4)
c.tiuse~i displacements along the faults of a total of 0.8 to 1.2 meters.
The eEforts to classify theae phenomena as the result of consolidation of
sediments are connected With lack of knoWledge of the physical-wechanical
lAfter thc earthquake, four special ahips aorked in the bRy. They took
more than 86,000 measurements.
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properti~g of the bottdm gnil which ~C e depth of ~ever~l meters, ns ~ r.ule,
hnr+ nrtill~;tblr rxr.rHp ~~ornatty, tn pny nothlna nf thr fnrt Chnt Chr riar
af chr Hen ur uc~cr~n I'inar in genrrnl do~e not lenve room far such explnnntione
(w~ nr~ not tnikin~ nbout bottom detormaCiong cnnnecCed wieh underwaeer
slidpo Ch~y baeicnlly ~re ~11 r~cogniz~d nn th~ songr recordings).
Thie phenomenon remains a mysCery.
Cravitationgl-Seiemotectonic beforma~tions ~
T,~e movement of the walls of the faulCs during earChqual!E'.8 frequenCly
cr~~tes favorgble conditions for moveme�t of Che roc~ r~asses under Che
effect of ~ravity.
The ~rovitgCinnal-seismotectonic atruCCUres are direcCly conn~ct~d wiCh Che -
~ctive seismogeniC faults, but enmetimes also with lnrp,e fracCures exp~riencing -
pagsive opening during the oscillatory movements of the earth's crust during
etron~ earthquakes. The length of the known eravitational-seismotectonic -
~tructures re~chee 7 km, for exAmple, the structure of Shartlay (Sol_onenko,
V.~ 19h2h; SFIS:tOTCCTONICS..., 1968, pp 25~28), an area up ta 10 to 20
~qu,7rc+ kilomhtct':t.
~ At this tiu?e landslips orcreep fault~ gravitational-seiamotectonic wed~es and
in n~~ c~se, supposedly, rupturing of a ridge slope are known. '
L.andelip faults are formed on the steep slopes of mountains WiCh high -
energy of relief, eapecially where the faults cut off the spurs of the -
_ mount.~ins. The development of these faults is pror~oted by a combination
of two systems of fractures: steep rear faults and more gentl.;? sloping
weakened zones inclined in the direction of the foot of the slo�e. Un~er
such conditions, even With small shoves of the blocl:s along the faults,
the rear fracture at the crust expands sharply, and as a result of the
_ stpepness of th~ slope, the imnreasion of significant vertical displacement
is created. Por example, in the landslip fault of the_Snezhnaya aeismoRenic
structure, the apparent amplitude of the vertical diaplacement is 25 to
90 meters, the width o~ the fault trenches is 35 to 9~ metexs, a~thou~h the -
~ crue mean-maximal. amplitudes with respect to the fault are 7 metets. In
_ some landslip faults there are 5 to 6 series of separation ~oints,�and
tiie landslip fault has a atep strur.ture (Khrcmovskikh, 1965, pp 15-64;
So;onenko. V., 19Fi4a, pp 17~-180� SEZSMOTQC'fON~CS..., 1Q68, p 47-50). -
The apparent amplitud~e of a landsl.ip fatilt 3oint downslope decreases, Ehe
landslip fault acarp wed~es out toWard the thalWeg and has the anpearance
oE Whiskers facing front on.licn+ever, sometimes the fault intersects the
- thalweg and the next cape, at the same time exhibiting its tectonic and
no[ Rravitational nature (Fig 1). Sometimes a true fault, emerging on the
slope of a canyon, becomes a landslip fault.
14
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- ~ , .
S~:" G
L
" . Y.r~,. :i`.
a
~ .
S5 _
1':
, j ,S
v `ii,"t^ '
~ ,'.~rrt,,.
~
:S
- �RF.. . l , s . ~
� .:k.H .`Y_-`.~
~ 'T ~ ~ ~ ~ ~ ~~~4 K ~ ~ ~ ~ -
?
_ i , ~ ~ ~ ~ ' L.. f ~~i I ~
. v ~ * 1~ ~ c, ~
5a'fIS . , .
, `4, ~ 1~, . . .r, ��`I
, ~ ~ ' a.
~
Y
~ . ~7
~~.ft r
. : ~ . . ~ ~ y, y~r ,
~ t., ~ ~ i'~'' ~ -
~ ~i'.t-� A r~
i~ ~ . .:.~i'. . , . '
Figure 1. Seismogravitational or Cravitational-Seismic
Tectonic Structure of Akiba (the Greater Caucasus),
photograph by V. M. Zhilkin
nuring force 11 and 12 earthquakes, sometimes gravitational-seismotectonic
Htruc[ures oE a special type are formed, the possibility for practical
inatantaneous formation of which has not been suspected prev~ously by .
anyone. These include the Rravitational-seismotectonic wedges and ruptures
of the mountain slopes.
'~he ~ravitational-seismotectonfc wedge combining the elements of tectonic
s~ibsidence nnd collapse was established for the first time in the central
part oE the nleistoceism region of the Gobi-Altay earthquake. Its location
was predetermi.ned by a cluster of ancient, new and latest faults, iricluding
three enormous EXactures connected s+ith recent earthquakes. In addition,
it is 1or.~ted at tl~e intersection of tWO large local faults and is
associ~ted with the north corner of the seismogenic central graben of
Ik1ie-Bogdo (1OX15 km) formed on 4 December 1957.
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nuring ti~e enrthqu~kc ng~inst n bnckground of g~nernl uplifr, th~ corn~r
of thc ,1ninCs op~ned ~p'ancl pnrt of ehe mnuntain (3254 meCers high)
mnde up of grc~niCi.zed ghales 1.1X3 km in area collapaed into tt~e earCh.
The nmplitude of the verCica]. diapl~cement ot Che tectonic wedse Ernm
euRt to west increa~ed from 156 Co 328 meCers (Che pr~ciginn of the
� determinntion was Erom +0.2 Co +2 meeerg). As a reault of the wedging of '
force nn the free side of the Bitut c~nyon, along rhe fronC of the wedge
extrusion of wedges of Che rocky ground Cdok place upward to 60 meCers -
ttnd the forn:aCion of an overthrusC-seismocupola frontal sygtem Cnok place
(Solonenko, V., 1963b; Solonenko, 1965)~
'fhis phenomenon was so extraordinnry thnt some of the geolo~isCs are seill
trying Co question Che possibility of the �orm~tion of such seismotecConic
displ~cement of a ~mall bloclc of the earth's crust and r~+~a~idet' that an ~
extranrdin~ry cgve-in tool~ pl.ace here. A detailed aerovisual, ground nnd -
photdgrammeCric study (by the aerial phoCo~rnph3 of the section made before
and after the earthquake) leaves no room for such doubt. The disappearance
of approximaCely t~alf of the volume of Che displaced block into the earth.
tlie Eormntion of milonite~s along Che fronCal displacer, and be�ore them,
. the nscending aeismocupola structures and overthrusts, the make-up of the
body of r.he sCructure from monolithic rather than crumpled ro~k, reliably
indicate the seismotectonic nature of the BiCut strucCure. lt is sufficient
tor a nonprejudiced ~eologiaC to look at a photograph of Che 13itut structure
(Fig 2) made during ita prolonged formaCion (3 January 1958) during the
aftershocks to understand that it is not possible to talk about an ordinary
_ cave-in here.
The rectilinear faults on the frontal part of the strucCure are well visibl.e
in the photograph. Later (in September 1958) during field.documentaCion
we established that these faults dip steeply into the depths of the slope
and are covered with tectonic clay milonites formed during the earth-
qualce (Solonenko, V.~ 1963b; Solonenko, 1965). It is clear that the forma-
tion and preservation of such faults in the cave-in is unconditionally
included. The mechanism of the seismogenic collapses indicates this:
during powerful earthquakes seismoexcitation of the crumbling mass takes
place, and it goes at enormous speed to distances that are unobtainable
in gravitational collapses (Solonenko, V., 1970a, 1972a,'b; Plafker, et
al.. 1971; Solor~enko, 1972a, b), which did not happen in Bitut although _
the conditions were more than favorable for this.
For subsidence of the tectonic wedge at Bitut, total opening of the frac-
tures bounding it to 12 ra was necessary, and the apparent (residual)
wi~lth of the fractures in the epicentral zone reached 19 meters.
i.ater this type oE structure was established in the Baykal seismic belt
(Solonenko, V, 1962h~ ~+CTIVE TECTONICS..., 1966; SEISMOTECTONICS..., 1968).
The largest oE thc.~, ~~~e Shartlay str~~cture on the west shore of Baykal
is more than twice [he size of the Bitut structure (length 7 km, Width
more than 2 km, vertical displacement amplitude to 880 meters).
, 16
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Tne ~mphithenter of the atructur~ turned toward the lake cut into the
I3ayk~1 ridge beyond the Leno~Baykal divide line~
RecenCly the gravitational~ae3emotectonic wedgea have bpgun Co be found
not only in the ttongolinn-Baykal seiamic belt but also in other t:tghly
eeismic zones. For examp]e, V. S~ Fedorenko (1968) considers dgmmir.~ ~f
Lake Sarychlek on the ChaCkal'skiy ridge of WeBtern Tyan'-ahan by a
seismogravitational sCructure of ehe Bitut Cype probable, It ia poesible
that thia type of eeructure o ce urr ed �on the Yeniaey 6 km above the
dam of the Sayanp-Shuahenakaya hydroelectric pow~rplanC. It encompassed -
both shorea and the channel of the river ~ohere ite local increase in depth
by 90 metera ha8 been establiahed.
Cenetically the mountain graben~troughing (aubsidence) of the mountain tops
established in the Stanovoy Iii~hland :(Solonenko, V., 1962b; ACTIVE
T~:CTONICS..., 1966), in Che Baykal region [Pribaykal~ya] (Khromovakikh,
1965), and in Che Caucasus (Khromovskikh, et a1., 1972; Solnnenko, V.,
Khromovskikh, 19~4 structurea of Labakaldi Tseri) are close to the
Rravitational-aeismotectonic wedges,
A ch.~racterietic nnd obviously rare type of gravitational-seismotect~nic
, atructure is the pu~nctures of the mountain slopes. Such a phenomenon has
still been establiahed only at one point north slope of the Southern
ltuy a ridge. Here Che rid~e in the form of an arc ii~ advanced into the
Muy a rift basin. A slip-strike thrust fault runs along the olope of
" the ridge, formin~ the chord of this arc at the same time as the frontal
fault (strike-slip?) bounda it along the border of the ridge and the basin.
The primary cause of the formation of the structure is assumed to be a
strike-slip thrust fault occurring during an earthquake with an intensity
. on the order of force 11 (M'>7-3/4). Here th~ seismic acceleration exceeded
~ .~:e gravitational acceleration which caused powerful stresses in the
rock massif advanced iuto the basin, and a sharp shift fractured it along
the surface ~ncJ.ined in the direction of the basin at an angle of 5�.
The maximum hor!iontal shift reached 170 meters. A rupCure 6 km long,
triangular in cross section, with an average width at the base of 800 meters
and heiglit along the rear fracture of about 200 meters occurred on the
slope. The volume of the rupture was on the order of 450 million m3.
The structure, although documented (ACTIVE TECTO~JICS..., 1966), under the -
conditions of its formation leaves auch unexplained, and it awaits
additional. more detailed studies.
4Jith respect to the ~nechanism of formation, the structure obviously is
similar to the shearing of the tops of the mountains the transitional
~ form from the gravitational-seismotectonic to seismogravitational deforma-
tions. ,
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G : ,h.' 1~ { ~f'v~r~r~~~""~~1, ~ k~`;�~, ~
~ ~{1~~_`~* ! * ~~,,~~~~~iFIF~~ ~~1. 4P~�. ~i 4Yi~ - ~~Fe~ ~4 .
~~r ~t' '..Y~{~tI~ 7~~ ~ i; f~~ ,~~ye~i`~ 1~1~. ~ `~c.. ..1 -
r ~~mn } 1~ M ~
~~~,h~~~fJ`}~S~a} "a Pt~~ {jkt~:r ~
51 ~
a,y~,t. (1�:~rt~~ +t.
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: 1 ~ ~ ~ ~ ?
: r
r~R,+?~ 1' t ~ ~ x
, { r . ~ ~ J
~ ' f 1 }~f ~~~ti ~ ~_e
~ ~ . . ~..t' V , . i.,
' + . . t.i'� p~t: ~i, :
! t .'.l~ l~~~ .
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Q. . S ~
�~\,L~ajrr'r~'.Yy ~ ~ ~g~+~::`~y ~
4 , l44 ~ ~ i i~ ~ ~ �~INt y�.i, . ~ ~ ,
{ : ~
i ~ ~ ~~'SYfi~~'r/+~, , I ~ ~ -1
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h~~ tt=! . e!
' ' :'v.. r
i ` t~.
~~~'~~~4 1 ~I~
`"t
y.,
,eti � ~'w~." P
z'1 ~~1' i a~ r . j~ ' ~~C ~ t:
,1
~x } ~3~~a ' r-t, ,
i .~~~4~~5 i;Y.z.- i ~ ~ ~iE,;~'~ r~Tj
a ~~~~y rr aV~.{ ,
w`` ~ ~ 6 ' 4 � 1~ a",~;''~ . s. ~ ~~~r
r b'r'
~~~i i: ~ ~I t a~ ~ ~ ~ F .
~~Yl.~! 1 y'~v ~..j t F .~,19
~ r� ,.aa~r~
+r ~t~ ~ -
.
.
d.
t}ua
y.
f ~~~~~'i":r,~ .
Figure 2. Bitut Structure. Photo by N. A. Florensov.
a-- rear fault, amplitude to 328+2 meters, dip to the south
at an angle of 70�; b--- faults on the frontal section of the
struc[ure dip to the north at an angle of 70�.
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In the ~nse of disaeCrous earthquakes, egpecially in mountainous areus,
often the greaCer part of rhe human victima and material losses are
connected noC with the earthquakes themaelves, buC wiCh accompanying
sei~mogravitaCional phenomena.
' The earChqur~ke on 16 December 1960 in China (force 12, M=B.6) killed
200,000 peop~.e; of them, na lesa than 180,000 clied in landslips, avalanches
and ea~th flaws.
During the e~rthquake of 10 Ju1y 1949 in the mountains of Tyan'-Shan'
(force 10, M~~7.5) the rayon center of Khait was destroyed in a lattdslip,
and the seiamogenic avalanches and flows were ~arried up to 20 l:m along _
Che valleys, destrdying dozens of populated places and fertile J.ands.
_ Tn MAy 1960 (ri to 8.4-8.6) the Chilean earrhquake caused thousanda of .
slides atid landalips~in part accompanied by the formation of new lakes,
the destruction of old onea, mud flows aausing greaC material losses and
lossofinany lives (Tazieff, 1960; Davison, Karzubovic, 1963; Weischet, 1963;
and so on).
- During the Alaskan earthquake of 27 tiarch 1964 (Pt=$.6) the greaCest material ~
losses were caused by slides, and loss of lives, by tsunami (Hansen, et al.,
1966).
The Peruvian earthquake of 31 i4ay 1970 (t4=7.7) came sadly to be known as
the Guaskaran landglip. The city of Jungey and part of the city of P~anrahirka
with 18,000 people 40% of the victims aad destruction of the earthquake
were buried under the landslip mass (THE PERU..., 1970). ?'he greater -
part of the remaining dead we*e victims of landslips, slides and mudflows
(Plafl:er, et al. , 1971) .
The epicenters of the Chilean, Alaskan and Peruvian earthquakes were in the
_ Pacific Ocean, and on the dry land their intensity decreased significantly.
Therefore the victims and loases connected with the seismic effect itself
amount to a Cotal of 1Q to 20X of the total losses, and with seismogravita- ~
tional phenomena, SO to 90~6.
Iiowever, not only are such unique seiemic disasters dangerous for man and
nnture. The "routine" powerful earthquakes encompassing areas many times
smaller are repeated hundreda of times more frequently, and their total
destructive effect is comparable. Thus, for example, during the earthquake
, in New Guinea in 1933 (M=6.1), landslips encompassed 240 km2. The vep,etation
and soil layer were completely strippedover an area of 60 lan2. According
to t}ie calculations (Pain, Bowlar, 1973), 60 to 70~ of the total denudation
.layer w.~s removed by earthquakes.
The presented examples (a few of the known examples) indicate how vitally
imPortant seismogeological engineering forecasting is. ~ven if the time
oE the earthquake were known, the settlements would still be destroyed,
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and Che ma~oriky of tihe people would die, buC not 3n their homes, but in
ureas where rhey cooul.d look for sa�ety. Therefore engineering seismogeology
' which is only in its infancy must 3oin the ranks or the most importanC
branches o� knowledge called nn to come to the defense of Che soci~ety and
its achievements againse earthquakes.
The sei~mogravi~ational phenomena themselves are varied and muCuall.y r,ver- -
l~pping: settling and subsidence ofmbuntainsides,landslipe,sl~des,avalanches
and'dirt flows, mudflows, and so on. They are known appreciably more widely
Chan Che first two types of seismogenic phenomena, for, first of all, they
are encountered apprec3abty more frequentiy, they have been observed many
times during earthquakes, and, secondly, for understanding of them the
- specialists do not need to croas tt?e barrier of tradiCional concepts of
the slowness of tectonic proceases.
_ In order Co discover the seismogenic nature of the graviCaCional phenomena,
the identification of their age, discovery of the relation to seismogenic
and seismocausative structures and the analysis of Che dynamics of movement
of the mountain masses have primary significance~
The simul.taneousness of various shi~~ts o~ the soil masses over a large area
is a reliable sign of their seismograviCaCional nature. They are usually
distinguishable from the gravitational phenomena connected with disastrous
:ains. The seismogravitational movements of mountain masses during
disastrous earthquakes take place over a~ enormous area (of thousands of km2):
rtuya, 1957, 150,000 km2; Chile, 1960, more than 130; Alaska, 1964,300;
Peru, 1970, 65, and so on. Simultaneously, hundreds and thousands o� land-
slip:~ slides,earth and mud flo~os are formed and so on. No other natural
pr~enomenon can cause such enormous movements of soil with respect to size,
amount and affected area. _
In mountainous regions of mod.ern orogeny, a significant part of the seismo-
gravitational morphosculptures have to the present time been taken as exogenic
(landslip.glacial, proluvial and others). This is connected primarily with _
the f.act ttiat the seismoexcited �landslipsand avalanches and dirt flows follot~T
an unusually long procedure, and the seismogravitational facies of the
_ sediments ~re similar to~glacial or p roluvial.
The se-ismogravitational, destructive and accumlative and the corresponding
- exogenic morphosculptures in indivi.dual cases are often difficult to
distinguish or indistingu3shable. However, they have their own qualitative, ;
nuantitative and temporal peculiarities. ;
The tectonic stresses of the rocks, seismic accelerations and vibrations
during earthquakes exciting the soil masses basically change the conditions
of their stability and movement. Accordingly, the seismogravitational
morphosculptures can develop under geomo~phological conditions such that
the formation of the analogous exogenic morphosculptures is impossible.
The formation of them itself in the exogenic version requires a different,
usually prolonged time up to many thousands of years and in the
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NUk p1~YiC1AI. Ug~ ONLY
eci~nwprnvitr~tion4l verni4n, in nractice~ it tak~s piace inRtAntAnrously.
Thc fir.nt in the reqion are of diff.ecen[ age (etretifie~d ~aornhonrUlptural
gen~ratinne), gnd the ~ecoruu~ ~ee Rimulc~neaus (di~~ontinuous oe iav~er~d
morphaRCU~ptur~i generetione).
_ The chnny~e in nr.ql,i1 icy ~f the mountain r.?~n~Q~ durinq egrthqu~k~en ran ari~e
- from differettt cau~es. The mo~t importAnt Qf th~m nre ch~ follrwingc
1) Aeismic ~ccel~r~tion~ en~ e~ decrea~e in ~tre~qth of the ru~k; 2) a ct~ange
in nlope ur.qle of the un~table planen; 1) thixotropic liquefACtion of the
aoil.
Seismic ecceler~tionR Are the cause of slides,lga~ielipr gnd other qrgvit~-
tionnl phenc~wenn Qn the $lop~,~, No one denies this, but th~r~ i~ nd
qatisfc~ctory mathematic~l m~odel of the relscion betveen [h~ ~rthqueke and
_ che gravit~tionetl ehift, s~d the ppssibility of so~ving thie probl~o iq
gtil~ not fareseen. The calcUlations of the prabs~bl~ n:~ture oE th~ str~R~es
occurriny, durinq the enrthquakpe on che Klopes nre being nerfbrmed in A
re~ion tonnidered co be linear (QCCardt.n~ to [he calculx~~d notee, the
' s,ei~rav~rams, accelo~ran~s, velocigrame), but the instrumentR record the
~~scillatory end not the true noove~enta of. the Qarth's cruat. When
cxemininR dieestroua earthquekes (~t>1-~/4, I~>fvrce l0) wherever it in
posnible reliably co detera~ine (by the ~slip surfaces, sneciAl types of
a~iRmoy,enic folded etructures~ snd so Qn), iC ig diacov~?r~d that thQ true
novement ig reciprocnl (in the verticel end horirnn~tal direction~) with
r~t:~cinn. The rotation~l deforrAinq movaaents ere clearly raanifesced elsa
in th~ fqrce B xone of force 9 estthquekes (So~onen~.o, V,, Tre~knv, 1960).
in ~ddition, Ear che cnlcul.ationa it is ngce~sary to coneider the depth of
occurrence of the parting surf~ce, the aeight of the ective and passiv~
parts of the landalide-slip,the stress-rupture ntrength and the s~rength
nt the cira~ of the tret~or, the snRle end dirpction of rapproech of the
seismic aeves, the d~arstion of the tre~or, the degree of floodinq, th~
dey,ree of ~tree~ relief or, on the contraty, the degre+e of preparation
for shif[ing of the mount~in niaeses by the preceding ear!hquake~ and a
nu~bcr oi other indexes, the wa,jority of ahich are irapossible to establish
in practice. especi~liy for a rep,ional ev~luation of laadslide-sli~ dQnger.
A Renernl !_dc~e of the effe~ct of seis~aic accelerstions c~n be obtained
!f u~ rvnRider the sei$mic effect on the ~lope as an increase in its slope
_ ~ngle
1 ~t w .~.s�
5 ~i-~/~ 12-23 0.5-t,S
6 25-5~ f .5-3
7 M/~-bi/~ 34-100 3--6 .
8 'S'/r-8~/~ f00-2r10 6-f2
9 b~l,-~ 20U-~Op t2-25
10 ~40-500 23-38
where I iR the fqrce acc~ording to the MSK-b4 scele: 't is the ruignicude
for deptha of centere of 15+5 km; m i~ the eeiemic ecceleretion (csa/nec)
for the perioda of 0.1 to 0,5 sec (Medvedev. et el., ~965).
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The pre~entE~ Ci~ure~ indir.~te thc~t under the ~nrre~pondinv, c~,nditions _
force 4 nnd 5 earthquakc~ ~gn alrQady be th~ csuge of nltde~ and 1and~lipg~
such r.n~es are kn~n. However, hy long-term dbserv~tions Qf slidee in ~
the Crtraes~ tt ha~ been Qgtr~bl ished that ~uring the period of excees~
cnoiature, the f.orc_e 4 enrthqunkeq even c~uRe Rlide activation et the same
ttme na uith ~ nh~rte~ge of c~oi~ture they have n~t ~hifted fc a fnrce 8
e:~rthquake (Clukhov, 1959).
tt iR mu~h rnore r~liable to dQt~rmine ~he danqerau~lnndelip z~n~~ by the ~
~sei~mc.at~Ci~tical ~nd paleoaeismogeoloYic~l (Solanenko, Y., 1962b, 1973a-C)
dr~[a tlian by th~ rs~thematicel awdelg. The cc~mbin~ti~n o~ the+~~ tWO raQthads
' bffer~ the po~eibility of nocing the boundariet~ t~f qrQas en~ompas~ed by
thc aei~r~ogravitAti4nal phQnoAena during egrthqual:e~ e~f defined inten~ity,
determinntion of cheir typeg, dyn.~~icg, snd go an ~h~rncteri~tic for the
~ivrn aeinmic r~giun with ite gpecific peculi:~ritipn of enqine~erinR seinaw-
~;~c~1~,~;y and ni.~nife~tatian~ ot ~e~rthqu~kes.
'Che seisrnoPravitatianal phenoaena have ma~a develdpment in the isoseismal
~rena of for~c 7-6 e~nd hi~her. The tt~ta~ area in Which it ig possible to
expect th~ developtacnt of seiRCroqrgvitativnal phenomens~ coincider~
~pprc?x~ra:~tciy with thc c4[dl nrer~ of poesible defarmationx aE th~ ~earth'n -
cruat ~nd tn tn a rnam depree gubordiriate tv the ~bove-pres~nted relgtion -
frtce p A).
V~rintion of che Slope Angle of Unstable Planes
y -
~ror., chc~ thcory of slidea snd landslips it is Y,notim th~t on metest~bl~
~l~s;,ea cliang~s of. the slope angles by tena of seconds ere Aufficient to
digtu~b the equilibrium of che elope and fvr potenti~l or stabilized elidea
and lnnd~lips so be put in motion.
~n~ of the most rel.ieble caees oE such slides was described by H.adley
(1964). ~urin~ the }icb~en ea:thquake (ti~7-3/4), depth o� center 10-12 km,
fnrcr l~; ~ee 2durphy, Brezee, 1964) a long ecabilized slide vas cut by
- a fnult aich nn ac.c~licude of 0,9 raeters. M a result, thc slope of the
slide aurfnce incre~sed by 23 minutes.� This diBturbed che eatAbLished
eq~~i 1 fbriun s~nd 5 days af[er the earthquel:~ the alide t~as set in aa[ion.
r.}1:lf1~{C in Rlope angle iR possiblr for all types oE seigraocectonic
d~_?fora?.~ttona reRional, zonal and local.
_ Ic is naturr~l th~t the altered slop~s afe not sufficienc aith respec[ to
che rncire deformed area for the appearance o~ slides end landslips, buc
durin~ reKional forecaRts this posaibility mvst be considered. Obviou8ly~
n~rt c~f tt,e glides havc taken p1ACe during the time ~f or eoon afcer the
Chf i�.~7n e~rthq~k~l;e (T:~zieff, 1960; Weischet, 1963) ~rtd having no OL~i~[
~pn~rent c~vAeB. aere connec[ed aith the change in slope of the veakened
j1IAi1rR in the rwuntein cu~ears.
22
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~
pOtt O~PtCtA1. U~~ ONL1'
7'he zonal ~eiemotectonir di~l~z~tion~ are ~cr.ompanied by a~ignifirant
numt~er o~ differenc l~ca~ ~~i~mate~tdnie deformationg (fauit~, upthrorr fault~, ~
qrabena, rtrike-glir ~aulte, c~nd ~o on), "Cogptheri th~y ra~ely ch~nge thE
gn~le~ ot nlope af tt~e weeN~ned r,anes in a~n ~re~ to )~1 t~ 2h,~Od nqu~r~ kilo-
meter~. Ila+ever, the b~nic volume of unetabie mount~in rna~~p~ her~ ar~
fractur~d during thQ ~arthqtt~ke attd ita aftprgho~ft~ a~ a result of eeismic
g~celerAtions. tf ~he ~eir~n~ie gtruetur~ find~ expiirit g~olo~ic~1 rpflec-
ti~?n i~ the favlt zone, th~n the r~~e ~iqniflcant chengpg in ~lopeg ee~ur
alnng thi~ tone. tn the ea~e df powerfui egrthqu~kes, gy~tcro~ of eei~mo-
_ di~lticati5n~ accur in th~m, the ~pproxim~te pxtent of uhich ~~n be
deterr~ined in the a~qnitude nf expe~ted earthqu~k~s (gee p 11).
Thixotrapic Liquefgction of 5oi1
nurtn~; an earthquake thie ph~nomenon causeg s~b~idence oE the ~eaeth's
~urf~ce, nud vol~Anoe~, and alid~g. N~ecous de~truccive ~lides of this
type vcrurred durin~; the r,hilQ~n ~nd Al~sk~n ~arthqu~kes. in Ala~ka the
dam~Ke in~.he cities of 8ewgrd, Veldez, Nhittier, Anchorage, were reckoned in
the hundr~d~ of miltion~ of dollar,~. The Ternahein ~lide encompa~~ed the
grelter p~rt of the rity df Anchorag~ (Han~en, et el., 19G~). tihen explar-
ing ttie nlopp at thp port lgt~r it axe egtablishpd that for the ~tatic
position :he sLope here is cotap1et21y eteble.
Tf~e thixo:ropi~ liquef$ction of th~ ~oil not onlp reducpd the bearing
cap~ricy ~~loaet t~ zero, but algo caused a pu~+erful dyn:~mic effect on the
c4ver. fr+rqu~ntly ~trdng bede ahich brokp out and ghifted. 5imil~r phenornena
vcr~ ob~~~wed on brosd areas during the earthquakes in t:ongolia (Khan~ay~kiye
_ un 9 r~nd ;!3 July 19A5, M=3.4 and 8.7; Gobi-Altey, 4 Dec~*mber 1957, ?t~1.6;
Nny~dskoy~t 5 Jenuery 19G7, ~t=7-3/4),
It wag pr~~pose!d earlier [hat predc~minantly silcy $and (true quicksand ~nd
pAeudoquicksand) are predoaiinancly capable of mass thlxotcopic liqueEactian,
but efter the earthquakes in Chile, Alaska and ttiigata (16 June 1964, M~7-1/2)
it aag discovered th~t often even sand end gravel, inoreine and other similer
~oil~ liquefy.
~then forecestinP sefiauwqrnic slides oE chixotropic rareEaction it is
necenaary to pay ettencion pri~sarily to the coascal regions t+her� earch-
qu~kea uith an inteneity of ~ore than force y~re poe~ible.
Th~e~ fol loving taain typea of eei~ua~enic slides and landsllps can be noted.
I. SeisraoQentc stripping of eoountein peaks aas escabli~hed for the first
tiee in che pleiecoceir~ zr,nr of the Gobi-A1tAV earthquAl:e. The stripping
occurred n8 follosrs. During the earthqu.:~kes che Amplitude of the displace-
~,rnc of the mouncein eaaasifg vae more than [uice che amplitude of che
- irrev~reibl~ deforaa[ions (Solonenlco. V� 19h3a~ pp 326-329). during the
�n.~in ~i~oct: thc ~aouncnirts shifced Ear to che eait and qbove the position
~f equilibrium, ~nd thrn they returned to the vest end dosm so energetically
23
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that th~y ag~in passed the point df equilibriun, but in the opposite
direction. The peaks of the mounc~ins ha~1 qreat~r amplitude of digpla~etnent
th~n theie baHe, n rp~ult of ahich *.her~ a~~ a lag af momentum nf the
pe~1~c~ of the m~uttt~in~ behind their f~et: r~h~n the b~~e began thp return
movEment~ the peaks ~ere ~till tnovin~ to che ~8gt, in cor~nerti~n uith uhich
po~?ps~ful ~hearing fdree~ oecurred in the~ (Sc~lenenko, V., 1968, 1963~;
~vlonenko, 19~55, pp ~45-~4fi), The l~a ~ngle ~E ~h~e~r slape of l.tl tn 15�
en the ea~~) indica~~~ that ~ue nf. the twd ~rtive fdrepg, ne~r hnrizontal
geismoinertial ~nd vertic~i gr~vit~tinnal, the fnrmer gi~nifi~cantly exr~ed~d
the l~tter.
?he crn~~ sections ~E the cleava~e pl~ne~ vet'e from lOn ta ~c~bX1500 n~eters,
their ~~currence uae At a depth frrnn ten~ t~ ~5~1 meterg. 'Che p~akg either
ahifted to thQ ea~t vith r~eeti~n COUf1tErC10CRM~ge or th~y aere thrrnn+n
into thP ~anyon.
'Che ~hearin~ r~f the mountain peak~ w~~ egtablished in ~outh~rn Pribaykal'ye
(fsaykal region~. tn the 5nezhn~ya seigmic structure, the sharp pointed
grnnite reaks wAre dEC~niteted to 100 to 15~ meterg (basc area b.3!t1.7 km),
and the heakg aere thro~m into the canyon af the 5nezhnny P.iver (Khromovskikh,
19~i5, ap 59 ~nd 99).
2. T~ctdnic-Seiemogenic Landsli~tes and Lattd~lip~
in the mc~dern orogeniC b~lt~, the overwhelmin~ m~,~ority df enoraious landalip~
and Iandslides are cied to the znn~s of neismo~ctive frgctures ~nd are
directly or indireccly connecced vith ~arthquak~e (Snlonenl:n, V., 1950, 1972g,
b; Chucinov, 196L; Zc~lotar~v, ~t al., 1968; Fedorenko, 1968; Solonenko, 19~2a,
b).
The geiss~otectonic movec~ents of the earth's cruat creace instability of the
rock s~~sses, and their disastrous move~ents are caused, as a rule, by earth-
quaY,eR. ::ot anly are landslips and landslideg fonaed, but n~v ones are
prepnred siraultaneously.
Tt~a teccanic-setsr~ogentc landslips develop predominantly as landglide-`laad-
~lips Haturally, avalanching takes place aftpr the most serious sei~mic
~~scill:~tion~, and the avalanching a~asB has extraordinary dynamics. including
t1~e ranqe of it$ ~pread.
in tiie areas ~de un of ~;foderately dislocated seditaentary or volcanogenic-
Redl~ent~r~ fortaations. in the presence of severe ~arthquakes, bands of
bedn up co several equare ki~omet~rs in ar+~a slide (se~ Pig 1). Enor~oous
cr~ck~. bench~s up co teng of ineters high in che forra nf scigaacectonic
~cnr;~a are forsaed, and a n~taork of tpctonic ,~ointe aPpears, and so on
(5ol~nenko, V.. 1971a-b; Solonenko, V., Khrocwvskikh. ~974).
l. Seinax~genic L.~ndslips vith SeiRmically �xcited Avalanche Nass
- For the fnraacion of euch landslips obviously tan conditions are necessary:
inRtanc~n~eoue collepae and cruahing of the rocY, and the effect of pos+erful
24
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~a~ dpptctai. us~ orn.Y
aeiamir, d~cfl]atlhng c~n th~ plunging fine to medium lumpy mn~~, excitinq
it ~imil~rly er~ n vibratinn ecreen ~t th~ or~ enrichment enterprige~.
'Che geiemieglly exCited aval~n~he mag~a mov~g at ~ndrmoue velc~ciey, it
tr~v~l~ n p~th many time~ 1dng~r ehan nrdinary, and it ~an ~rogg brd~d
vnlleyg and ri~e high on th~ oppa~ite slopee. Th~re ~re f~~cg indiC~tin~
che po~gibility oc ~ueh ~n ~valgneh~ a~ee eroesing ~ canyon (Shcon~nkd,
Khrda~vekikh, 1974).
5o f~r g~ i~ knnsm, only ~np ~uch lgndglipg h~g bppn do~um~n~~d
(5~lc~n~nkd, V., 197~) in conn~~tion uith th~ Kh~ie p~rthqu~k~ on
10 July 1949 (farce 1n, M~7.S). 'Php landglip in the D~rikh~uz Cgnybn
(Pig 3) mov~d ~t n ep~~d of ebo~t 100 km/hr, it crneg~d the Ygrkhyeh
River (~biic~bud) end rns~ td ~ 15-~etpr t~rrac~. Th~ ~rp~ e~E the
iandslip rmrs vas 10.7 ka2, and the 1ong~~t p~th vag 1~J.5 km. In the
ca~e of ~n ordinary grevitationel ~valanchp it did not ~xceed 1.5 to 2 1�.m.
A poa~rful ~ir aeve p~g~ed befor~ the le~ncleliu~ It ~wept aaay etructur~~,
bral~~ off tr~~a or tore thrm out by ch~ root,~ ~nd toseed th~n hundr~ds
_ oE m~ters through thp air. A cascade prufile is cher~eterietic of guch
r~v.~tan~hee: ehe weakly inclined gection~ ~nd in ateep scgrps (there are
~ix 1s~rg~ aeves Wich che ~cerp hei~ht up to 50 to 60 m~t~r~ ih the
Uarikhaux C~nydn). 3oi1 gpurte from the s~iemic~lly excited mass, forming
charn~teristic ~arth pyr~mids vhen it fa11s, ~nd it eque~z~g th~ l~rge
ro~k nwnolitha into the ghapp uf obelisks. With eome pl~nation which ig
unavoidable ~.t time~~ th~ morphosculpture of the avalanche field could
~~~ily bp teken es glacigl.
Tr~ces of the seismically excited ~valanchpe hav~ bQen established in
varioug highly seiea~ic regione. On che Zaali~sl;iy ridge the eeisnog~nic
avalanchee h~ve traveled a path up to 30 km, they have departed 10 to 15
k~a Erom thp fooc of the aauntaine, thpy have croASed an int~raantan~
begin ~nd ro11~d up the elope df a ridge. The avalance mass which Was
previously taken ae ~lacial denositg cov~red an area of up to 150 km2
(Kurdyukov, 1964). Obviously, che Saidrnarreh landalip (Iran) one of the
larqest in the aorld wich a volurae on the order of 30 km3 (length of
seperation aa11 14.8 km) is of the same type. The avelanche mas~ traveled
up co 17.5 km, croseing a ridge up co 600 ~eters high on its way and
covered an arQa of 16S km2 (Herrisen, Palcon, 1937).
4. Seise~ovit~ration Landelides and Laadelipa
Obr~iously, in individuaY rare cases the ecale of eeiswic dislocations
depends noc only on che incensity of the earthquake, the depch of the
renter, the cype c+f aeismogenic structurp and geology of che area, but
also the duration of the semisaic vibrgtione. Thus, on che 81eck Sea
co~~ac of the Caucaeua (Tuatse-Map) A. 8. 4etrovskiy (19~Oa,b) egtablished
masx developa~nc of characceriatic landelides, shifts of the ~ountain
elea~ents, poaerful fcaccurea. and so on, the fot~ation of Which is
connected aith the diaastrout~ eacthquakea of the pasc. Nhen gtudying
this arcn in 1971 on the Abrau Peniosula (bet~+een Novorossiysk and
Anepa) ve encouacered tha basic tyne of geodynamic phenoraena: enormous
- 25
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POtt O1~I~ICIAL U5g l~Nt,Y
~ (i) e
.
~~f "
.
.
~ � .
_ c~~..~~~:; ~ ~~2~ .c9~
.
: .
~ , . ~1~~
. ! . � . . ! ~w r
. ~ , . ,
. �
. .
/r ~ ~ .
. ~
~ ~
~ � ~ �
d. ? ~ �
.I � . � .
: . : ~
~ � , ~ ~ ..j:;. t ;
, ` ~ i~:
~ ~ .
� ~ ~ ~ y ~ a:? ~ ~l , ~
Pt ~ ~ � ~
~ g ~ . ' t ~ t!1
7 ~s ~6 ~t.`, ~ .
1 D Qb, (~n ~'on~
,.,~;;;drw:~ri~+~~~.0~ ~ K ~a
~ (6~ 0,~ ,��aQN~~C~
Figure 3. Pl~n Vi~+ of the Khait Landslip on 10 July 1949
dravn by P. Solonpnko.
1-- s~+e11s of ancient avalanch~s; 2-- Y.hgit Landslip;
3-- scarps of the avalanche maes vavps; 4-- rock-avalanche
ac?phitheaters; S-- landslip amphitheaters in loess;
6-- aeiamogenic rocky landalide-landslip and direction
of its movement� 7-- landslides and protruding knolls;
8--direction of motion of the landslips (I-IV cheir
auccessive phases); 9-- seismogenic upthro~? fault;
t0 seismogravitational landalip-landslide iointg;
11 mudslide ri~l; 12 divides; 13 caraine;
14 proluvium; 15 ailuvium (Q3); 16 Proterozoic
(Pt(?)) and Siluri~a (S) ~aetamorphic series and granites;
17 outlines of populated placea buried under the avalanche;
Key:
1. north S. Yaqman
2. south 6. Flond plain of the 3urkhov River
3. Khisarak 7. Yarkhych (Obi Kabut)
4. Khait 8. Dokhaitskiy debris cone
9. Darikhauz
10. Leke
26
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~dtt nppiCtAL U5~ nNtY
with re~hert to width (up td 100 to 150 meter~) ~nd depth (to 9d meterg),
but ~hort Cnd more th~n 4 1~) gplitg dr ghifts of �drts of the mountaing
(~i~; 4) rnvering ch~ v~ll~y~ With rogtge~lumr rock fldwg running up to 3.5 km
frdm th~ir gour~e (dnang them, up to 7 km into the ~ea), ~t the ~~me,time
a~ Ear e grdvitaeion~l ghift the gv~l~n~h~ m~eg could tr~vpl nd mdre
than Sb tn 100 meter~ f~om the foot of the avalanche glopp Cm~ximum
het~ht le~~ eh~n 400 met~er~).
y~verth~l~g~, pven during ehp mdgt poW~rEul earthqu~k~~ knnwn on enrth,
guch f~rm~tinns hav~ not acCUrred; in ~ddition, they hnve not been CntltleCted
aith explieit gpigmag~nir f~ultg gnd th~y se~ rtot ~eri~mpanied by ~~eigmo-
~ravit~tinn~l dhgtrurtion of ine~untain~ of the ~orr~sponding srale. We
have come tn th~ ~nnrlu~ion th~t here ae ~r~ d~~ling with ~ tt~w phenamenon
hrevioug]y unknown in geology with ~ type df seigmog~nic-vibr~eion~~l
rre~p ~nd disintegr~tion of the mountain maggifs rauged by prolong~d
seismic vibrntiong of mod~rate int~n~ity frorn ghallow eenter zan~g in th~
~he1f zc~ne af the B1~ck S~n. Thig phenom~non whiCh we have called the
"Ponti~n phenompnon" (Shcc~nenko, Khromovskikh, 1974) r~n al~o occur in the
rtediterr~ne~n 5ea a~iere extraordinarily long-lagting ear[hquake~ h~ve been
recorded more than on~e in history (th~ last of them wes on 9-13 Augugt
195~ aith tt up to 7 on the Ioni~n Islands).
~
_ !ti ~
4
~ . ~y -
.
~ # ; , ~
~ . . ~~ti~ S �
. ,y. rx r� ~v:,~�
.���T�: ~ -.,~p",
~rr
t �:y'`~ ,_,t_ . � .
. ~�'r.. �
` �
` ~ ~ ~ . �
. .
l~~4 .
.
~ ~ -
~ -
A
, Z~
~~~r~t ~
ti.ti. ti ~ 1
�
F'ip,ure 4. Vibr~tian-$ei$motecconic Joint oE the
Utrish Structure on che Abrau Peninsula.
Photogroph by V. P. Solonenko
21
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- 5. Spi~mogr~vit~einnal Lgnddlipg nn ~n Air Cughinn
A uniqu~ nv~lnnchh orcurrpd during the t'eruvian p~rthqu~k~ nf 31 Mgy 1970
(?t+~'~.7); 50 million e~ 1h0 milliun m3 of ~oi1 end ice broke lnnse from
Cu~gknrm ttnuntnin ~t nn eltitude of SSIIA t~ 6400 meters. The nvnlanGhe
fel] 1 km vprtiC~lly, and eh~n ie ran 3 lan along a~2� ~lnpp ~nd 10 1cr~
~idng a S� ~1ope. Thp eval~nchr~ dev~lep~d ~~p~e~ ~f na le~~ eh~n ~~0 tn
385 1%m/hr, xrtd ttccordin~ eo b~lligti~ celGUlationg (the multitnn lumpg -
were thrown to th~ ~ide up ta 1600 mee~r~), th~ ~p~ed r~~~hpd tnor~ th~n
450 km/hr Whi~h mad~ it ~a~~ibl.~ for th~ av~lanche n~gg to be hurled
hrrdgg a ridge 230 meter~ high, ~erdgg the Rio S~nt~ V~11~y ~nd ergvpl
83 mee~r~ up thp oppu~ite ~id~. *tud trav~led 160 km aldng thp Rid 5~nt~
River td the gen, destroyinp, n bridge nnd n hydroelectriC po~rerrlnnt.
tn pl~ceg where th~ evalanche pneged~ the vegetation and soil 1gy~r turn~d
out to be undieturbed. Th~ invegcigatore di th~ avalanch~ ~xplained this
fact (~ugt ae the enormous speed of the avalanche) ~y the fact that the
~v~~lgneh~ m~gg mhved on ~n ~ir ~uehinn (Pl~fker, et al., 1g71).
6. r LippinR Lttnd~lide5
In ~re~s m~d~ up oc mndernCely dislocated sedimentgry or volcanog~nic-
sedimentary forr~atione during earthquakes in gCatically atablp spctions
bands oE beda up to several square kilometers in area slipped. Thus,
- during the bagestan earthquake on 14 May 1970 (td=6.6, Ip=force 9), numerous
slipping landslides aere formed. The Achiygkiy landslide (~10 million
cubic metera) 1 km lon~ croseed the Chvakhun-Bnk Valley and bloct;ed it.
The qraben-like trench up to 180-20~ metera aide and 40 met~rs deep formed
on the slope. Higher up on the slope another seiguwRenic line of Soints Wae
Eormed ~rhich prepared a neW landslide (Klimenko, Tearev, 1971). At
- another location, the sliding of one of the peaks of the cuesta crented
the illusion of ehearin~ of the mountain peak.
In the case of sharply exF,resaed bedding, schistoaity or tectonic jointing
planes, the slipping landb~lides can also occur in crystalline rock.
7. 5eismogenic Earth Avalanchea and Streams
On the slopes of mountains covered with talus, placers, and, especially.
loess goil, a mags of landslidea, mud streams and landslips develap
The latter are especially dangerous. 1'hey move similarly to sno~a
avalanches. The individual earth avalanches can cross valleys and travel
hundreds of ineters up the oPposite slope. If there is a sufficienCly
oowerful stream in the valley they can turn into mud streams. In the case
of mass descent of avalanches (especially with countermovement), on
collision ttie earth masses acquire powerful dynamic momentum, and they
rush do~ard at enormous velocities, forming a high-speed earth stream.
28
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~o~ o~~icr~, us~ orn.Y
~ -x~r~~.. . . .;4 � d ~
~
i
kr
. ' ~
. !F ~
_ ~ f,~,. ?j~ s
_ . "~~~~i ~ . ~ ~
i~'i~;ure 5. Chnrnct~ri~tic Microrelipf of nn ~arth Stre~m.
Photograph by V. P. 5dlonpnko.
In ttie case of the l~ait earthquake, the enrth avalanches and streams
traveled into many of the valleye. Along the broad, gently sloping vnlley
c~f the Ynsman River, the earth str~am, in gpite of small bottom slopea
(2 to 3�) traveled 20 km, destroying 20 ki~hlaks [Centr~l Asian viilages)
nnd fertile lands. This caused the first investigators of the earthquake
to concl~de that a mud streara had nassed through the valley. However, the
- seudy that we made later of the morphology of th~ slide rock, its internal
strurtur~ to a dePth of 15 to 20 meters and microrelief demonstrated that
~ scismically excited earth atream had passed through the valley alEhough
in places (in areas where the aater from the submerged stream broke
[t~rauRli) the earth mass could have assumed a mud consistency. The first
insrectors did not note Che mass development of the hummocks caused by the
earth spouts, a diatinguishing feature of geismically excited earth strearas
(Snlonenko, V., 1970b). This microrelief (Pig 5) is usually taken as
sedimentary hummocky-sinkhole relief or periglacial earth cone relief.
Sec~ndr~ry spouting channels terminating ac the surface in residual sinks
oE spurious craters can be seen ~.n the cross section oE the cones in the
seismically excited earth streams (~ig G). This is a reliable characteris-
tic of the spouting cones of the seismogenic earth avalanches distinguish-
~ ing them from earth mounds of other genesi.s.
29
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~Ott Ut~i~ICIAL US~ dNLY
~i f:-
~ ~~?M h
I ~
; ~
y.' , ~
. ' ~ ~ , .'~:,~?:;t!;~~.
~ ~i~fi~!~1`'t -
~igur~ 6. ~~rth 5pout r.iound in Ch~ KheiC Avalanch~ in ehe
Yn man River Valley
1-- p~1p ~Q11oa etructurelege logm; 2-- th~ a~m~ wirh r~stnr~d
1o~~e ~CrucCure; 3-- dnrk broan Iogm with flow t~xture.
The muund w~g formed on 10 July 1949 end it Wa~ digcovered
nn 21 October 1968.
In geigmic erp~g with thick lopea d~poaiCe on e,~geneially any geceion with
~ glnp~ of more than 10 to 12� Che occurr~nre of earth avalanches and
gtr~dms ia possible. Ther~fore che most dangeroug greas must be distin-
~;uiql~ed. :l~ese ehould include the nrobable pleistoceism earthquake xones
aith Eorce 8 intenaity and higher. The vall~ys parallelto seiemically
~ctive faults are the moat dangerou~. The f.ormation of powerful earth
streams ia most prevalent in them.
Under p~rmnfroat conditions the formation of earth atreams during p~werful
~arthquakes dependa to a high degree on the etate of the active layeri
in the winter when the active layer has merged with th~ permafrost, th~y
cannot occur in general (the Tas-Yuryakhskoye earthquake on lt3 January 1967,
force 9-10, ?t~1); at another time the melting part of th~e active layer
slips, and depending on the degree of wetting, earth avalanches or mud
floas are formed (the Oymyakonskoye earthquake on 18 May 1971, force 9-10,
M=7; see Kuruahin, et al., 1972).
In che seismic zones with broad fields of thick friable deposits, especially
loea;,, the earth avalanches and atreams can be widely used to discover the
pleistoceia m regions of preeeismostatistical stron~ earChquakes.
t~ihen there is aufficient flooding, the earth streams Lecone the mud �lows
whicli in general frequently accompany poWerful earthquakes (Solonenko, V.,
1963c).
Role of the Paleoseismogeol.ogical ttethod in Forecasting Landslides and
Landslips -
In the paleoaeismogeological method broad use is made of the trsces of
ancient seiamogravitational deformations.
30
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The p~l~nepiemoR~ologic~?1 d~ta nn Ch~ p1~i~CoC~iem zone~ nf the mo~C
gcverr eerehquakc~n of. thi~ r.enCury gccompnni~d by di~aetrou.~ ~eiemo~rgvita-
ttonnl rhenom~nn indiCat~ th~t thp lergest landglidee and lendslina hev~
a~table tendency to reppat in G~rtnin areae (Solonent:o~ V.~ 1972a, b;
Snlon~nko, 1972g, b).
AGCOrding to our ob~~rvations, Chie ie ronnect~d with tao princio~l ceuses;
1) high etree~ of th~ rock maeses in the body of th~ s~isnsogenic etruceur~
and 2) with the preparaCion of new rock ma~se~ for avalanching during
preCeding earthquak~s.
The strega of the rock in high].y active aeismogenic etructures is ~o gre~t
~ that the landelipe frequently occur wirho~t any app~rent reason even on
~lop~~ Chgt ar~ gtable with respect to ouCward ~igas. Thus, in the
C~ntral Graben of the Dovachanakaya Seigmog~nic Structur~ (sep Fig 7)
by aerovixiual observ~tione we were able to photograph th~ gvglanching of
_ n slope 2.~ km long (Fig 8). During field examination of the etructure in
_ 1962 two aval~nches occurred before our eyes on a single day.
The cheracCerisCic aign of the landelip~ in the overstresAed maseifs ig
splittin~ of thc~ rock, Erequently independently of the existing weakened
plnnes. The blocks (in our caee up to 1.5-3X5 meters) have the shape of
decritus obteined when ta[cing eamples of rock for cruehing, and the fresh
cleavag~ planea are powdered with granite dust (ACTIV~ TECTONICS...,
1966, P 30).
These l~ndslipa cannot date etrong . earthryuakes, but they are a reliable
index of the hi~h seismic potential of the eeismogenic etructure.
In the area~ With powerful seiamogenic landslips and landslides, conditions
are simultaneously prepared for the following shifta: Eravitational-
seismotectonic and seismogravitational ~oints encomoass neW large areas
- (Sotonenko, V., 1978, b, 1972a, b), often reaching the divide on the oppo-
site slope. To the side of the seiamically active faults on steep
mountain alopes amaller landalipa and landslide~ are prepared s~hich ia
reflected in the seiamogenic (Beismogravitational) settling of the slopes.
When predicting landslides $nd landslipR it is necesaary to realistically
consider that the estimation of the seismogenic-gravitational stability
of the sloneA by mathematical nodele (considering the regional forecasting)
is impoasible; therefore the forecastin~ of seismogravitational danger
must be carried out prir~arilq by the seismostatistics and the naleoseismo-
geological data (on an engineering-aeismogeological base).
The enRineering-seismogeological re~ions Where there are eraces of posrer-
ful Reismogravitational phenomena must be closed to large-scale construc-
tion. For example, the village of Khait. Which Was destroyed by the land-
~lips of 10 July 1949, was conetructed in the path of two earlier such
landslips, and now everything is ready for a fourth seismogenic landslip
(Solonenko, V., 1970a,b, 1972a, b).
31
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32
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~igure 8~ Avalanche in the Central Graben of the
bovachanakayg Structure (left scarp in :ig
' Photograph by V. P. Solonenko.
In tl~e vicinity of SArezakoye Lake (61 km long, up ta 505 meCers deep) formed
~7s a result of the seismogenic landslip on 18 February 1911 (*i~7) there
arp traces of far more ancient landslips. At the present time on the right
bank of the la~Ce more than 2.2 km3 of rock are ready to avalanche. On
the left bank fissures have loosened a mass of rock extending 2.5 km. Thus,
it is clear that the Sarezskoye Lake can at any time become a source af
disaster in the Aartang, Pyandzh and the Amudar'ya Valleys. A special
commission on Sarezskoye LAlce working in 1967~ U11~@ A conceptually correct
decision tut one that is erroneouswith respect to specific recommendations:
in orclcr to g~sarantee stability of the Sarezskiy slide rock, it was
- proposed th~t the level of the lake be loWered by 1~0 to 150 meters,
Uuildin~ an 800,000-kilowatt hydroelectric powerplant (Poslgvskiy, 196E).
'Che commissionbegan with the fact that when more than 2.2 km3 of slide rock -
nvnl.7nches into the lake, its level can rise 50 to 60 meters and reach the
c�rest oE the slide rock, that is, only the possibiliCy of a simple rise
In w~~ter ]evel wa~ taken into account. By the existing analogy, the wave
hc(~ht Juring auch a siide can reach many hundreds of ine[ers,1 and even if ~
tl)urinfi the e.lrthquake on 1.0 July 1958 in the Lituya Day, a landslide
tnt.hl inF 3(1. 5 mil lion m3 c~~used the Water to splasr to a hei6ht of up to
516 metcr~. Giant wnves were noted in the same bay during the earthquakes
of 1853 or 1054 -12~ meters, 1874 �25 meters; 189Q 61 meters;
1936 147 meters (Miller, 1963; Tocher, 1962).
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it doeA not brenlc thxough rhe glide rock, on fa111ng ~rom ehe kiLomr_�tier
heigl~C it wi11 desrroy the hydroelecrric powerplnne, and everythinE; in
the 13nreang Valley below~
Inasmuct~ as the statistical data have deciaive aignificance �or predicting
seiemo~ravitaCional phenomenn, we conaider it exCremely important to
catalog them.
Seiemogenic Sedimentary racie~
Tn addition Co the direcC signs (seismic dislocaCions and seismo4ravita-� _
- Cional phenomena) Che seismogenic sedimentary facies can indicate earlier
powerful earth~unkes even for periods when there have been flareups of
seiemic activiCy (ACTIVE TECTONICS..~, 1966, pp 29-34). The intrusion
of th~ coarsely clastic, unsorted sedimenta which were unlayered or have
uncleveloped bedding, into the rhythmically cons~:ructed foothills section , !
intermontane basina and largz valleys,especially wiCh anomalous development
with respect to area and remoteness from rhe feed areas, can indicate the
- relaeion of such deposits to the disastrous earthquakes. On the contrary,
the introducCion of fine-grained sediments into the coaraely clastic
alluvial and proluvial deposits of Che mountain valleys and basins indicates
the sudden formation of subchannel f.acies which can be connected with
covering of the river beds with seismogenic landslips or seismoCe~tonic
dams. In the mounCains of. Tyan'-Shan', Par~~ir and the ad3acent regions of -
Af~l�nisCan, many lakes are known which were formed as a result of chocking
of Che rivers by aeismo~enic landslips from tens to many hundreds of ineters
high.
The valleys of many of the streams flowing into the Baykal were covered by
the landslips, in part seismogenic. For example, the valley of the
Selengushka~ River (the right tributary of the Snezhnaya ~tiver) at the
Snezhnaya seismogenic structure was �illea with slide rock to a hpight of
ahout 100 meters. The dam obviously was broken ttaice, but now a chocked
lake about 2 km long still remaiae.
The s}~arp replacemenC of the litholo~ic types of sediments can be caused
by earth and mud seismogenic atreams. Thus, in the case of the ear;hqual:e
of 9 June 1887 in Zailiyskiy Alatau (Mushketov, 189Q), there was a mass '
Eormation of earth (loess) streams. In the ore-bearing valleys, they
EYequently became mud f.lows. The deposits of these flows formed terrace:.~
up to 50 meters high. Many of them went out on the plain and covered ,
it with a slick up to f3 to 12 km in radius in the mouth of the ravines.
- In all of these cases the fine-grained deposits, without any intermediate
sedimenKs with respect to granulometric composition covered the coarsely ,
clastic alluvial-proluvial deposits.
It is nntural that it is impossible to isolate the seismogenic facies of
the sediments onty with respect to sharp renlacement of their lithology, _
and careful complex analysis of the paleogeographic conditions of the
34
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ri~'~�~u�ul~~~ lun ~?f nrdimrntN. thr t~rtnntr~ rr~,tmr nt thn dfnrrtrtn nnd thr
Nc~tMmu~~~~nl~~ plic~nnmrnn c~f ntl tyaea ia necenKaty.
'~I~e col ~uvium r~t ehe RJ tde r~ck fn~i~d in the ~onea wi[h higt~ gei~aicity
t~ ~iqnt[iC~ntly more utd~eeprtad thAn uen Assua~ed ~e~rlier. ItK qre~ter
part ig docurnenced s~A gl8cigl depo~sits dr vateht'OCIC ~tr~ms. The
coaipoeician of tt~e lAndrlide o~p~ deppnde on the geologicat, t~ectnni~c,
~~Q~oarphologir~l conditi4ns, the kineti~s of thp landKlip, th~ incensicy
of :!~e ~enrihquake, the degree of intensity of the roek c~~nifs and
g~oqr~phic mQdiwn.
in the c~~e of the land~lip fsules, the shifteel rnr~~ges ar~
~plit intv Qnormous block~. In the firet nc~ge oiten the sail Af1d ~1I8f1CN
lnyer iA retained. The surfa~ce of the edvsnce, ~anrt ahifted stqp,eg ie
covered wi.th gr~vel-block landalide n~[erial cominq down off che slvpee
of [h~e uf~per ecr~rps, On the surface of the land sl ip- f au1 t
etay,ea, the loose tmterial duting the ~ourse af the shift
(u?ore pr~~i~ely, at tne tirae of it~ sharp inhibiCion or cegnetind of motion)
spurt~ ~nd Eorms d~o~itianson~ts.~e surfare of the scarpe cdv~red vith
~~u~h c_nners, reAemb2ee in the fresh form the colonien of teraiite etruet~ixc~r~
(Solunenko, 19b3a, 1974), and sub~equently, their enict~relief is ~imilar
, to the Hoffoaion-subsidence relief.
= Un the frontel edges of the seismogtnic landnlides ~oeaetic~s characteristic
cun~,l are forAed frosn extrusion of. clAStic materi~l up to 10 a~etera
hiKh or more (SolqnQnko~ V,~ 1953, b, 1966, p 11).
~ Th~ inJex of seisraogenic nawre cf e 18ndaiip can be the na[ure oE the
clastic rn~~terial itaelf $nd the morpholoqy of the l~ndslip maas: the
cnRCade profile, the large block~ obeliska, end so on squeeaed out
of che eeneral, ~re ~r less unifora? ma~s (SolonenY.A, V., 1970b).
Soraetim~s it is possi~le co e$teblieh the correletiun betaeen gn ex~otic
lay~r ~ediments and a specific seisa?ogenic structure. Thus, for
examplc~ tao 1nrKe l~ndslips chocking the ShAr[lay River Cenyon e~re
qeneticnlly connectad aith the Shartlay seis~aogenic structute. The
tr~ceR ~f the vater and rock saud~lide fora~ed an breakthtou~gh of the land-
Klip d:~c, can be Reen in the c~osn aection of the ren~ ina of che debrie
c~ne nree~erved in the mouth of che canyon. ?'he debris cone of tfuit tiae
~l~,ny, the upthrusc bank was droDpnd er?d covered aith aodern proluvi~m.
The up~er li~riz~n of the nroluvi~l depo~t.t~ differs shhrnlr frow che
ntratifi~ed, ordirwry proluvial deposits uadNtlyinR it it is larRe-
_ blu~.k vitt~ bouldec-block-rubble fill. 7he basic aa[erial of i[ ia
ehar~ctertstic of landslip facics and not fot pr4luvial-alluviel faciea
liY.e the ruiterinl uf the rcxs.~ininR horizons of the debriR cone. Zt doe+~
noc hnve anything in comnan vith [he materiel of the aorAine deposits.
T'tic cr.otic nature of chis layer indicetes the exotic conditions ot its
for~ati~n (SolonenY.o. V., 19b2b, 1963c).
- 35
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~in~ult~neou~ly, the diaegtroug development of the lendglide f~cies of
~~i~niEt~nnc ~rea can bp a sign +~f their r~lation td ~trong e$rthquakeg.
'Che~e tAndhlide f~ciQn ~re knnwn nn thp south ~hare of geyY.a1 ~nd in th+~
virtnity of Lske Guninyy in 'Ccansbaykal.
Vu)~an~Yeric term~tiAnn r~n in~iie~t~ arcivatian of aeinmic sctivity. in
the 5t~novoy ne~toc ~f th~ fiAylc~1 rift ~y~tem it in pvn~~ble tc~ ~~ee four
nqe~ af ~eignic e~tivetfon when the d~ep a~agaaa-Cdnducting
fractureR vere forraed: in the Upper popleir~tocene, thQ louee plpi~tocene,
the upper plei~tocene to louer holo~~ne ~nd uppec holocerte. We ~te bb~eev-
_ lnp, echo~n df che~e event~ ~tt che presenc titae. The ~pi~enter~s of ~ny
veak Qhrthquak~s, ~om~timQe ~~rthqu~ke teenche~ (to de~xe~~ per d~y) aith '
~ depth nf centern of
about 25 kta ~re coordin~tpd with the pl~i~tr?Cene-
holncene and holocene velc~noes.
'Che conatsnt faraeation of. neptuni~ dikp~ takes place in the ~ei~mically
nctive reqi4n~. ~n exla~ninin~y the pleistoceis~ zone~ df r.wdern p+~+erful ~
e~tthquake~ (farcp 9-12, M�f,.5-8.6) and ~tudying the paleoseismadiglocatiAng~
w~ observed the forrnAtinn oE ~~is~aogenic nepcunie dikes of t~m typeg:
ascendinP and descending. The nscending dikes r~re Eot'med by [he introduc-
tion ~f vet ~r v~ter-beering eoil into the fieeuree, a~ a rule, sand,
qflty, ~andy Qnd other type~ of soil. When reaching [he surfACe they
aps?ut nnd fot~n ~ud cones. The neptunic dikes (or gystems of the~) can be
~f atp,nificanc :e~qth. Por ezamrle. in the cgse of. the central 8~yka1
rnrthqunke of 29 Au,~u~tt 1959 (force 9, !t~b-3/4) che main line of the mud
di~r_I~er~yes wae nbouc 10 k~ long. The ntripping of the ~nil d~mnnetret~d
tt~~t chere ere fissures filled vith silty sand quicl:~and running
betacen che Gn~d cone~ (Solonpnko, V., Treskov, 19fi0).
The descending dikes are fotaEed on filling of the aeist~ogenic fissures
vfti~ cingtic materiel ahich travele upw$td. Thia tvpe of neptut~ic di~e is
developed quice broadly in the seismic region~, especially where che
sa_isawdi~lvcationa ~re connected aich shearing of the earth's cruat.
Ab~nrpti~n of cleRtic a~aterial taY.es place in the fisaures for tens pnd
hundreds o! years. Thc preservation c,f the g~iss~ioc~ctanic figsurQR in the
reltef ta poeaiblc c?nly au a r~~ult oE thiB eaechbnism; otherviBe tiiey are _
quic'r.ty leveled, in auch fissureae fre~uently sinka are obeerved
nb~nrbinY ati+allos~ holes ftoo~ fractione of ineters to tens of ineters deep
nnd in disneter. In the fiseurea and ~+alloa holpe, not anly is finely
rinacfc sn~cerial ebsorbed vhieh is retaoved from the slopea. but slso
blorka up co enoraaus on~s of 12 to 15 roec~re inclusively (~CTtY~
TF.CT~;i1C5,..,, 1965, p 193; Khro~averikh, 1965, p 60). The chick (up to
tenR of inetere) neptunic dikes Eillpd vith their ovn breccia. extra-
ordinarily nonuniforsa vith respect to Rranul+~aetric cosaposi[ion are 1
f~?rm~�d in chie aay. Theae dikes reach soc~e depch still unkno~m, but in
mnny c~n~~ ic is n~ lese th~n many tenn. and raore aften, hundredn of
eaetera, for thr depch of the svellosr holes in cheir body reachee 54 ~
~e[ers or care f5olonenko. V., KhrosaovskiY.h. 1974j. ~
36
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'Che mylnnitpr ("tectdnic clay") er~ a~p~~igl eyne of ~ei~tnogenic (aeisrao-
tertonic) f~r~tion. Ag thp experience of thp Gobi-Ait~y parthqugke h~~
gfinwn, th~ mylr~nite~ are fe?t~~d Et'c~ the most varied rock (froa~ ergilltte~
to qr~niteA), but they bggi~Ally Are o~ one ~~~poeitinn hydrosnicg-
~onta+orillonice. Their e~t~blishpd thicknpg~ ig up cc~ 1~aeter. Th~y have
b~een far~ned not anly it~ pra~etir~ inet~ntaneuugly, but vece gqueexed out
of thp rracke like p~sEe And in p18c~g fora~ va11~ sore th~n 1.5 m~ters
hiqh C."~olatt~nko, V., 196~a, PP ~23-~26; Salonenko, 1~G5, 1966, pP ~42-~45).
The depogite nf the ~o-e~11ed turbid flovs can dccur ~s e Bpeciel type of
Aei~raog~nic sediment in the 1er$e bodie~ df vater.
_ previou�ly Attention wa~ ~iven to th~ Eact that the ~h~rp replaee~nc nf
the deep watpr ~edi~ents vith rh~llov vat~r ~neg, the aare st~, aith
coa~t~l f~une ~nd rippie anrke ~ith ~cr~tige~phic diecontinuity ig ~on-
sidered nA unconditional prooE of th~ courae of eventgs t-- r~pld
tectonic uplift of the ~Qa floor~ 2-- regreseion of the ee~, 3-- coaci~
nQntai devie~ion, 4-- tr~ns~ression, 5-- reetc~retion oE the deep vAcer
rrKfine. It ig clear co ~very geoingigt that at le~~c tens of ~illione of
yearR ~re needed for this eourBe of. pventA. In re~lity, this can o~cur
- tn calculabl~ numb~r of hou~s (Solan~nko, V., 1974a, p 25). This cype
of ~xtrc~ordinary etrAtigraphic section can be created by ~eigmically -
excitrd earth str~am~ sub~qual aud Elovs (5olonenko, V., 1973a). As
a result of ptecise recording of the cis~ of ~gr~hquakes gnd damage to
undergrvund cebtes, significant fectuai data hae b~en accumulated on thp
n~vetnent of the seismic~lly excitpd subaqual eaud flowe. Th~ Grand 8eni~
earchquake of 18 tiovembpr 1929 i~ a cl~egieal example (force 9-10, ~t+~7).
During thie earthquake, 12 cgblee located up to $00 km frc�a the epicenter
vcre succeesively broken. Tt~e apeed of the suhaqual aud flov vas about
90 ksn/hr on the continental stope, and 36 km/hr in the abyesa~l plain.
Uuring th~ Algerian earthquake of 9 June 1954 (force 9, 1~N6-3/4), five
undervacer cables aere broken laid at a distanc~ of 6 to 1~0 iu~ froa thp
_ coast oE Algeria. The gpeed of the fla? on the continental slope vas 60
km/hr; on the deep aater plain it dropped to 8 ken/hr. 't'heae apeed~ end
the tength of peth oi` the eubaqual a~ud flows nac r~tcainable vithouc seisoic
excitation exp]ain their gigantic erosion activity, the ~enetracion to a
depth of up to 4240 meters of the coastal caarsely clastic deposics
(Cudzon Canyon) forming cones e[ the mouths of the unden?acer canyona
vf?i~t~ are worphosculptur~lly s Lniler to the proluvial debrie cones and
~beence of a connection between some of th~ canyone no[ only to the
continencs end s~outha nf rivere, buc alao to the shallow aeter (the canyons
on thc H.~rian underuacer ridge Z00 km eouth of 3apan).
Tt~e undrr;rater cenyona and anomelous distribucion of the sedimencary
_ Eacieg .~re charact~ristic noc only for thc eeas, buc Also for the large
contlncncnl bodie~ of water in the highly seiamic regions. In the seykal
bnsin there are undervatcr canyons And intruaione of coarsely clascic
depo~ita into the deep-vgter eecciona ~f the basin and eections free of
sedienenc co e aiqnificant depth. All of thia is unexplainsblp vithout
considering the iwr+erful aeise~ic osciltatione.
37
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wOk ~fNptC1AL U3~ c~NLY
The l~olntion nf the ~~igradgenie facipe of the ~ediment~ from litholdgiealiy
~tmitqr fnra~~tlr,n~ rpq~~ir~a ~~r~at d~a1 of ~tcpn~idn and ranndt al~ray~ be
epli~biy ~eee~pli~hrd. Th~ moet ~requent ~rror whi~h nugt be ~neountpr~d
t+hen uAin~ th~ nt~teri~l~ o! dth~f ~edlogists is the cla~aification of the
g~i~rnap,enic land~tip and proluviai-1ar~d~lip faei~g ~a gi~~i~l, ~lthnugh,
in ~ur apinian, they ~re eamp~ra~ively ~~~iiv digtinguighed (vith re~pert
td ghape of the clastic mateei~l aad bloek~, cumpd~iti~n, nature gnd
car.rpveition di the filler, th~ gl~rial gtri~tian t~r ~b~~nce df ie~ the
cumulative micro and me~efar~ag of r~lief, the ronfiguration di th~ e~rth
covered by the deposits, Ehe ~cco~panying mnrpho~culptur~l ph~nomen~, and
~o on).
It i~ anpreci~bly mere diEfieult to digtinguish the ~olifluctidn rock
~tre~tt~~ froa~ ~he ~~ist~g~nic l~ndglip and landslip~prvluvi~l forcnationg
~ ~t the feet of the mduntains (the oblique piedmont plein~). H~re it ie
necexBary to cangider th~t in the plei~tocene and pgrt of the holocene
the permafro~c aae developrd eppcecidbly more bcdac~ly th~n at the prpsent
time, e~nd the ~oliflurti~n proced~ea had ~ region~l ns~ture. tn ~ome ca~es,
- the coaatr~l bre~cie of the die~ppe~ring bddie~ of vacer, che aval~nche
d~pr,sit~ ~f dth~r ferrn~ti~n~ ~f the eoliuvi~i typ~ c~n ~au~e c~nfu~ion.
~ Far di~gnaeis of the ~edi~ent~ it is nec~~~ary to gtudy the gr~ag oE [heir
pr~p~getion, thirknpse, co~o~ition and relatinn~ to the g~iemo~enic
structure~. and eo on.
Age of i~aleogeismodtelocations
The d~[ermination oE the c~ore or lesg exact age of the paleoseismodisloca-
( tions etill rea~aina a Weak place in the pal.eoaeismo~eolo~ical method.
This is connected noc only vith procedural but also practical difficulties.
Until recently both in the USSR and World practice only our s~aall -
coltective at the Laboratory of Seismogeology of the Institute of the
E.~rch's Crugc has bpen eng~ged in sygttm~tic paleoaeistaogeological research.
in che remaininP highly seismic regiong of the earth, che method, alchough
used quite broadly in recent timee, hae been u8ed sporadically, for the
most part vhen examining the pleistoceism zoneg of awdern pvwerful and
dis~ucr~us earthquekea. The determination of the exace age oE the paleo� -
~eiam~~dtstoca[ions requiree peinatakinq, detailed ecudiee, as a rule, aich
~ a iarke volume of entth �ork.
6'or detern+inatton of the a~p r~f the rQSisfuel setgraodeformacionR, the
Cntlrnring methods have been used end can be used in the future: geologi-
r_wl, englneering-geolaRical, hietorical-archaeola~!ical, dpndrochronological~
~nd rndio carbon.
Ry chr ugual geologicnl saethods, in the overvhelmin~ majoricy of cases
t1~r n~e ~f the residual seisnwdeforniations can be determined highly
npproxfm.~trly, which can have grent si~nificance for knos+ledge of the
- evr?lution of the aeistaic activity of the region, buc noc for applied
tiUt~AREA. In order to deter~aine the level of iaodern seiswic eccivicy of
the neotectonic atructures it ia necessary to knoi+ the ~vents of no more
38
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Pdt~ dpt~ICIAL U3~ ONLY
th~n the firdt thou~nnd~ d� ye~rg agd. Th~ ~xtr~pnlatinn of th~ ~v~ntg
further in th~ pngt to mnd~rn tim~g cgn i~~d to thp gr~a~p~t ~rror~: in
n11 seismic region~ Wher~ corr~~rehding mat~riaig apr~ c~btatn~d ~.ttongoli~-
tl~yk~l~ C~ntr~l A~i~, thp C~ucggug, N~dit~rrgne~n, Iran, end so on) ehe
artamlC nctivity ef g~verel thoue~nd~ nf y~~re ago Chnngpd nherply~ e~ n
rul~, in th~ dirpction op a dpcr~a~e.
`Ch~ p~1ea~~ismog~ologieal daea ~re ~ chronirle ~f the m~gt poo?~rful
~~rthquake~ iMprinted in the g~olagiCai-geom~rphoingie~l d~~um~nt~ of
th~ perth'~ ~~rface. By eh~e~ d~cg, in the Baykal rift xnnp we have
e~tpbliehed four outbreaka of ~Qiemic ~~civity. In ehp r~~ion of the
expangion of th~ riEt r.one on ite ~astern f1~nk in the upp~r hdldc~ne, the
~ei~mir ~~Civity inerea~ed ~harply in conn~ction vith the migration di th~
riftngenir proce~~~g cn �he ~aet ~f th~ apparerit end of the rift ~ygtem
(5olnnenko, V., 196E3a, b), and on thp gouttn+~~tern periph~ry, in eastprn
5ayan, it Jecreaeed.
tn the norttnr~~cera Ceuc~eu~, according tn the pgleogpiemdgpological
nnnlysie A. B. O~trov~kiy (19~Oa)ieoleteg [~?o ageg of activatinn of the
a~i~micity: 1-- ~pproxia~acely in the middle of the lat~ plr~istacene
ond 2-- historic, ending at the b~ginning of che first thougand ypars
A. U.
Nith re~pect to the paleo~eismodiglocgtions in th~ vicinity of che
Ta1nAO-Pergan fault, V. K, Kuch~y (1971) establiahes the maximum vf the
Aeismie accivicy Ac about S~J~000 years a~o, a r~duccion in thp maximum
forc~ of the e~rthquake~, 10,000 y~ar~ ago. Thp cadern earthquai:es are
the weakegt in a 50,000-year period. The paleoseisawdislocations have
been videly developed in the vicinity of the Uzhungar fault (Voytovich,
1969). Nevertheleae, the modern eeismic activity of it is los~. Thie can
eitt~er indicate recent chaagee in the seismic regime or temporary seismic -
quiet. The importance of che statement of epecial paleoaeisnageological
rpsearch in such area8 ia obvioug.
it ie possible to use the engineering-geological methods for approximace
dacing of anecific seigoiodielocations. Data on the rate of deatruction
of che rock and raovemenc of the eoil on the slopes can be uaed for this -
purpoac.
I
Wherever the b ed ro c k has heen uncovered as a result of seismic
deformaciona, che time of this slipping can be calculated by the depth
of destruction of che rock.
Under the conditions of che Baykal region, the formation of talus,
including structural, tat;es place at greater sreed (cm/year): diabases
1.3; granite~ 2.3; granite-gneies and gnei� 3.3; crystal limeetones~
marble, maeAive Jurn~sic sandstones 4.4~ thin-layered Jurassic sandstone
9.~ (Solonenko, V., 196~b, p 17). 8. A. Agafonov (1974), vrho perfonaed
speciel observations in ex~erimental areas on crystalline rock obtained
39
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the gnrne r~t~~: 1~.5~87.b rom/ye~r. It i~ ng~urgl that th~ w~~th~ring
praeeed~ n~nUnif~rmly, th~ r~t~~ ~redu~lly chdng~, end dn reeChing ehe
thirkn~g~ df ~rintpr freezing af th~ ~rdund, th~y drap ~h~rrly ~lehou~h
the formation of the talus does noc cease (as a result ort annual
flur-tu~cion~ in temperetur~ c~nd chemicgi W~athpring).
In thp ~ae~ df eons~rv~tion nf th~ gpi~mogenic d~form~tinng nn ehe gC~ep
glnpeg dr dt their ba~~, geme id~~ of th~ir ~gp ran be dbtnin~d :rw.n the
cnlcu~atinns of the ~peed of movem~nt of the ground. Nowev~r, in thig
case We cnn, as a rule, obtgin only the upper ag~ limit~�or in the seismo-
~enic ;~o inte uauatly int~ne~ ~bec~rption ~f ~lasri~ matprial takeg p1~C~,
~ncl th~ h~ighe of th~ se~rp~ ~an vary during eh~ courg~ of gubs~qu~nt
(nfter th~ Qarthquak~) raov~m~ntg of the egrth'g ~ru~e.
'fhe speed of the lonee ~aterial und~r the cr~nditiong of 8aykal seigmir
b~lt ig v~ry high: in the bald peak zone, on gldpe~ ~f 3q ta 3S�, thp
gnil ig ~hifced 4 to 5 cm/yenr (Agafnnov, 1974); che speed of movpment
nf t1~e placers ie up cn 145 cm/year, the denudation meter is in placeg
only 210 yegrg (5r~lon~nl:o, V., 1950, 1960b). ProgpeCting ch~nnelg fre~
quently are completely leveled in a fe~+ yeare. The cuts on the KYU~t~baykal
_ railrnad up to 6 to $ metera deep abandnned in 1912-1914 not only were
filled wtth e~lug by 1941~ but in places forests had aopeared on them.
'Chese conetantly active factors, to eay nothing of the "volley" removal
of ineterial from the slopes (during rain, avalanches and go on), mugt
level the static forma oCCUrrieg during earthquakea of an intensity of
force 9-10 during the courae of 10-~5 to 1~0-150 years. No~,rever, the
~o ints remain. for a longer time, fur the clagtic material is absorb~d -
in them.
In recent times efforts have been made to deterniine the seismodeformationa
and their approxia~ate age by cave etructures (Langer, 1970).
The archaeo).ogiral and hiatorical data can give more exaCt information
abou[ the seismodislocation time. The breaching of encampments gnd
gettlements by a seigmogenic structure offers the nossibillty of
determinin~ its upper age limit. ~or example, by the presence of the _
tate neolithic culture, the age of Pogdl'al:iy Sor the analog oE the
i'rovc~l $ay on Lake Baykal has been established at no r.are than
2000 to 3000 years; by the dynamics of the shoals and sandbars, no less
than 500 years (Rogozin, I974). The second [igure is cloger to reality,
~ for at the end of the 17th century and beginning of the 18th century the
rcmains of the trunks of a aubmerged forest etill stood in the bay.
There ~re especially broad possibilities for using historical data in long
inhabited areas With a thousand-year culture. For example, ahen study-
inr tl~e consequences of the earthquake of 31 August 1968 in Iran it aas
extablisl~ed thac in the last 100 to 20~ years the underground water
galleries are shifted by more than 10 meters to the left (Ambraseys,
et al., 1969, p 10).
40
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V, ti, ~'rifhndv (1971) tlr~rribpd th~ ~hift of the Kahriz-w~] 1 lin~ nbnv~
thc undrr~reund ueter ~nlteci~A ~.n thp vicinity of th~ t'din Kobpt-ba~
Eeu1t. Dep~ndin~ on th~ eime o~ eongtru~eion, eh~ K~hrix 1in~~ w~re '
~hift~d ~rom fl tn 3 m~Eerg. No~r, from the hietorie~~ ~nd er~h~eoingical
r~tudi~g ~~iemaloqi~t~ ~nd s~i~mo~eologigte e~n ferr~t out ~ grpat d~~l df
import~nt information ebout poaerful parthqu~kes fr~quently W~i1 d~c~d,
t~g We h~ve done ahen ~tudying thp epismogeologyr of th~ aeet~rn Gaue~~ue
� (5olnn~nka, V., Khromovekikh, 1974).
The higt~ri~~l ~nd ~rcha~oldgical d~tg cnn be direet Qnd indir~ct. There
i~ no doubt that their rol~ in the dating uf th~ powrerFUl ~~rehqual:ea of
thp pagt, th~ time df fdrnation nf the eeisnagenic strupturee, d~t~rmine~
tion di th~ recurrence r~t~ of th~ Gacagtrophic earthqugkes, and evolution
of gei,~mie prnc~~ges will increas~ quickly.
'I'h~~ dendror.hrennl.o~icr~l method ie appli~~bl~ for dating eei~mogenic
stru~tutep in th~ fore~t zone. It moat pa~ily offer~ th~ poesibility nf
det~rminin~ th~ loWer ag~ l.imit nf the atrucCure with r~spect to th~ age
di the trees grnwing in the seismodeEormationa ("a struccure no younger
chnn ii yenrg old'') .
L�'xnct dntin~ is poseible �nr young etructurea 1n ahich Che trunks of the
felled trees or, by fortunate gccident, uprooted treea were pregerved. The
rnrrelation of che annual ringe of live and dead tr~es c~n permit determinn-
tidn of the year of formation of the aeiemodislocation~
'Che dendrochronological method has be~n used in the pleistoceism zone of
the Tiississippi earthquake of 1811 for separation of the Niseissippian and
~ pre-Mississippian dislocations and in Alaska (Page, 1970).
~
The experience of the application of dendrochronoloqy in the Baykal region
has demonstrated that already at 10 meters �rom the seismodislocation the
trees do not experience significant digturbancea in the nature of the Wood~
al~ich must be strictly taken into account when using this method.
Tt~e radio carbon method appears to be the mosc nrospective. For certainty
of tiie correctnesa of the an~lysis, it is neceseary to extract from ti~e
seiamodislocation organic remains ahich could not be brought in after the
cr~rchquake, which is impoesible to do without Rerious mining operations,
but we still have not had this possibility. Nevertheless, its application
offera the poseibility not only of dating the time of seismic dxuasters,
but algo determination of the direction of [he s1oW movements of the
earth`s crust during the period betWeen aeismic disasters (Plafker, 1968).
in spite of the tempting nature of dating the seismodislocacions bv the
rnclio carbon method, it is impoasible not to give attention to the~fact
th.~t the seismically active fauits are special geochemical zones, and
the primary C12/C14 isotope ratio in the plants in the seismogenic zone
cnn be different than usual, ahich can lead to sharp diatortion (increase)
in age).
41
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- anrCr ~~elr
Wherever you g~e ra~k wieh er~ck~, the
tracea of an ~~rthquake ar~ unque~tinn~d;
th~ more s~vpre, the mor~ ungeable the
d~brie, the rac~ and Ch~ m~d.
M. Lrnnonosov (6 5ept~mb~r 17S7)
Th~ ~mpirical d~ta obeained ahen 3nvegtignting powerful e~rChquak~g indi~ .
CA[EB that the ~iz~, Che tyn~s and mnrphoingy of Ch~ reg3dual dpformations
for the ~eismogeologic.~lly unifom zones nre mor~ or lesg constant. Thie
of~pre thp poagibility of enlvin~ rh~ invprg~ probipm; with resp~ct to
the ~~ismog~niC re~idual deformations to determine, of.cour~e, approxim~tely
the intensity and magnitude of the pr~e~i~moetgtistical earth!~ugkeg~
Thia s:ale c~nnot be universal for a11 seie?nic zoneg~ Th~ acale and type
of the ~eismodielocntions and tl~e gravitational phenomena d~ppnd not only
on the energy of thc earthquake but aleo on many other factorsi the depth
and mechanism of the center, the type of aeismogenic structur~, the
orientntion of the center zone, the geoingical structure of the relief~ and
eo on. For examplp, the area encompasaed by the geismogravitational
phenon:ena, their type and sixes depend on the regional engineering-geologi~
cal (including the geocrynlogical) condiCions. Therefore it is imposaible
mechanically to tran~fer the force acale from one seismic zone to another.
It is also impoaeible to create a universal forroula for calculating the
theoretical igoaeisn~l lines, although seismologiste propose and use them
for theoretical and applied purposea. One thing is certain: each poarer~
ful (M.6.5) earthquake aith a crustal center leaves ita traces on Ctie
surface of the earth, but until recently only a few simply kneW hoW to se.e
them.
The scale of the residual deformations usually is aapreciably greater than
indicated in the scales of the seismic intenaity, including in the most
perfected of them the MSK-1964 (Medvedev, et al, 1965).
The Eirst scale aith respect to residual deformations was proposed about
15 years ago (Solonenko, V., 1962b). Recently broad ne~+ factual material
has been accumulated Which Was collected ahen studying both modern -
earthqunkes and paleoseismodislocations in various highly seiamic zones
of the earth. On the vhole, it confirmed our scale of 1962~ and has not
, required the introduction of theoretical changes into it.
~
Force S(ti=5-1/2 to 6-1/2). The regional and zonal seismotectonic
phenomena can be established only by geodetic studies, but they also still
do not alwnys provide undiaputed material. The changes in the relief
and hydrography from tl~e paleoaeismogeological pointe of viea are difficult _
to detect and atill more difficult to prove. :he io~si ai8io~acio�8, as
a rule, do not reach the aurface of the earth or they are insigni�icant -
with respect to aize; therefore they are quickly destroyed by denudation.
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Neverthelee~~ under fnvnrgbl~ condiCiong, egp~~ittlly in the dry eteppe
re~idn, on the bn~i~ nf ~hc nerir~l photograph~ th~ loc~l seismodislocntionB
~nn~eim~~ gre mnnif~c~t~d dn eh~ eurfn~e of th~ p~rch end can be det~~t~d,
fnr eheir extent Aometime~ is quite si~ni~i~~nt. Fdr ~xgmple, for the
enrthqunke of 14 n~c~mber 1950 in California (M~S.6) three fqults w~re
Cdrm~d with a vereicel dieplncement emplitude to 0.2 m~ter~ on n parh
witf~ n totgl ext~ne of abauC 9 km (RichCer~ 1963, p 477). In the centr~l
Sudan in Che case of the force $~~rthquake (M~5~7)~ a etrike-glip fault -
~bout 4 km long aas formed in 1967.
In the Baykal seismic zon~ alc~n~ in one case opening of a fault was
oba~rved for an earthquake of mddern lntensity (.to for~~ 3?) 2 Ndvember 195~
(td=4-3/4, but, posAibly, 1ow) .
T!~e epicenrer of the earthqu~ke wag loc~Ced in the vicinity of the
Kh~niyskiy fault at the point of intere~ction af the blekma River by it.
Along thp fault cuCting the ailicified precambrian crystalline limestone of
th~ Udokan series of tt~e late proterozoic, ~oinCs were formed
running 200 to 250 meterA. As a result of the opening of the old fault,
absorption of the block materi~31 0~ th~ placer covering.the rent began
(Koct~etkov, 1964~ p 41).
They diEfered from the aeiemodi~glocations connectied with the force 9
earthqur~ke by the amall amplitudee of the shi~ta (the difference in maximum
ehiEts wns 10 to 15 times)~
In order to :iscover the epicenttal zones of the force-8 earthquakes, the
seismogravitational phenomena appeared to be more reliable. The basic -
difficulty here is to establish thQ simultaneousness of the �ormation
and independence of them With respect to exogenic cauaes. In the force S
isoseism~l field of earthquakes with an intensity of force 9 or more, the
residual seismogravitational deformations develop o~er a larger area than
for the force 8 earthquakea. Pseudotectonic deformation can occur here.
For example, in the case of the central Bayral earthquake of 29 August 1959
(M-h-3/4, force 9, h=18 km) in the force 8 zone, a line of mud eruptions
about 1A km long Was formed (at an epicentral distance of up to 43~45 km).
T}~e cones of the mud volcanoea are a~sociated with the cracks which are -
oricnted along the lines of the large blind faults covered by a series of
neop,enic-Quaternary sediments 370 to 100 metera thick. The establiahed
uidth of the cracka ia to 10 cm. They were filled with sand and quicksand
inJected from below (Solonenko, V., Treskov, 1960).
Such neptunian dikes can be uaed for determination of the pleistoseism
re~ions of the preseismostatiatical earthquakes. They differ from the
ordinary neptunic dikes by the presence of, repeated spouting channels.
Oti~erwise they are difficult to distinguish from the exogenic neptunic
dikes.
in che sharply broken mountain regions in the force 8(and higher) iso-
seismal area mass landslips occur. Under other equal conditions their
43
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~
~OEt U~I~YCIAL USL ONLY
number, ~iz~ and pnthg o� mntion nfCpr a fdree-8 isog~igm nre aharply
_ r~duc~d, which for r~gidnel engin~ering~seismdgeologicnl etudi~~ wi11
rermie mnre or lea~ certain outlining of th~ fc~rc~-8 zane~
~orcr 9 (i~t~6-1/2 to 7)
Thc r~ginnal .~nd zonc~l def.ormatinn~ during fnrre 9~arthqunkes ar~ clparly
exhibited only und~r ~gpecially favorable cnnditionq, predominanCly on the
low-lying banks of large bodiee o� water. The g~odeCic sCudiee indicate
movement of the earth's crust with amplitudea exceedin~ the pogaibl~
dbservaCion errora in an aren to 600-Sflb km2~
'The locgl seiamodislocgtions are repre~enC~d predomin~ntly by seismo-.
tectonic frgcturea and only in two casee have we been able to observe
gravitational-seismotectonic subsidence which can be connected with the
force 9 earthquakes.l
_ On the pnth of the seismogenic faulr or in the cracks connected with it,
jointe ~re formed which extend tens or hundreds of ineters and, rarely
more than 1 km. The total extent of the ~oint zone reaches 2 to 3 km,
and in the case of. predominance of the shear component, sometimeg up Co
_ 10-12 l:m. In the latter case obviously we are dealing not with the
consequence of an earthquake, but with total residual deformations
connected with the main shock, its aftershocke and the shifts taking place
after the egrthqunke. The initial maximal amplitude of the vertical dis-
plncement can increase from O.f3-1.2 to 3-5 meters.
The significant seismogravitational deformations are observed over an
area of up to 600-80~ km2, randomly to 5,00~ to 6,000 hn2. In the
force 9 isoseiemal area of force 10 earthquakes under the corresponding
conditions, seismically excited earth and rock streams occur.
Force 10 (rt~7-7-3/4)
In the c.~se of fdree 10 and more powerful earthquakes, depending on the
type of seismogcnic structure, the morphostructure and geological struc-
ture of the seismic re~ion, the regional and zonal residual deformations
of ttic earth's cruat are manifested to a different degree, and various
types of seismodialocations are formed with different extent, amplitude
oE the vertical and horizontal shifts, gaping of cracks and the nature
of the seismogravitational and other accompanying ph~no~ena. In the case
of the u~thrust faults, powerful, but short (from several kilometers to
15 km, in the case of strike~slip normal faults up to 30 km) 3oints
1STRUKTURY LABSKALDI I TSERI ~A KAVKAZE [Labekaldi and Tseri Structures
in the CaucasusJ (Solonenko~ V., Khromovskikh, 1974).
44
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~Ott U~~tCIAL U5~ ONR.Y
nrrur ur to 15-20 mpter~ wid~ (for upChruxr fnultg~ gtrik~-~lip thru~t
fr~u1~H nnd uvrr~hruNtr~ thc Crnc~urea nrr rreclominnntl,y rldprd) aitii nn
nmhlitud~ nE v~rticnl di~plarement of up to 7 eo 8 m~e~r~~ ~'or ~hifCg,
the ~ninC~ gre 1eg~ ~xpr~~~pd~ but the total extent of thp zon~ ~~n
re~ch 100 km. Th~ xon~i defnrmatlon~ are th~ r~ogC obvidue in thp e8s~ af
b1nc1: eeiemog~nic gCructureg. The blocks 2S0 to 300 lan2 in grea are
~hiftpd. Sometimeg grgb~n-likp sub~id~n~~~ gnd ~tir~,pp~ of Che mount~in
pe~ks oceur.
The s~iamogravitational phenompna nccur over an ar~a of uh eo 40~000 kmz.
The landelipg reach gigantic dimeneione and oft~n ~enerate geiemicgliy
exrit~d rock ~Cre~me. Under Eavorable geologiCal~geomorphologi,coi _
conditiong, eapecially in the lae~e areae, mass developm~nt of ~arth
gvalanchee is observed which can form seigmically ~xcit~d e~rth gCreamg
often more desCructive than tf~e earehquake ite~lf~ In th~ cage nf
~uffici~ntly decailed studiea, the morphogtructure and internal grrucCure
" oE suct~ atreams permit reliable distinction of them frnm the formc~tion~
of other genesig (5olonenko~ V.~ 19~Ob~ 1973a).
Force 11 (ri=7-3/4 to 8-1/4)
The regional aeiemotectonic movements of the earth~e crust encompa8e c~n
area of up to 100,00~ to 120,OOU km2, possibly, even more.
The nrea of zonal deformatione depends on the type of seiemogenic structurea,
but, obviously, it is no lees than 60~90~C20~30 km.
In order to diacover the regional and zonal paleoseismotectonic movements
of the earth's crust, detailed and exact geomorphological studi.es are �
required over a broad area which will permit establishment of a sudden
aimultaneous change in conditions of denudation and accur~ulation.
Such studiea have still not bpen performed although the first ateps in this
direction have been taken in Japan (Sigimura, 1968), Alaska (1'lafker~ 1968)
and the Caucasus (Solonenko, V., Khromovskikh, 1974).
The local seismodislocations in the case of force 11 earthquakes are
formed over a significant area (tl~ousands or up to 20,~00 aquare meters).
Two extreme groups have been isolated which have diff.erent mutual con^
versions (Solonenko, V., 1962b, 1973c; ACTIVE TECTONICS,..., 1966).
1. Itt the strain 2ones in the case of fault mover~ents, poWerful~ but
not extenaive (20 km or more) ~oints are formed with observed amplitude
of vertical displacement to 10 to 12 meters (Assamsl:oye earthquake on
12 June 1897, force 11, M~~.O), and with resnect to the paleoaeismo-
dislocations, up to several tens of ineters.
2. In the case of ahifts, extended (up to 350 km) fracture zones are
forcned With amall amplitude of vertical dieplacement. The main fractures
are nade up of fea[hering tension and compreseion joints, in placea
45
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~OIt O~~ICIAL US~ dNt~Y
(asprCi.7iiy ih th~ ~ectione wt~ere th~ ~hifCChgngpg gtrike) th~y be~nme
q~iqmntectnni~ tr~n~hE~ up tn 8�1~ met~r~ nr mare uide~ A~c~rding eo Eh~
pal~naeiamc~g~old~ie~1 d~e~, in Che pr~sence nf fnrc~-11 ~~rthqugke~, thp
"brok~n p1~t~" geruetureg enn b~ fnrm~d toith rgdially diverging ~nd
brenching n~twork df ndrmal Enule~ gnd fau1C tr~nCh~~ up td x0 m~terg
wide in th e ro~:l:y ~round ~Khromov~kikh, 1~65).
Thp grgvit~tiongl-~ei~mntectonic and g~igmugr~viegt3,ona1 d~formaCion~ c~n
b~ rerre~ented by nll known type~. `Che lntr~r enec~mpase an ~r~~ of up to
150,000 i;mZ or mnre (et ~n epicentrel digCanc~ of up to 350 km). The
farmer nr~ coordingted with rhe ~ei~megeni~ faule~ ~nd h~v~ an ~mplitud~
of verti~~1 di~pl~c~ment to several t~n~, pog~ibly~ a hundred m~e~r~~
~orce 12 (M,~$-1/4)
The shnrp chang~s in reli~f and hydrogr~phy nver th~ entire ar~~ of zangl
movementa of the e~rth'g rrust (pgtabli~h~d areA to 7,OOb ro 10,000 km2)
nnd noCiceable regional vari~tinng, over an ~rea eo 300,000 P.m2 ~nd morp.
The fr~cture zones, reactivated and newly formed, extend up ev 450 km,
pdgsibly, even more (in the Chile~n earrhquakes 21-22 tlay 1960, according
- to the geismologiC data, the fracture xone at the boCtnm of the Pacific .
Ocear~ w~g 960 to 1280 1:m long; gee Plafker, Savag~, 19~0), and the estab-
lished total len~th of the fract~res in the pleiatospism region of
cnntinental enrthquakes reachea 8S0 km (Solonenko, V., 1963a; Florensov,
5olonenkn, 1965, 1966).
The specif ic cieformations o� the force 12 earthquakes are gravitational- _
- seismotectonic wedges with an amplitude of vertical displacement of
hundreds of inetera and shearing of the large mountain peaks. Inasmuch as
the seismic accelerations during such earthquak~s can be twice the gravi-~
t~~tional acceleration, it ia necessary to assume the posaibility of
the formation of the most improbable deformations~
Until rer.ently, only one pleistoseism zon~ oE a force 12 earthquake _
completely located on dry land had been investip,ated in detail with the
~pplication of a special aerial photographic survey, the informativeness
of which was almost exhaustive. All of the known types of dis~unctive
dislocations and previously unknown deformations gravitational-tectonic
wedge with a vertical displacement amplitude up to 328 meters and shear-
ing of the mountain peaks have been established in it. The instantaneous
Eorm~~[ion of thick arylonites obviously is also a specific feature of the
force 12 earthquakes (Solonenko, V., 19GOa,c, 1963a; Florensov, Solonenko,
1965. 1966).
Seismic Conditions and Paleoaeisr~odislocations
None of tl~e existing seismolo~ic and seismogeological methods offers the
pnssibility of reliably determintng two in practice r~ost important
elements of the seismic regime: the maximum intensity and recurrence rate
oE powerful earthqc:skes.
46
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~Ult d~~tCIAL U5~ dNLY
it is impos~ible in thi~ xe~pc!ct tn under~~t3met~ Ch~ ~ignifi~~nc~ nf th~
r~~urr~n~,~ r~ee rhares~ the a~ismi,e ~~eiviey Chart~, the K~peak and the ~
g~i~mic ~.~u1n~r~bility, that ie, ehe ~~i~mol~~i~ method of
determir..cng ~h~ ma~t impartnnt param~t~rs of .th~ seigmie ~'~~im~n d~velo~~d
by X~. V. RizniChpnko, p~ al (Rixni~henko, 1958, 1962, 1966). How~v~r,
w~ ~hduid ~1~~ not over~~timace thc~n, for th~ deEQrminarion of th~ m~ximum
in~~n~iey 8nd r~eurrenc~ rate of the mose pow~rful earehquak~~ r~maing ~
Ch~ir "Ar.hill~g hp~l": accnrding to rhee~ dgta it is impo~~;,b1~ to
d~termirn~ on wh~e lev~l eh~ carve should be disconeinu~d or infleee~d ~nd
in each r~~ismic zone 3t ia neceseary to propose the possibi.lity of a
farce-9 ~arthquek~. The r~currence rat~ of the earthqualces which ia clo~e
eo tru~ ~an bp obtained only for broAd (a minimum o� eens of thousands
squ~r~ kilamptere) ar~as, and the ar~a df destructive tr~more Cof fdree ~
or mor~) in the CggE of forc~ 9~nd force 10 earehquakeg ueually i~ a tdtal
df 6,500 Co 8,000 kmZ. 'Chie ~reatly lowers the applied signif icance of
t1~r. indic~ted methode during seismic dereilin~ nnd micr~regionalization.
= Yu. V. Riznichenko emphasizes thae Che dependence of K on the activity
is nf n general nature and is almoat identical fdr nllmo~ the seismic regions -
wcal;ly nnd highly active. Therefore the moat difficult problem is
di~semination of the poesible intensity of the earthquakes which requires
~athering of historic material over Che longest possible time (Risnitschenko.
' 1973) . t,ie have already demonc~trated (Solonenko, V. , Khromovski~:h, 1974) ~
thr~t ~ven for such a seismic region that is rich in seismoatatistic~l data
~~s the Caucasus, the Riznichenko method can givp distortions of the true
pi~ture as g result of incompleteneas or nonequlvalent seismostatistical
dat~h. In particular, on the KmgX map of the Caucasus (Riznichenko,
Dzhibladze, 1972) the K-16 isolines cut the seismic zone of the main
Caticasus �ault (insufficient information!) which is unique with respect to
paleoseismogeological data, and the seismic danger of the Tbilisi region
(K-17, that is, more than force 10) is high (the relative redundancy of the
informntionl). There is no doubt thaC using paleoseismogeological data
would make it poasible significantly to refine the K~aX map of the Caucasus.
Thc prediction of powerful earthquakea by seismic cycles pr~?osed by
5. A. :edotov (1968) at firat glance appears enticin~. At the present
time this has served as the reason for broad popularization of the method.
- For large seismic zones it can be and is applicable, but within the limits
- only of theoretical-reference goals. In order to predict seismic danger
for a specific local section, it is more than risky to use this method.
"The main assumption of this procedure is the hypothesis of constancy of
[h~ seismic regimen. Without this hypothesis, it is impossible to determine
[he recurrence rate of the earthquakes" (Fedotov, 1968, p 137). Neverthe-
less~ it is well known that we cannot talk about constancy of the seismic
re~;imenfor the local areas (the earthquake prediction used in practice is
expedient ~nly in the case where we can).
47 ~
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~OR OF~'ICIAL US~ ONLY
y. A. l~eclc~~nv r.nnHicir.zH th~tC for Che J~panese-Kamch~Cka secCion of Che
1~,7~~ifir~ hc~cr~n ynnr thc~ ~v~ra~e ~furatinn oC Che ~eismlc cvcl.e (ehe time
I~r~Wnr~tt fw~~ rv~rllih~int~~~~ r,f. mnximiim fnt~rr~ M�,~7��1/4) 1ra 14f1+fi0 vrnrn. Thr
nv~~i�ii~;~~ ~lul�~~I l~~n ~~I ll~~~ IurrNliurlt ~ncl riCrerNl?uc~le l~~~r1~uIH tr? I~ Yl!l1CH en~~l~.
!t tp propn~ed tha~t nErer n powerful earChquake and powerf~l aftershock
n"nnrmnl" sei~mic regimen ariaea, of course, without d3snstrous earth-
- qunkeg in t1~e center zones (their dimensions are up to 100X50~ km; see
~~dotov, 1969, Fig 1, but the fact rhat this is not the case is obvious
frnm the dnta on eh~ zone investigated by S. A~ Fedotov. Near
Lake Hakknido in 1894 there was an earthquake with P4>8 and consequently,
in the "cenCer zone" a subaequent earrhquake with 2i~7~3/~i could be
~xpected (wiCh an average duration of ~he seismic cycle of 143 years; see
redoeov, 1968, p 124) only at the beginning of the 21st century~ Actually,
on 4 t4arch 1952 the disastrous earehquake occurred wi.th M=8,6~ aad in 1971~
with tiQ7.2. The latter earthquake cannot be considered as an aftershock
of the 1952 earthquake (latel), nor as a foreshoc~ of the nexC maximum
earthquake (early!). From the pracCical point of view it is enti.rely _
indiEferent whnt this "seismic cycle" element is; the epicenter was
locnted nearer to the island Chan the epicenters of 1394 and 1952 and,
consequently, although "nonmaximal," the earthqual:e could turn out to be
morc lilrmful than the "maximal" enrthquake with the epicenter located
far.ther from ehore.
On the Kii Peninsula in 1954 there wer.~ two "most powerful earthquakes"
in a 24-hour period (Richter, 1963; p 546). On 7 December 1944 and _
20 Uecember 1946, two maximum earthquakes occurred in th~ same "center
zone" (M=8.3 and 8.4) with close epicenters.
Earthquakes (M-E.3 ar.d S.6) with merging center zones occurred near
- Honshu Island on 23 October 1894 and 31 August 1896. It is possible ta
present a number of other examples both with respect to the Pacific Ocean
and other less active zones, r~here the duration of the seismic cycle -
"is many hundreds of thousands of years" (Fedotov, 1968, p 126). The lat-
ter immediately �excludes Che possibility of the applicaCion of this method _
for the ma~ority of seismic territories (80 to 90% of the seismically
active area of Siberia).
How canfusing this method can be in its ~ractical application of earth-
quake forec:asting can also be seen in the example of our Baylcal seismic
zone. For its greater part it is necessary to consider the earthquakes
' witti M,6.5 (force 9~~nd more) "maximal." During a decade there should be
on the average three such earthquakes over an area of 221,000 km2. In -
reality, in 1957-1967 theie were five earthquakes ~aith M=6.5-7~9; of them,
three (Nyul:zha, M=6.,~; Olekma, *t=6.5; and Tas-Yuryakhskoye, _
M~7) were in an area of less than 500 km2. -
In the vicinity of the Selenga River delta over an area of about 1,000 km2
, three "maximal" earthquakes occurred in a century; 12 January 1862,
Porce 10 (Pts7-3/4), 26 November 1903 force 8-9 (ri"6-1/2), 29 August 1959,
' force 9(M=6-3/4), and their zones af destructive tremors (�orce 8 and -
hi~;her) overlapped each other.
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P~it t7YpiC1Ai. U5~ ANLY
Al i uf the existi.n~ a?~thnd~ ot anr~lynis and fore~a~tin~, vf the seismi~
candi[i~ne nr~ ael~mnntntlRticnl, but th~ ps~leot~eisrno~yentop,i~a1 methnJ
lir~a the pa~at,bi 1 ity of obtaininq dr~ta about th~ gtron~eat Qarthqual:rg in
n mor~~ prelonped timc~~ period, Theref4rQ the determinetinn of thp r,~xinu~l
enrtliqunke~ must be r.amptex wich r~apect tn AhiAmal~qicnl end palro~etamo-
KCQI~y,ical d~tn~ '~he mnp Qf the maxir+wl e~rthquek~~s en~i their ~Vef~Ke
~lonY rnngc) r~ccurrence rnt~ mugt bc m~tclied with th~ ~~iemngeole~~i~al
dr~[~, aithout ahich no mnp ~nd n~ forec~~t enn be r~ecoP,nized as antinfsr.tory
innsmu~h the eeismic pracees i~ n qeotaqicgl pr~c+~ss, vhi~h i~ facp,ott~n
c~r not considered tn qenerel by t6~~ atu~,~ority a[ aeir~molaqiste,
Kesrntch E'rocedut'e
PirRc of all it ie nQCeeRnry t~ ~onsider that the paleosr.ismng~o~ogi~~l
~~hRCrvntiQns ~re r~ camponent port nf the ~rnapl~ex Qei~ulogical, s~iarao- _
ge~~lopi~:nl dnd qeephy~sir,al 14tU~iQB. in tf~c~ ~nsg uf r~giAnel ~nd detnilQd
K~~isr~ir. reqionnlizoti~n, nnd in thc esp~ecially highly ~~i~taic zdne~
evcn durin~ mfcr4.rrgioneliaAtian ~E4r morc~ prec~s~ det~erminntt4n of the
- tnitinl calc~~lnted fbrce) it 1A neceas4ry to cn~am~nsx or~ag nf tena
~nd hun{ir~,d~ o! tt~oueends ~nd ev~n morc thdn n million aquere Y.itrnneter~
- r+ith [hc~ p~lc~oseismogcol4qi~c~1 ~bgervati4ns, It irs natur~l th~t t~iChout
pr~elir~innry ~eriouR c~nd c~snprehenstv~e prep~rntions for field etudt~es in
~uch ar~e7a it is poRRib14 tA search un~ucc~ssfully Ear tacrrc thnn 1 yenr
f~r ~?~leoReteawdinlottt[ions, Thcrefore, durin~y the palcoseiRawqenloPic41
Atudfes~ they hnve themselves been divided into the Eolloti+ing st~p,es.
1. Prc~l iminary [.eboratory Pcepuration
_ Accurding tc~ the selerstioet4tiRticgl. historicot-c~rchaeolopical~ seisawlQp,ical,
~e~~logic_ri~ s~nd qeophysicnl., $eor~rpholoKical and other materials (depend-
tng on lacnl conditions) the Areas oi probnblt manifestation of powcrful -
ezrthqu~k~s have been isolated. and in them, in accordanc~ vith the proposed
~r knvc+n type of seisrrwgeneratinq structures, the geosaorphological and
e?~gir,eering-geologi~al conditions, the aec[ions oE morc probable sppenrance
~f reRicli~l seiRmo~e~ic ~deformacions.
2. Uecn~ling ot Aeri~l Chotographs
Pr~r th~s [RQlated regiona decodiny, of the aerinl phocoRr~phs tak~e~ plece.
'Phc� opt ia.zl Rcnl~e uf the phoeoqranhs is 1:300~0. On [hc 1:60000 scalc
phutny,rnphs, 4s our mnny yearR of experience have demoru;trated, frequently
tht~ am~ll seiRraodisloc4cionss do n~t find expressiQn ot they are difficulc
~sr ir~posxible to distin~uish from the photoeffect~ of other taorphosculptureg~
c~xp4ri~11y in fores:~d nre.~a. The l.~rqe-ec~lc photagrsphA ate decoded
for th~� K~ec[lonK of ptcviously i~vlAted structures And in the case of
tf~tir ar:rovlsu~l ex~raination end field documen[ation.
~
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pOEt OppiC1AI. U~~ dNi.Y
in Qrder tn abtain ~r~e1 iminary r~uantitgtive parttm~eter~ of the ~ei,~modi~l~ca-
ti~n~ tt iR n~c~+~s~ry to p~efacm inetrwnent prores~ing af ,~e ph~td~r~ph~.
it !a r99y fnC the t14t1!lpQC~~l~~t to manter qu~ntit~tive decoding on ~n
interp~r~~~gcon~.
ic t~ imp~rtAnt that the parci~tpanr~ in the ~~!i~mo,ppalo~irdt etudi~en
knna hoa to abtain AE~'i`t?A@EEQCtt~ without a atereoecope, whf.ch qr~atly~ ~
~r,celprgtes the ex~eninntic~n af the phr~taqrr~ph~ (e~nd for ane field sse~,son
it i~ nrcesn~ry co examine thounendg or tpns af thaUA~ndg nf them), i~�
mhke~ tt po~~tbl~ t~ tnake full Ug~ ot thQ ph4to~r~phs dire~tly in the
Cield ~nd soaaetin~e~ to con~idQr [he dc~tnils af the ~eisnwgenic and nc~n-
seism~genic r~orrhosculpcures which rannot be cauqht with ~n ordinary
gtereoR~op~ (the photoqrephs are bent for thin purpoee).
Thr r~s~ult~ nf the decading are plntted on torographic niape c~n ahich gero-
vlaunl rout~s atli b~ drevn,
Aerovisual Observationg
h~er~~viRUat obs~rvetions munt be performed not only in the sections of
~r~pvaed pr~leoaeismodt~lore[ions isolr~ted by the aerial photographs, but
atao in the ~ercionr~ of poasiblr activc ~eismogenic atructures i$alAted in
ncrordrlnce aith the geological-geophy~ieal d~ta: in ronnectinn aith the
concittianA of the die~uesion during the ~nerial phntograph assembly som~-
ttmeu even highly diatinctive s~iemodisloCations are not recorded on [he
pi~ocoy,raphs or are vcry unclesrly expressed. Previously in rNmote areae
wc performed the ~erovi~ual observationn on the AN-2 or YaK-12 eircrnft~
nnd in nearby arens, espectally during Rround field o~erAtions, on the
Mi-1 Ar the MI-4 helicapters. Nos+ the ?t1-2 turboprop helicopter is the
most cnnventent for these purpoeee (When flyi~g over seismodislocations
nt ndmissibly lrnr xpeede). With some akill wo observers (on the helicopters
_ ;4I-l, M[-2 or from the copilot's seat on an aiYCraft and the 1tI-4 helicopter,
even one observer ) usu~lly are able to see the details of thP cwrpho- '
- sculpturea indicating their eeiemogenic or noneeismogenic nature, to plot
the seisruodislocation plen and the plan of the accompanying phenrnnene on
thc s~~p, detcrmine the type of etruc[ure, gpproximately, and its pacameters
(crnc~k atdth, .~mplitude of vcr[ical and horizontal disPlrrcem~nts, and so
on)~ to tr~ke photographs and rnake recArdings, to note the tfaces of the
p,round r,~~prooch to the atructure c~nd toqeth~?� With the ~ilot, select the
ne~rs~pc lnndinR ai[e suiteble for 14nding the helicopter.
- 4, Nic1J Cxamination and Aocuments[ion
lturtnc; the field examination it is nec~essAry first of all to be convinced `
c?f t}~e rseismogenic nature of the morphosculpture isol$ted on the basis ~f
tlie rertnl phatographs and aer~visual obsQCV~tions. A[ firs[ glance this
atmpl~ prohlec~ often re~uires sharp obaervotion on the part of the
y,coloPist ~nd free orientntion in [he problems of tectonics. geomorohology,
enp,ine~rinA geoloAy~ field lithology~ petrogrAphy, end so on.
.
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p01t UNpiCiAL U~~ t~NLY
'Chr broY.en nnd plicqtive ~tructure~~ $ravitationai defnc~aatibn~ ~nd
Cnr.i~s a~ the ~edtments ~~n be A con~equence not nf che eeiamogenic
hut other proc~as~~ (4olonenko, V., 1962b; 196b~ p 33).
7't~r fn 1lnwtnq rnn reaemh 1 ~ gei~mod~forn?~tion~ s
1) Ps~ud~t~ctanic ,~~iat~ frequently developed alon~ th~ enei~nt f~ultg
g~d ter,tnnic ,~dintg volcenn-tectonic dame~ gnd d~epeee~ion,~, exotpcEonir
(di~piric ~nd ~in~ii~r structurp~~ exnfolding in the river valleyg), ~nhydridn-
~Yp~Ud1 LlCt011~CB~ Sointg of mud volcenoeq, ~nd in rare e~~ea, ~gtral
~tr~cture~ of ineteoriti~ cr8terg~ the ~dints in th~ folding nf the
he~ds of che bede, exogenic 18ndalipr, gubsidence trenrheg ~nd ~ediments
of the elopee, lsndslipg, l~ndglides, including rock, cannected aith them.
- tn th~ CAUranug cce ~ncountered curioue exog~nir fdrn~g re~drded ant
unly by aerigl photographs d~ring aerovieuel oba~rv~tion~, but glgo nn
the fir~t grnund expeditionr ~e reisnwgenic faults thege are th~ upp~r
ed~;e~ nf canyons [illed aith the landelip ma~g (the vicinity of Amtkel
Lake) or encien[ nlluvium (the kolkhid foothills on thpiGoredi4tiver ~nd
~n~t of it). The edg~ di the canyon itgelf excellently eimulates a
fnult q~nrp, and che subeidence jointe, thQ accotnpanyin~ seiaeateetanic
,jointg. ttoreover, in the walle of euch joit?te, the slip surfaceg
_ wrre forned in placeg With striaCion of the gcrike-slip fautt type. Only
det~iled investigacion (in the latter rase~ h~s made it poesible to
escc~blinh that the general direction of th~ "structure" aas decermined by
the edge of the ancient ranyon longitudinnl to the ridge, and the diBplacemenc
in thc couree of thp eubsidence of part of the blocks in the direction of
the modern cenyons tranaverse to t~~e ancient ones, created ~n illusion of
~hift. inasmuch as the subsidence ~oints qo deeper tl~en the mod~rn
~urface of the nncient nlluviuia, in placegdisplaceoreotoookplace under
- compresaion conditione, and ~rooving and slip striations occurred on the
valls of the ;oints in the liaestone;
2) ~laciol and nival forcaatione: lateral, radinl ~nd especially raarginai
channels, preseure rtw raines accompanied by glaciel dialocationa (~specia:ly
overthrubtg and large glacial erratic ma8aes), groovea on the ehoulders of
the trough valleya, subglacial holla+s, multistory valleye, longitudinal
ranparts of lateral moraines on the slopes of the valleys, fluvio~lacial
forms of relief, nival trougha and eWells, and so on.
Thc periglacial fields of the earth conee, somet Lnes the cones of the
soffoxion-subsideace relief cnn be eimilar to the seismically excited
enrth nvdlenches and atreams with regpect to morphosculpture. The
~ Rei~a~ogenic forraations differ froai the latter, as aaa noted above, by the
nreqence of spoutin~ channelo ahich are established on excavating the cones;
3) The erosion foros, including the rnud flov canyonn, the runoff troughs,
e8pcci4l ly in the field sric!~ large tectonic f ointing ahen hollorr massive--
Peeudotectonic forms of relief are created;
51
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4) ~x~~enic-~r~vitntidnnl fdrm~ (lefld~lide~, land~lipg, lnndglide ~nd
1anJslip trench~e~ uhich ~ometime~ create thp illuainn of eei~mogenir
ghearine of the m~unt~in cc~p~ ne~r the ~orries ~nd horn peak~);
_ 5) ~orrns df gelected denudation prepared contact~, includittg te~ta~ti~,
veined hndie~, in the ~rid end semiarid land~ca{~e zotteg, d~fintion fnrmg
Whieh ~r~ th+~ gh~rp~~t on cdincid~nce of thp ~crikp of g aeak lgyer or ~
Jetritug, zen~ Ntth prev~iling dire~tion ~f che uind;
6) Und~r permaf.rost ronditiong roelting of che v~eined iee, ~~lifluction
saellg dnd mountain terrare~, che front.~l ew~li~ of the rork gtreamg,
~nd ~prtng ~offo~ir~n rille;
7) Artifi~iat ghape~ ancient irrigation gystems and oth~r hydrd-
enE;inp~rin$ etructur~~, ritual ~nd other path~, ancient def~nsiv~ ~tru~-
tue~~ ahich can ~xtend tens and hundr~ds of. rilometers (the GenghiB Kh~n
r~mparc in South~en~cern Tranebaykal and Horth~r~ rtongolia), ~ometimeg
mr~ktng ~ood uge of the t~~ctenie scgrps in the r~li~f, under~round wor4:ings,
r~nd ao on.
_ With the expansion of the eeismog~ologiral ,~tudies in the various geologi- -
c~l-~eomorph~logical and landsrgp~ zones, the liet of pseudog~igmngenic
furms, of cnurse~ Will be expended, but the qualified seismogeologistg
aili digtinguish the seiemogenic formacions from similar forn~ationa nf
ocher genegis Withaut ~error if not by aerial photogrephs and aeroviaunl
nbgervations, then by ground observations, although (in rare casea) ic is
lmpo~~ible to do this aith certainty aithout c~ining operations.
Thi.a is ahy in the initial, stages of the development o: che procedure we
Warned against excess involvement of paleoseismogeology (Solonenko, V.,
1962b). Unfortunately, at the present time reports and articles have
appeared on ti~e problems of paleoseismogeolo~y based on the published data,
sometimes reinforced by deciphering the aerial photographs. This~ of
course~ is an easy~ quick aay to accumulate information, but it is the
shortest vay to the grossest errors.
Tt~e Reismnj;enic structures arc carefully docuc~ented: a general seismo-
j;ec?ic~Fical ~lnn and the most detaileci eeismogenic deforraations With its
morphometry are compilcd. The relaci~~n of the seismogenic Eormations
to t{ie tectonic structures and Reological foraiations of the area has been
discovered. The age and force of the ~ea~~hquaYes and algo the potential
seismic activity of a large morphostructure or part of it Within the
limits of ahich they have developed, and the moat probable sections of
reRidual deformations and probable paths of movement of che seisnagenic ~
landslipx, earth avalanches and streams, and so on, liave been established
by coraplex 81$ns.
In the case of detailed regionalization and microregionalization in the
_ vicinity of paleoseismodislocations, teraoorary seismic stations have
- been set up to determine the degree of modern seismic activity of the
52
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~trurtur~, cierth nnd mechani~m of th~ C~nter~ and th~ ~olution of other
qriamnqenl~qieai prnbtc~m~,
Nhen orgenizing eeiemoingical ob~ervati~ne, ag uur experience hag demon-
~tr~t~d. it i~ n~cesaary to consid~r chet th~ younger end mor~ pow~rfui
th~ ~~i~mic dielocetion~, th~ loaer their modern s~igmic activity. Por
ex~mpl~, in th~ pdwerful Chin~-V~1c~t~i;aya atructure obviously foctn~d on
1~ebrunry 1725, only dne epicent~r Wae re~ord~d in 196~-1964. The
powerful zone of young sei~mi~ diglocatinn~ on the apgtern shore c~f Baykgl
' is ~1i~htly activey Ther~fore, in guch seismic dialoeation~ it is ne~~ss~ry
to plnnnere prolonged sei~mic observntions than in th~ diglocationg with
an age of a~ny hundrede or a feo? th~usand ye~re.
_ During the period since the time of firat ueilizatlon of ti~e residual
epismogenic d~for~tiong to diecover the seir+mop,enic tectonic ~truct~res
and ~picentrel zonea of powerful earthqunkes, the correctnes~ of the
p~leoseismog~ological method hes be~n confirmed both by subeequent spiemic
eventR and the reeulte of our application of iC and ite application in
almoet all highly seismic xonea of the world. Thus, in the northeaetern
pnrt of the Baykol seismic belt noted at the end of 1956 (Plorenaov, et
nl., 196A), eartfhquakea occurred: Muye 27 June 1957, force 10-11
(M=7.9); Nyukzha 5 January 1y58, force 9(ft~6.5); Olekma
14 5eptember 1956, force 9(M�6.5); C~ntral Baykal 29 August 1959,
force 9(M~6-3/4); Tes-Yuryakhekoye 18 January 1967. force 9~10 (t1=7),
for Eorce 8(?t~S-3/4-6) and more than 30 of force 6 to 7.
The paleoeeismogeological studiea in the Central Asian and Caucasian
seismic provinces demonatrated that such earthquakes ns Payzabad,
Ashl�tiabad, Khait, Chkhalta and othera t+hich turned out to be unexpected,
anomalous Eor seismic regions distinguiahed With respect to seismo-
statistical, instrument and geological dat~ occurred in areas ~shere therc
are paleoseismogeological traces of the same type or even more powerful
earthquakes (Solonenko, V., 1970b, 1972a, b, 1973a-c; Trifonov, 1971;
Solonenko, Khromovskit;h~ 1974; Nikonov, 1974). On the other hand, ithas
been eatablished that at times the seismic danger or probable recurrence
rate of seismic disastera is unreasonably high (Solenko, V., 197$).
The paleoseismogeological method is still the most reliable method of
determining maximum earthquakes (aith M>,6.5) with crustal centers and
thcir average recurrence rate and the only method for determining the
potentinl seismic danger of aeismologically uninvestigated territories
and Wiien reconstructing the geological history of the development of the
seismic processes.
Paleoseismogeology has at the present time such a strong base that it is
impossible to shake its foundacion, and only people Who are unfamiliar
With the reaulta of the investigations of the pleistoseism regions of.
p~erful earthqunkes of the highly seismic belts of ~urope, Asia, Africa,
Ye~,r Zealand, North and South America, can doubt its effectiveness.
53
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~~x drxictnL us~ orn.Y
The pnleoBei~mo&~olo~icgl methnd ha~ b~~n ~u~firi~ntly well cheCked oue
that it cnn b~ included in Chp mgndntory ~et of criterig for ~aubgt~nti~eing
thp geiemic rpgional, detailed and microregionalizgtinn mapg.
Disc~seidn
We h~ve alre~dy nor.ed (Solon~nko, ~1., 1973e) that the paleo~eigmdgeoingical
meth~d has nnt been ~ubje~ted to subgtnn~Ciated criticiam. Moreover, ~om~
of th~ sp~ciali~te in ad~acent acience~ with seiamogeoingy have ~aeily
Come to detect paleoaeismodislocations wh~re Chey cannoC oCCUr or takp
formntions of other genesis for them dr to us~ the mpthod to discover
enrthquake epicenCers in ancient (before th~ arch~an) s~riea, and so on.
'fherefore, at the beginning of the development of the method it was
emphasized that excessive uge of the proposed method can do it greater
hnrm thnn unqualifi~d criticism (Solonenka, V., 1962b).
We t~nve conetanCly emphasized Chat the palenseismogeological method ie ~
component part oE the complex geologicel-geophyaical mpthod of determining
the level of seismic ar~ivity of aeismogenerating morphostructures. The
gtntement that "in the w~rks of certain Siberian scientists the paleo-
seismodislocatioas have been taren as a barely unique geologic~l
_ criterion of seiamicity" (Petrushevskiy, 1967, p 65) is based on misunder-
standing. In our publications on the aeismicity of large regions the mnin
body (G/5) of works deal with the geological, ~eophysical and aeismologic
criteria of seismicity.
The quite ordinary ob~ections of our opponents include: 1) residual
deEormations can occur during slow movements of the earth~s crust; 2)
resid~sal deformations are noC tectonic, but gravitational formations;
3) it is i~rpossible to determine the intensity of the earthquakes by the
size of the seismodislocations.
1. The occurrence of deformations of the earth's crust without perceptible
- earthquakes morpholoAicall.y similar to seismic dislocations is actually
possible (see p 51). However, the paleoseismogenic structures have been
discovered, as u rule, not by one sign, but by a set of signs. The
combination of seismotectonic and (or) gravitational-seismotectonic
deformations with seismogravitational is the most reliable. The slowly -
developing deformations are not accompanied by gravitational ones which
could be taken as seismogravitational.
'fhe seismo~enic deformations, as a rule, are under �geomorphological
conditions such that preservation of slowly developing ~oints is impossible
(sec p 43) .
2. Some ~pponents, who have not seen seismic dislocations in reality doub[
thetr ~eismotectonic nature and try to show (not by fact, but by subjec[ive '
notions) that they have a gravitational or seismogravitational nature.
54
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~dtt n~FYCIAL U5~ ONLY
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y^~ i� . ~ ~r . ~ . y ~{P~`~} ~ ' ..'~'.~i
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. Y~y 's1 .1 f & ; . . . i,.~ ~ ~ xt ~i Ca" :r~ ~ 1
i . P~ ! ej', ~y' . .i f,~- 7'.
t~ ~ ~ . t ~ � . . ~-T c.i..~. ~ . .
~f -iC~Y"a i ~ ~ t : - . f y
j ~ ~ ,
~ ; t ) i ~ r ~r�. - ~
? i .
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r 's~. s .+f #'~~t ~ -
e:i. � . .I~.:
Z~ e`~~f.
~ ~c~
_ . ?
_ ~~r'~
, .
Figure 9. Seismogenic Structure of Abal;ura in Svaneti a.
Strike-slip Normal Pault in Crystalline Rock.
Photograph by V. P. Solonenko
55
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h'Ok qF'F'IGiAL U5~ nNI,Y
Such ide~~ gr~ the le~~Cy d.f the d1d view~ Chgt the r~~idu~l d~forn?~tinn~
pert~in only tn the loose cov~r edil, Thp Gobi-Aleay ~~rthqugk~ fin~llv
r~fured such idea~, buC pffnrC~ ere made to revive them in one form
ar nnoCh~r from Cime to time. Ie i~ ~ympComatic that nmong the proponene~
of th~ ~urf~ce nntur~ ~eiemndigloc~tidn~ Wp do not know a gingl~ author
_ who has examined even onp disastrou~ ~arthquak~. The irr~fue~ble f~ce~
cnnfirming ~hp teCeoniC ngCur~ of gpismodislocaCiong ar~ available in ag
lnrg~ ~ numbpr one might lik~, and nlmoer pv~ry tt~w ~arthqual:e wiCh
M>6.5 ~nd a cru~Cgi cent~r incr~~~pg thp numb~r of guch factg. Th~ -
compnrieon of thp m~chanigm of the mdv~menC di the e~rth'e cruat cnnnpcted
with p~rthquakes determined indeppndenr.ly by seigmogeological gnd seigmo-
ingic methodg (Balakin, et al., 1972), of course, if Che s~iemodiglo~~tiona
- were comptetely and qualifi~dly mapped, is in itself irrefutable proof of
th~ d~ep ngtur~ of seiAmodiecloations.
W~ pncr~unt~red, perhap~, the most active desir~ Co refuCe the tectoniC
nature of the dislocationg nfCer their diecovery in the greater Caucgsue.
'Che Jiscuseion in this area only inhibits the developmenC of paleoseisfio-
beological research in the Caucasus without subatantiation. Th~refore we
shall present two examples.
dn che left side of the Tsintskali River Canyon (15 km east nf the Inguri
llydroelectric Powerplant), the Kvira structure has been mapped (~ig 9).
~rhis is a fault extendin~ about 2 km with vertical displacement amplitude
i7 ti~e Jurassic sandstone-tufogettic soil. A one-sided graben hae been
formed on its southern section (60X500 meters). The fault cut through
5 channels of temporary streams previously flowing into the Tsintakali
River, and it aent their f1oW together with the waters of a group of
powerful springs aseociated with the seismodislocations through the bro~:en
d~.vide into the Dzholori River. Two large landslips are connected with
the structure. Inasmuch as the structure cuts the divide along the
- diagonal, it is not appropriaCe to talk about its landslide origin.
On tlie divide of the Inguri and Khumpreri Rivers in Svanetia, Che seismo-
~enic strike-slip normal fault (the Abakura structure)rQjuvenated the previous
deep Er,~cture (hyperbasitea with aulfide minerAlization are tied to it
in tf~e structure zonea). The strike-slip normal fault (amplitudes 0.5-
20 and 50 meters respectively) 3.7 km long intersects the divide
diagonally (Fig 10). The fracture is continuing to absorb clastic material.
- The depth of the closed absorbing swallow holes reaches SO meters. A
line of powerful landslips is coordinated with the zone (on its continua-
tton to the easC and west).
.1ust as in the first case, the gravitational nature of the Abakura
structure has been excluded.
3. The intensity of the earthquakes with respect to seismodislocations
is determined, as a rule, quite reliably (some examples are presented in
Table 1)by conversion in terms of magnitude (according to formula (2),
p 12).
56
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` I~OIt Ot~PICIAL USL OM.Y
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57
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58
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FOR AFFYCIAL U3~ ONi.Y
t`
~
~
f
;-f;~ r;
t' t f _~~,f~
~ .
�
Figure 10. Kvira Structure. South Slope of the Greater
Caucaeus. Photograph by V. P. Solonenko.
The ratioa of Ip and M(or K), according to different authors, are within
- the limits of accuracy of the analysis (see Table 2). Therefore ehe
objections to the determination of the force of earthquakes by magnitude
in the absence of corresponding macrosei~ic data in the epicenter are
clearly meaninglesg. Nevertheleas, theae ob~ectiona have been encountered
in recent yeare ~hen diacuesing the method of compiling the new seismic
regionalization map of the USSR.
'Che force index remains and will remain for a long time the base for seismic
regionalization for utilitarian purpoeee. For the enormous uninhabited
areas or apareely inhabited~areas the determination of the intenaity of
earthquakes in the overWhelming ma~ority of casea ie poseible only in =
terma of tnagnitude aed seieaadeformationa for stron~ earthquakea.
59.
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- CNAPT~R II. STRUCTURAL-T~CTONtC 1t~GI0NALIZATION OI' TN~ FR~CEN020IC
BAS~M~NT
The gtructural-r~ctonic regionallzgtion of Ch~ ~duth~rn part of ~a~tern
5il~eria (~ig 11) was carried nut in ~ccordanc~ wiCh thp formgtional-
Htructur~l and tectonic Aigns (time of formation of the etrucCureg, true
compo~iCion, peculiaritieg~of lithogenesis, m~tamorphigm, magmatism, fold-
ing, pogition in the geogtructural sysCem and the gequence of the transieion
Erom the geogynclinal developmenC to platform). The reader will find ~
det~ileJ atructural-tectonic description of the Baykal mountain region in
the paper by L. I. Sa1op (1967).
Region of Pre-Riphe3n Folding
. In the southern pnrt of the 5iberian platform a moat ancient folded base-
ment is mnst completely repreaented in the Cerritory of the Aldanskiy
Shield. The outcrope of the pre-Riphean tectonic complexes on the surface,
their geological atructure and metamorphism indicate the complex
heterogeneous structure of the lower platform sta~e, the greater part of
whi~ch is covered under a thick mantle of slightly dislocated Paleozoic _
and !lesozoic seriea.
Aldan Shield
The age of the most ancient Aldan metamorphic complexes (the Iyengrsl;a~?a
and pzh~ltulinskaya series) is 2.640 billion to 2.340 billion years
(TEKTONIKA YL�'NRAZII (Tectonics of Eurasia], 1966), which permits them to
be pnralleled with the saamides~of oCher shields. 'The structures bordering
the ancient nucleus on the west and south (the Olel:ng and Stanowy =
zones, including the Kodaro-Udokan trough) belong to the Karelian
phase of the folding, for the deposits of the Udokan. series are '
penetrated by the synorogenic intrusions of the Kuandinskiy complex of
~ranitoids (1.650 billion years).
Severnl stages have been i.solated in the nost ancient history of formation
oE the southwestern part of the Aldan shield. In the beginning the
Aldan lithoplinth was formed (Dzevanoyskiy, et al., 1968, 1970) made
up of the early Archean formations of the Iyengrskaya and Dzheltulinskaya
60 �
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geri~g d~Cermining eh~ laCer etru~tur~l level of Ch~ Upper Arch~gtt complexeg
of th~ St~nnvoy ~nd Olekma zottes~ '1'he pl~t�oXm atage c~f developmenC
oE Chp Aldan ~hield iCsel�, o~hich was ~ub~ected Cn ~aignificnnt reworking
diirin~ quh~equenC ~pc~rha of ter.Cnnic ~rci~ario?,, be~~n with Che I,ower
!'rc~eerozoic. ThuA, thp weeCern p~~rt oQ Ch~ inveatigated ,territory (Che '
Kodarn-Udok~n. R~gion) served the accumulation baein of the terrigenic-
rdrbonnceous bede of th~ Udoken aeries during the Lower Prot~rozoic.
'Th~ pliraCive dislocetion~ of ehe Aldan Shield have been sharrly cor~~pli-
cgCed by fracturE tecto~nica. The lgrgesC faulta enter into ehe system of
th~ Str~novoy structurp~l surure which extends hundreds of kilometera to the
west and the eeet. ~t ia controlled by the basiCe and ultrabasite inCru-
siona, a wide band r~f diaphthoritic and ca~aclase rock, crushing and sct~iat-
�ormation zones. 'fhe development of the deep atrucCural auturea and large
dislocatione with, a break in continuity on each new level of tectonic
activation wae n~redetermined to a significant degree by the plan of the
~ncient faulte, and frequently proceeded along the folded substrate not yet
touched by the dis~uncCives. All of this together created a mosaic-block
structure of the Archean basement, especially broken in the deep fracture
zonea.
~eqion oE Baykal Folding
The Eolded etructures of Baykalide in Eastern Siberia border the pre-
Riphean Siberian platform on the south in arc aeparated from the
latter by a syatem of marginaldeep faults. They separate the Angara -
prn~ection of the platform into two branches western (Sayano-Yeniaey)
and eastern (Baykal itaelf), ~ained together in the vicinity of the southern
extremity of Baykal.
The Yenisey -Sayan Baykalide region forms a narrow strip extending along
the southwestern edge of the Siberian platform. It is divided by the
Bol'shoy Sayan fault into two tectonic zones. For one of them, the
platform zone, block uplifts of the ancient Baykalide foundation are �
typical, and the other, the outer one, is a deep Riphean trough.
The occurrence and development of the Aaykal geosynclinal took place in the
marginal part of thQ Archean foundation of the pre-Riphean platform
which was either partially broken and reworked or was involved in a power-
ful geosynclinal procesa. Correspondingly, in the modern erosion section,
large and amall blocks of reworked Archean rock~ developed oredom~nantly
in the platform parr of Eastern Sayan bounded on the southwest by the
main Sayan fault~ emerge at the surface.
The Archean structures inside the Baykal geosynclinal tectonic complex
itself make up the Garganskaya block isolated at the beginning of the
Proterozoic in the form of a stably uplifted block. Later, participating
in the qeosynclinal process, it separated the sedimentatian basin into
individual aublatitudinnl trougha (Okinskiy, I1'chirskiy). The uplifted
Garganakaya block was the nucleus of an anticlinorium.
61
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~y ~4
~3'~/% ~ T ~e ~ '49 ~ ,
~o ~ _
(I~{) n~ ~ V I#) ,1 -
~
~ 6o3~ubo - ~ '
I' �
6pamcr ! 0 I )
, ~ ~
(I) ~
a yr' pl
o ~ t ~ \
~
, ~ ~II) ~ o
~eqa
~ r ( t.. / ~ � ~ ~ ~r~ ~
O � e~"~
~ ' . I u wo
_ ~ pnymcx ':,w .
- o.. \u~a~
yna~+- 83 r
~ t
Ce~�M=� . , -
V
Figure 11. Schematic of the Structural-Tectonic Regionalization
of the Pre-Cenozoic Basement of the Southern Part of ~
Eastern Siberis.
Compiled according to data of A. L. Yanshin (1966)
and T. tJ. Spizharskiy (1968)
1-4 region of folding: 1-- pre-Riphean, 2-- Baykal, 3-- Caledonian,
- 4-- Hercinian; 5-- mantle of ancient and epiproterozoic platforms;
6-- faults; a-- basic, deep, b-- other, undifferentiated; 7-- Mesozoic
basins and troughs; 8-- tnain rift basins; 9-- b~undaries: a-- of the
re~ion of Mesocenozoic activization, b-- Baykal rift system.
Key:
I. Bratsk IX. Lena
II. Angara X. Olekma
III. Irkutsk ~ XI. Shilka
IV. Selenga XII. Chita
_ V. Ulan-Ude XIII. Vitim ~
VI. Lake Baykal
VII. Vitim
VIII. Bodaybo .
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_
. POIt pPPiC1AI. US~ APtLY
The B~ykalide ~c~mpt~x w~s represented by m~etAmorphic rocls m3kin~ up the
two lncR~ nynrifnnrin ~Akinskiy, I1'chirskiy) gnd the Khara~r-Dnbansl:iy
nnti~:linocium, The net of Proterozoic effusive e~nd ~~dim~ntnry focmationR
metnmorphos~d under tfi~ conditi4nx of the green ghale faci~s ~f regionnl
metnmc~rphinm and retlecting n deEined P~ntectonic rep,ime aill perrait th~e
cnnsi~l~.�ration th~t hare, in the encient Arche~an found~tipn an independent
Rn.aKynrl in.'tl ~y~cem ~rose r~nd devQloped.
_ The int~rru~l a[ru~tUre Af the synclinorta i~ made up of syumetric anti~lin~ls
nnd gyn~lin4ls; che overturned fc~lds sre observed only along the periph~ery
nr in contect aith the Archea~ bl4cks. The qeneral sublatituciin~l plen AE
~he folded str~ctures mm~etime~ ie disturbed. 'fhi~ ia explnined eitt~er by
the ~fE~~~t ~n~! the reuorking of th~a by the C~ledonian mr~v~m~ntg ar tl~e
prim~ocy nAnuniform Qrient4tion of the PrAterox4ic structures cr~u$~d by the
folded-bl~~k nnd blq~k ~tructure of the bs$ement ~~ayteev, 1963).
Tt~e Khnnuir-Uabr~n enticl inorium is msde up of ~a~rbonsceous rACk af the -
mt~~ ~~riex, snd the limbs Were rpade up of gnei,~e uf the Khangarul'sfsAyo
s~ri~c~. The t~inge of the anticlinoriwa is undulAting, aavy in plan vie~+,
++ith K~en~eral aublatitudinel striY.e. Its limbs are ma~e up of folds of
hiy,t~~r ord~r~ hnving nnalo~ous orientation.
. Tf~~ f~nYY~I zone encompaRSes the vestern and eastern B$yknl regiqn
(t'rib;~ykul'yeJ, the Bayk.~lo-Patom~koyc highl~nds and a significant part of -
che StnnovQy hiqhlAnd~�
- Tt~s Arch~enn bASea~ent protrudes in ite nad~rn Rtructurs In the form of
K~y~ral blo~ks bbunded by fault~ ~ayknl, *'uys Aa~latRkay~, ~
- 7nd x4 An. The bloc{~.$ sre aiade up of gneiss-shale and carbonaceou~-gneis~a =
Rnri~e~ With a t~tal thickne,s~ up t~ 10 to 12 kca (Prolova, 1962). Linear
ful~lR Qf predoainantly northeasterly strike are charecteristic for the
Ar~h~an aupcrcrystnlline formation, The complication of th~e large fold~d
- farm~s by smsiller ones (to miccoplication) snd n~es grani[iz~tion of the
r~~ck i+s npt~~ everyHher~,
The ~;~en~yn~lin~l compler. Af ~aykalide~ ia "ncoken down into the outer mio-
s;c~,Rynclinnl An~f the inner euy,eosynclin$1 zones (TECTA:i1CS AF BURASIA,
19h5). The forraer, in the for~ nf A broad src which i~ convex to the
- nnrth, ta lracated alAC~~ the p~riphiry of the Siberir~n nlatforra. Un the
~outh Lt is bound~d by n Aystr_na nf deep fault~ separatiny, the An~Aro and -
tht Ald~n pr~o,~ections nf thc platfArra froca the folded Bayisalide system.
in th~~ n~~rth its fald~d Atructur~ea con[inu~e po~sibly in the direction of
tf~~s ~ilyus~~ya synQClfse. In the outer zone, in addition to the already
m~cntioned b1ocY. projections of the $ncient baseraent, a n~mber of large
fnld~~d ~~ructures are isolat~ed: ?~e~herskiy, Tonodsk.iy and ChuyaY.iy
ant i~l inurin, Nac~xkiy. Ek~daybinskiy and PribAyks~l synclinoria~
Thc~ fnternnl baykAllde aone occupi~es the rentral zone af the Baykal
s~r,unt~fn r~~io~, raa~ing upthe broad, compler.ly zonstructed Barguzino- `
t'i[im synclinoriura, The r~ide of the s~nclinoriwa in ao.ade u~ of a thick
E~ 3
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(~ip tn 12 krn) ~c~t ~~f. bnnic e[[uaiv~s and [heir tuff~ af ~pilite-keratophyre
fnrmnttnn nnd m~tamnrphoeCJ ehnles, sondgtonee nnd lin~atonrs meking uP
_ che loacr etructucal ~tnge. Len~ ahaned bodiea of hyperbanite intrusivee
are conneeted aith chc f~ult~ af the pre-geykal de~osie separatinE thQ ~
puccr nnd inncr rane~t.
Rrginn of Cnledoninn i~~ldiag
~
in aastern Siberia, in acc4rdnnce aith the modern ~conc~ptg (Yanshin, et
nl., 196fi; Stizharskiy, et nl., 19~iA), the strip of C.aledonian structures
bocders the 3lberinn Bnyti;n).idc reqion ~rom the south (aee Fig 11). The
- nr~a of their propogation is bounded by the structural autures
nr.hidi~o-Vitim on the northwest and tt~nqola-~khotAk nn the southeast.
Out o( the two r~�cles af Celedoni4n folding develApracnt, early and late,
_ Anly the former hns found reflection here. The ~e~,synclin$1 regime of
- carly Cnledonides begins to be exhibited from the Kiphenn, the completion
of it tnkNS plnce at the end of the Middlr and beAinning of the Upper -
C,~mbrtnn. Aver the extent of the entire period~ fonaations ha~?e occc~rrgd
_ ahich ar~ At~ndard for eArly ste~es in the development of the geosynLlinul
re~;inns.
The Cnledonides of the investigated ares can be divid~d with respect to _
structural-tectonic peculiarities into tWO parts: Sayano-Altay ~5~rkhuysiriy
synclinorium) nnd Trans-Baykal (Dzhida and Udino-Vitim synclinort~m3. ~
Snynno-Altay Zone -
The lcnaer Paleozoic structures are repre~ented here by synclinal folds in
the tr4ughs ahich are complicated along the perimeter by upthrust faults
.ancl overthrusts. The ~edimentary complex of the lower to middle Cambrian -
~effusive-terriRenic and terrigenic-carbonaceous rock occurs on tiie erosion
Rurfnce Af the Proterozoic and Archean blocks.
?he ~nst completely Casabrian deposits are presented in the Sarkhoys~iy
aynclinorium where the total thickness af the geosynclinal complexly dis-
]orated Reries 1A b.2 I~. Alonp,Withthe isoclinal and syaa~etric folds with
- Rteep (7Q-80�) limbs gently sloping folds ~re noted which are made up of
(lexures (Vo~.kolEkov,196A; Arsent'yev, Volkolakov, 1964),
- The l~er Paleoaoic folding stage turned out to be the final one. The ~
- tectonic structure, the set of formations, magniatisni and metamorphism
_ indicnte that here the geosynclinalregirien ended in the pre-Cambrian time. -
Tn tlie west the SarkhoyAkiy synclinorium is bounded by the Shutkhulayskiy _
up)ift b.~sically made up of the pre-Bay{%al metamornhic complex belonging to -
the rcy,ion of Fiayk.ll folding (T~CTQtiICS QP EURGSIA, 1966) ,
_ ~
b4 -
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Transbnykal zane
'I'~+n auhr.onee nr~r iRC~l,ited in tl~~ 'Crnnsbayknl zonr. One af them tncompnReine
th~ hnain oE thc upper couree oE the Dzhida Riv~r and the left bnnk of the
i4dngolian port of the Sel~ng~ River is repregented by the gtructurea of
the bzhida eynclinoritnn m~dQ up oE tao ,atages of 'Aend�Cambrian depoeits.
'fhe centrgl end edge parts of the eynclinorium gre made up oE faults end
folds of difEerent order. Pirst of all, this pertains to the ~outheaetern
limb which is connected with the pxoximity of the active zone of the.
bounding deep Eoults (AfanAS'yev~ 1973).
Simple linenr fo~ds, in places ieoclinal and overeurned, perticipaCe in
_ the internal formation of the synclinorium. The centriclinal closure
ta cempliceted by o deer fault with northeasterly ~trike. In the axial
pnr[ of the ~ynclinorium a centc~~l nnticlinal is isolated ahich runs from
the borde~r, of the USSR with Mongolia to the central course of the Darkhituy -
Rtver. 'I'tce ~eoeynclinal developn~ent of the Dzhida subzone itBelf ended
in ti~r Ffiddle Cembrian.
In Che enst the Dzhida synclinorium becomes the Udino-Vitim (the sec:ond
Rubzc~ne) through the basement protrusions. Its boundary runs along the
Routfic~xtern slopes of the Khamar-Daban ridge: the Vitimkan and the
_ Tsipikan Rivers on the northaest and the central course of the Chil%oy,
Ing~da r~nd Tungir Rivers on the southeast. Similarly to the Dzhid$, it
occurs on the broken pre-Cambrian found$tion, individual blocks of ~?hi~h
_ l~.~ve been retained in the internal geoenticlinal uplifts (Zaganekoy~,
Yablonovoye, Malkhans~oye, and so on).
Hercinian Folding Region
On the Tectonic Map af Eurasia, the region located southeast of the -
tlvnRolo-Okhotsk structural suture (see Pig 11) is all consider~d to b~
- part of the eastern Siberian hercinides. However, in the description of -
the map it is stipulated that this region hns mixed structural features,
_ .7nd the problem of ahether it should be classified among the hercinides
ur meso~oidea cannot be considered finally decided (TBCTONICS OP Ei1RASIA,
1966),
Ttie geoRynclinr~l coa?plexes of the lower structural stage of the hercinides
be~an to be formed in the Ordovician or Silurian, and the end of tfieir
formation beiongs to the middle or ttie tops of the *[iddle bevonian
(T~~TA~iTCS OP EURASIA, 196b). Begianing with tl~e Devonian and, anprox-
_ imately, to the upper Carboni.ferous (in the Aginskiy trough to the
Lower Triassic), the complexes of [he upper structural stage Were formed.
~ In tfie trouphs Where the hercinides are deposited, there are silicide-
torrigenic and terri~enic formations; in the uplifts, they are supplemented
_ Iy volcanogenic, volcanogenic-plutonic diorite-granite and intrusive
p,rnnodioritic complexes.
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'Che fnlded xerie~ in the outll.nes o� the hercin~.an geoAynclinol nre
det~rted in the zachikoy~kiy, Dnurskiy, Aginekiy and the Pri~rgunekiy
Ravons.
A tt~ick (6-7 km) annd-ah~le Zach~koyskaya series oE pre~Permian ege hn~
dev~toped in the 7.~chikoyxkiy Reyon. With re~pect to formr~tions it is
~imtlnr to the Centrnl rnleozoir formations of the Aginskoye field and
northeg~tern Mongolia. The rocke oE the Zbrhiwoyskaya series are in pleces
penetrated by grenites 395 million to 425 million years old, which indi- -
cqtea the possible presence in its compvaition of Lower Paleozoic rock
(Kosygin, 1965). In the bottoms of thi~ series the polymictic sandstones
predominate. At the top of the section they are replaced by congloneratea _
and striat~d shn~es. The largeat folded forms here are the Aginskiy
enticlinorium and the Chikokonskiy ~ynclinorium.
A characteristic feature of the Aginakaya structural-formational zone is
the fact that here the geosynclinal reEimesihas been retained until the
Permian to Central Triassic (Amantov, 1963). In the Upper Pnleozoic tc~
i,ower *+esozoic, thick (more than 5 lan) series of terrigenic sediments have
nrcumulated: aleurolites, polymictic sandstones with lenses of conglomerates
anrf arPillaceous shales. The rocks are crushed into linear folds of
different order. Intensive plication and razval (disinteqrated blocks =
piled up on mountain slopes] formatiori have developed in them, and numer-
ous extended fractures are observed (predominantly overthrusts and shifts).
In the Daurskiy synclinoriur.~, the section of the sedimentary series differs
sort~ewhat from the ad~acent accumulation regions~ Here carbon-quartz-
sericite shales (in the lo�aer section) and schistose ~olymictic sandstones
(in che tops) are isolated. In addition, interlayers and lenses of
greenstone metaeffusives of basic and me.dium position are encountered in
the section. The total thickness of the deposits is to 5 km (Corzhevskiy,
~ and so on, 1970).
- The PriarRunskaya ~eosynclinal zone is predominantly made up of larg~~
clastic deposits and limestones. Sometimes acid tufogenic rock is
- encountered among them.The apparent thickness of the deposits is more
than 2 km. In the basement rocks they occur with sharp angular mismatch.
A br.lchyform nature is characteristic of the folded structures of this
~one.
The hercic~ide section is crowned by proterogenic continental or marine
molasse ~~nd granodiorltic Permian-Triassic forniations (Zonenshayn, 1967).
With respect to their lithologic attributes they are very similar to the
- hercinide sections of many other regions of the eastern part of Central
' Asia. On the other hand, similarity of ther~ to the ~eo~synclinal sections -
of soa~e of the mesozoide regions of northeastern USSR is detected. The
most ch~racteristic in thi.s respect is the Priarpunskaya zone sahere in
recent years small fields of marine L'pner Triassic and Lower Jurassic
depnsits were detected. This has permitted some researchers (TF.CT4:JICS
66
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OF' t',(11tASTA~ 1.9~i6) to ronsider the ~iven reginn ne n trnn~itiona] ~tructur.hl
r~�Yf~~i~ h~~twrr.n typl.~~ni I~errlnfdr_H nnd mceozoides.
- Region of ttesoznic Activntion
The Mesozoic tectonic-magmatic ~activation has encomp~ssed an enormoue
areu: the periphergl part o� the ancient Siberian platform, the re~ions
oE pre-Riphean Daykal, Caledonign and Hercinian folding and southeastern
Trnnsbaykal where up to the Upper Meaozoic obviously the subgeosynclinal
regime was retained which was caused by Che effect of the Mongolo-Okhotsk
synclinal belt.
The evolution of the meaozoic structure is preaented in the following form.
Since the end of the Upper Triassic, large arches have been formed the
Sayano-Baykal arch and the Yablonovo-~Stanovoy arch (Bogolepov, 1967)
or n single archeJ uplift (Koreshkov, 1960), In the Middle and Upper ~
Juransic, the differentiation of the movements has led to isolation of
the folds with lar~e radiua of curvature: the Sayano-Stanovoy outer and
Khentey-D~~urskiy inner belts of block upli�ts, the Selenga^Vitim zone of
relative subsidence (Arsent'yev, 1967)~ the Irkutsk and Chul'man foothill
coa]-bearing troughs (SAlop, 1967). In the Upper Juressic to the Lower
Cretnceous, differentiation of the block movements are intensified, which
_ promoted the formation of numerous intermontane br~sins and block anticlinals
([vanov, 1949).
Thc ;tiddle Juraacie volcanogenic-sedimentary rock of the Selenga-Vitim
. zone of relative subsidence are made of acid effusives (felsites, felsite-
rorphyries, porphyritea, quartzitic porphyries, and so on), tuffs,
tuffoconglomerates, large block conglomerates, gravelites, aleurolites
, and .zrgillaceous shales. The series are usually metamorphosed:
chloritization and silicification appeared in the effusives, and argillaceous
shales were converted in places to quartz-mica shales. The deep analogs
of the effusives in this age are the subvolcanic formations: microdiorites,
dioritic porphyries, diabase porphyries, alaskites, ~ranosyenites, and so
on.
Inside the western, eastern Sayan part of the outer belt of. the block
upllEts with block differentiation, a group of Urda-Oka grabens was formed.
They are bounded on all sides by the fracturea of the !'.ain Sayan System.
Here the Niddle Jurassic deposits are separated into the Naringol'skaya
series (Florensov, 1968) with a total thickness to 2.5 b:m made up of
breccia, conglomerates, sandstones, aleurolites, carbonaceous argillites,
gravelites covered by coarsely-clastic c~n�lomerates ~nd fan~;lomerates. The
_ rock is intensely dissociated. Near the fractures bounding the grabens
and m,zking up their internal structure, overturned folds are observed.
On the whole, simple synclinal folds predominate here (Basharina, 1973).
67
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In Che Centrnl Juragaic Cime, enatern 5uynn gerved ~ts Che bnsic s~ppll.er
of clustic mnterial for Ftlling the depresaions of the Irkut amphitheater. `
Tlic eouth edge of Cl~e latter wns ~t that time a foothills trough which
_ orcurred at the ~unction of the pre~Mesoznic folded sCructures of the Bgyknl
(northeastern) and 5ayan (northwestern) directions~ The principal age of
sedimentc~tion the Middle Jurassic was preceded by the formaCion of
the basal series from 50 to 300-400 meters thick. The amounC of coarsely
clastic materinl inCre~ses to the south. The sand-aleurolite horizons
contain numerous coal beds. In the southern part of the Irkut amphitheaker
n combination of two troughs of Sayan r~nd Baykal orientaCion converging et
right ~ngles is noted. The Mesozoic ~ynclinals frequenCly coincide with
the ~~nalogous forms of the Lower Paleozoic. Here the former are more gently
sloping and are somehow embedded in the latter. The dip anglea of the
Jura~sic layers on Che limbs of the synclinals reach 20 to 25�. �
The Chul'man trough is located in the basin of the upper course of the
Aldan. Structural-geolo~ical complexes of the Jurassic and Lower Cretaceous
have developed here which make up botii the Chul'man basin and the system
_ of grabens containin~ it to the east (the Kudulinskiy., Khaniyskiy) and the
relict 1�[esozoic denressions of the Kodaro-L'dokan- P.e~ion.
The western r~nd of the Chul'man basin was represented by the
tJizhnetungurchinakiy or Usmunskiy trough (Dankevich, 1969). It was
executed as a thick series of continental coal-bearing deposits (Itokrinskiy,
1961, 1962; Mironyuk, et al., 1971). On the whole, with respect to composi-
tion they are alike and are made up of rhythmically alternating conglo~-
- erates, Rravelites, sandstones, aleurolites and argillites with interlayers
of coal almost completely compensating for the troughs; clearly expressed
geologically, it is weakly manifested in the modern relief which makes it
- similar to the type of inverted structures. The ~otal thickness of the
Jurassic sediments is 1350 to 1500 meters (Ishina, 1961), and with respect
to geo~~hysical data, 4.5 km (Mikunov, 1965; Dankevich, et al., 1970).
_ By the end of the Middle Jurassic the volcanogenic formation gradually
is replaced by the coal-bearing formation. The conditians of sedimentation
in the Upper Jurassic age were favorable almost everywhere. In Trans-
Bayl;al, the coal-bearing Gusinoozerskaya series was formed in the Upper
Jurassic to Lower Cretaceous 1.2-2 meters thick. At the same time,
conglomerates, sedimentary breccia, gravelites, sandstones with interl.zyers
- of aleur~lites, argillites, carbon-argillaceous shales and coals were
~r.cumulated in the northeast.
'fhe formation of the Mesozoic structures was a direct consequence of the ~
wavy distortion of the earth's surface with the formation of parallel
swells (arches) and subsidence belts between them. The slow wavy bending
(surf~ce Eolding) was initial~ but not decisivp, for the faults and bends
hang on each other and follow one out of the other (Florensov, 1954).
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In the ex~mple o� gevex~l o~ the bael,ne N, A~ ~lorensov C1960~ comprehen-
sively investignted the basi.c atzuctural peculiarieiee and deri,ved some -
generol lnwg of their d~velopment~ In the ma~ority ttie basina are
synclinat b~aement Croughq compensaCed for by thick sedimeneary aeries.
They are not syannetric either in atructural or in facies reapecr~. The
bottoma of the troughe were nlmost flat and level, and the maximum
depresgiona arf eomewhat ehi�ted to one side, The marginal faults are
n~ted along both sides of~the basina. Many of the faults have l~ad an
active influence on the course of aedimentation in the Upper Jurassic to
Lower Cretaceous time. The transverse faults had great significance in
Che poataedimentation period. The overthrusCe occurring in the latesC
stagea of Mesozoic activation possibly occurred from the more ancient
faults. All of these atructural-gPOlogical peculiariries are characteris-
tic of the ma~ority of Trana-Baykal basins.
Basic Abyssal Fractures
The natural boundaries between the regions of the Saam, Karelian, -
, Baykal and Hercinian folding are usually the large zones of abyssal
_ fracturea extending 800 to 1000 km (the ttain Sayan, Stanovoy, and so on)
to 25Q0 km or more (Mongolian-Okhotsk). As a rule, they are accompanied
by thick (to tens of kilometers) zones of tectonically reworl:ed rock,
large and sc~all hasite and hyperbasite intrusions, the centers of volcanic
eruptians, gravitational stepe usually depicting discontinuous variation
in thickness of the earth's cruat and characterizing the great depth of
penetration of them into the de~~ths of the earth. -
- The time of occurrence of deep fractures is determined by the age of the
ge~synclinal systems developing in the adge paxts of the formed platforms
(epiarchean, epibaykal, and so on). Over the extent of all of the subse-
quent ages of tectop,enesis, these linearly extended structural sutures
were the moat mobile and penetrable aectiona ~f the earth's crust. A high
degree of fracturing of the rock and intensive metamorphism of it are
characteristic of them. In addition, the deep fractures are accompanied
by a dense network of contiguous subparallel and f~athering fractures of
different genetic type (faults, strike-slip normal faults, overthrusts,
and so r~n), and also thP depressions next to the fractures in which relicts
of [he Paleozoic and Mesozoic deposits were retained. The genetic variety -
of dislocations with a break in continuity in the abyssal fracture zones
is caused by variability of the tectonic stress fields with time. Accord-
ingly, the ages of predominant developr.?ent of the upthrust faults and over-
thrusts were replaced b}~ ages of fault formation. The role of the shifts
- remains unclear to the present time.
The Stanovoy abyssal fracture extends 800 to 900 km from the Vitim River
in the west to the Dzhu~dzhur ridge in the east. Over the entire extent
it is accompanied by thick zones of various tectonically reworked rock,
large and small intrusions of basite~hyperbasite composition~ depressions
of different age and fields of Cenozoic basalts (Kazmin, 1962). The
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Erncture bounds Ch~ anci~nt nucleue n� the Aldnn ehi~ld from Che snuCh
nnd inr.ludee a seceion betwepn the Chul'm~n ~verthruat, th~ 5Canovoy and
Yuzf~nn-5tnnnvoy nhy~~nl frnrtures in the inveatiRnted t~rrieory. Arcording
tc~ th~r ueorhypicnl dnCn, n zone hne been establiehed h~re with a density
de�icit of no less th~n 0.1 g/cm3 with respect td the encircling aeCtinns
- of the ehield and the Upper Archean fold~d re~inn. It exCendg up tn 10 km
- in depth with a width from 25 to 80 km. This zone can be caueed eiCher by
local dispersion of the Archean complex of the shield as a result of the
granitized rock, granitea, diafluorit~ea or ehickening of the earth's crust
connected with tte bending under the effect of the overthrust of the
Stanovoy region onto the ancient nucleua of the Aldan shield (Uankevich,
et al., 1969, 1970),
The Main (Greater) Sgyan Fracture exCends 1000 l:m from the southern
- extremity of Lake Baykal to the norChwest (300~-310�) almost to Krasnoyarsk.
In the modern denudation section it is a system of fractures with powerful
zones of crushing, ~ointing and m~rlonitization. All of Che rock from rhe
_ Arche~~n to the Paleozoic inclusively were sub~ected to dynamometamorphic
reworking. The basic "trunk" of the fault is accompanied by numerous
subparallel, longitudinal and feaChering fracCures of sublaCitudinal
(270-290�), submeridional and northwestern (330~350�) strikes. The
entire system of fractures from 5-6 to 8 km wide (Smixnov, et al., 1969;
Derzin~ 1967), and in some places uo to 30 1�.m, forms a characteristic
- "horsetail." Small hyperbasite bodies, basic rock dikes and numerous
granitoid intrusions of different age are associated with the fracture
zone.
The occurrence of the fracture belongs to the Late Archean to the be~inning
oE the Proterozoic, and the subsequent shifts were manifested more than
once to the present tim~. The analysis of the structures in the vicinity
of the Main Sayan Fracture and its walls leads some researchers
(Arsent'yev, 1965; Ptusatov, 1964; Berzin, 1967; et al.) to the conclusion
of the participation of horizontal differently directed (along with
vertical) displacemenCs along the fracture. Being the boundary of the
structural-facies zones, as the aeromagnetic research has demonstrated, `
- a fracture separates the differently oriented linear magnetic anomalies.
The magnetic fie3d of the fracture is characterized by a narrow, linearly
- elon~ated zone of sigr.-variable anoroalies and large gradients (?lusatov,
196~). With respect to the gravimetric data, the fracture has an inclina-
tion of the displacer plane to the southwest at an angle.of 55+5�. The
= rooE of the basaltic layer southwest of the fracture occurs at a depth of
14 km, and northeasC, 8 km. Thus, the fracture is interpreted as a fault
_ with an amplitude o� about 6 km ('fonseyenko, 1969).
Pribaykal F'ault
In the western and southwestern Baykal region [pribaykal'ye] the system
of abyssal fractures separatin~ the ancient Siberian platform from the
_ folded structures of the Baykal mountain region framing it on the southeast,
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becumeH pnrt oE tl~e Obrur.hevekiy fnult aygtem. It i~ nisn knnwn under
thc ~~um~ o~ Che l~ribnykn] f~ult (5nlop, 1967) or the t3nykal m~r~innl
euCure (YeRorov~ 1971). it extende 1300 km~ In tiie dpinidn of cert.7ln
resenrcl~ere it b~~nn Co he Eormed in the Archenn (Zamnr~yev, 1961), nnd r
nccnrdinq to other~, in the Lower Proterozoic (Salop, 1h67). The faule
outlines the platform From Sourhern Baykgl to the Patomgkoye Highl~nd gnd
~ predeterminea the orienCation of the geosynclinal eysCem of baykalides
ad~acent to it.
- Tite syatem of faulte of the Baykal marginal auCure obviously is reflected
in the sCructure of the geophys~.cal fields. Tn Che magnetic field it is
obvious with reapect to the linearly sCriated anomaliea. The radio-
active field in Che fracture zones ie high, and the gravitaCional field,
- on the conCrary, ae a rule, is low. The auture boundaries are most clearly
expresaed in the radioactive field by replacement of the level and struc-
ture, and in the magnetic field, in addition, by variation of orientation
of the anomalies (SEISMOTECTONICS..., 1968; Yegorov, 1971).
In western Pribaykal'ye, the presence of a marginal suture is well.
conEirmed by deep seiamic probing. In all the seiemic sections intersect-
ing tlie Baykal basin, crosewise from the Selenga River delta to the head-
waters of the Lena, an abyesal fractur~ hae found reflection which extends
along the weat banlc of the lake. It has a vertical dir and runs below the
Mokhorovich divide. At the intersections of the southwestern side of the
basin, a scarp-like uplift of the mantle aurface in the direction of the
lake witl~ an amplitude of 3 km is noCed (Puzyrev, et al., 1973). -
_ The Dzhidino-Vitim abyssal fracture (structural suture) is extended in the -
northeasterly direction from the boundary with Mongolia in the vicinity of
the upper course of the Dzhida River, along the Uda and Vitim Rivers and
then along the Kalar River. It obviously runs to where it ,joins with the
Yuzhno-Aldan marginal suture. Its total extent in this direction is more
than 1000 km with a width from 5-10 to 50-60 km (Arsent'yev, 1965).
The beginning of the formation of the fracture pertains to the time of
completion of the Baykal foldfng and the beginning of the manifestation of
. the Caledonian folding, that is, it serves as an interface between the two
, regions of appearance of the folding of different a~e. In structural
respects the suture is represented by echelon arranged fractures with which
the breccia zone, the zones of cataclase, mylonitization and cleavage of
rock of different age beginning with the pre-Cambrian are connected.
According to the geophysical data (Arsent'yev, 1965), the fault bounds the
maRnetic and gravitational fields which differ sharply with respect to
nature and intensity.
The Atongolo-Okhotsk abyssal fracture (Gorzhevskiy, Laz'ko, 1961) is a
suture zone from 5-20 to 60-80 km in width extending more than 2000 km
within the boundaries of the Soviet Union (Misnik, et al, I969). The
fault runs fram the border with Mongolia along the Chikoy, Ingoda,
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5htik~ ttiver vnlley~ und then to rhe northea~C to th~ ~har~g of the gen
nf OkhoCgk. Alon~ ~~imngt ehe ~ntire exCent, the fracCurp ig the ittC~rf~ce
I~r.tween tl~e Hcrclninn nnd C~ledoninn folded ~CrucCurep (~ee ~ig 11). Itg
nceurr~ncc b~lon~~ ,~t len~t to the L~re I're-~ambrian. The EnrmaCion~ nE
rhe t,nt~ Pre-Camhrinn nnd Ghe ~nrly Paleozoic in the Mongolo~OkhoCsic
Eruce~re zone are repreqented b,y greenatone, ophiolitic formaeiong
(zdnensh~yn,1967).
The depth of the fracture and thp duration of ies existence are emnhasized
by rhe relaCion to it oE numerous massifs of inCrusive rock of differene
compnsition and nge. The shArply elong~Ced masaif~ of Upper Mesdzoic
gabbro-dioritea And monzonites, Late Lower Cret~ceous granitoids and
Paleogenic bagalts.
According to the data from deep seiamic probing (Iiulin, et al., 1972), the
- fracture zone coincides with the sectiona of the shPrp scarpa in the
surface relief of Konrad and Ptokhorovichich. The amplitude of the scarps
of the Konrad boundary reaches 3 to 6 km.
In conclusion, of course, we must attswer the following question: do the
structural-tectonic elements of Eastern Siberia have any effect on iCs
seismicity, and can the hiatorical-structural analysis be used under our
conditions (Petrushevskiy, 1965) even for the general determination of the
_ seismic potential of the lar.ge structural-tectonic regions?
On the whole, the answer is found to be negative. It is unique but it is
possible when determining the seismic potential of the pre-Cenozoic
structures to use the fact that this is in practice aseismicity of the
greater part of the region of development of the Siberian platform mantle,
but strong shocks often occur here (M to 5.2, K=13). Another eleuient of
the Siberian platform the Aldan shield (a region of pre-Riphean folding,
; see Fig 11) in its different parts has seismic potential almost from
0 to 14=7.9, possibly even more. The same thing can be said of the region
of Baykal foldin�. We are not talking about the rift zone as a specific
neotectonic struc?.,ural element, but other parts of the baykalides, with like
mesocenozoic rejuvenation, uniform with respect to its seismicity: from
.~seismic (Vitim Plateau, part of the Northern Baykal Highlands) to force 9 _
or more (~astern Sayan).
The zone of Caledonian folding over its greater part is almo.~t aseismic,
and only in the region bordering on Mongolia are there individual epicenters
of modern earthquakes, but then to the west, in the territory of Mon~olia,
its activity increases quickly and reaches maximum values (to N=8.7)
although with respect to external manifestations the Cenozoic activation
in tt~e entire zone is essentially light and all the more so in the seismo-
active part it is yuantitatively less expressed thanin certain in practice
aseismic region.
The s~me thing can be said of the region of hercine folding. In the -
extreme northeast (Shilkinsko-Argunskiy Rayon) only rare earthquakes are
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known with M to 4-1/2. Then stretching 650 km to the southweet, only
indivi,dunl epic~nterg of weak eaxehhugkea are known. On the D~urak~~~
Ridge Cher~ ie 7 Elnccid ep~cenetral �3,eLd with enrthquakea of mod~rn
ine~ngiCy (CO fnrce 7, rt to 5^1/4). In the territory o� Mongnli~, the
eeigmic nctivitv of ehi~ region ryuickly increases on moving to the weat,
and the magnitude of th~ earthquakeg reaches 7-3/4 (ttogodakoye earthquake
on 5 January 1967), and with respect to paleoseismogeological data, eo 8.
The sei~mic potential of Che abys~al fractures is not uniform. The various
parte of Obruchev, Mongolo-Okhotsk and other fractures are in practice now
aseism~,c and now they have limiting seiamic potential (earthquakes or
traces of preseiemostatistical earthquakes with Pi to 8.7).
The sCrucCural-tecConic level has no defined effect on the apread of the
tremors. If the level o� high-force (force 8 and higher) isoseisms is
subordinate to the level of seiamogenic atructure, then the subsequent
isoseisma extend noio along and now across or diagonally to the structures
visible on the earth's surface. Previously the existing concept of regular
_ orientation of the isoaeiams in the Sayan (Northwestern) and Baykal (North-
eastern) directiona was not confirmed although for individual earthquakes
the isoseiamal fielda as a whole or individual sections of it turn out to
be extended along the regional structural fields.
The real composition of the geoiogical complexes is felt more definitely
in the spread of the seismic oscillations. The decisive predominance of
the seismically active regions of dense zrystalline rock causes weak damp-
ing of the moderate (~.ess than force 8) seismic tremors which extend to
significantly larger areas by comparison with seismic zones made up of
, thick series of sedimentary or volcanogenic-sedimentary rock (Central Asia,
the Caucasus).
It is natural that under favorable conditions the seismogenic movements are
using the existing weakened sections of the earth's crust independently of
their age, including the transverse and diagonal fracture zones of ancient -
occurrence which are isolated in greater amount in accordance with the
detailing of the geological and especially the geophysical research.
However, it is quite definitely obvious that the seismogenic movements
with respect to the ancient structures take place only as a function of the
modern seismotectonic processes, and the latter are genetically independent
of the ancient structures.
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CEIAPT~R III. BASIC CHARACTCRI5TICS OF TH~ LATEST STRUCTUR~
The Cenozoic tectonic activation in the southern part of Eastern Siberia ~
was preceded by a comparaCively long (Upper Cretaceous to Paleogene)
- tectonic interval during which Che denudation planation surface was formed.
The development of the large laCest structural forms (in parCicnlar, the
- rift Uasins) began with the end of the Paleogene to the beginning of the
Neogene. In the Middle Pliocene, the 3ntenaity of the tectonic movemenCs
increased sharply. However, the increase in rate of movement was not
accompanied by radical rearrangement of the structural plan. Therefore -
for solving the general problema of genesis of the lateat structural forms
it is admissible to consider them as the final reault of the deformation
of the basic (Upper Cretaceous to Paleogenic) planation surface. The
- mapping of this surface presenta known difficulties and it requires special
~eological and geomorphological studies. Unfortunately, these studies were
made in far from all of the areas nf tfie invesCigated territory.
The approximate representation of the modern position of the deformed
initial planation surface in the uplift regions can be given by the
imaginary surface env~loping the mountain peaks. It is possible to construct
this "peak surface" by sufficiently detailed topographic maps considering
the geological materials. In the basins, the basic planation surface is
buried under the Cenozoic deposits. If the precipitates are not thick
(the basins of the Transbaykal type and certain small basins of Pribaykal'ye),
tlie approximate representation of the structure of such depressions can be
given by a smooth sedimentary surface relief. If the thickness of the
deposits is large, then for analysis of the latest structure it is necessary
to use the geophysical materials. The large basins of the rift zone have
be.en most completely investigated by the gravimetric method. The quantita-
[ive inCerpretation of the negative local gravitational anomalies observed
over these basins combined with the electrical prospecting data, seismic ~
prospecting and drilling offers a representation of the relief of the
~ crystalline bed under a powerful series of weakly lithified continental
deposits.l
= 1
A procedure for interPretation of the geophysical data with respect to
hasins, just as the procedure for conatructing the "neak surface" in tite
uplift regions was discusaed in the monograph by Yu. A. Zorin (1971).
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In the s~h~mntic oE the laCesC strucCure cpmpiled Uy ehese methoda
(~~e ~ig 12), isohypaes o� the deformed planat~on eur�ace nre depicted
whlrh oF~er the pns~ib~,liey of c~uanCitntive estimat~,on of the amplitudes
uE the vertl,cal tectonir movrmenCe. The faults that are active ar the
lntepr time ~re depicted in Che dictgram. The faults have greater amplitude,
they are well exhibiCed in the planation aurface acarps. The faults with
small displacements are plotted on the map according eo ehe geological
daCa (ACTIV~ TECTONICS..., 1966; SETSMOTECT~NICS..., 1968). ~
The southern part of Eastern Siberia is divided into ehe following regions
wiCh respect to degree o� manifestarion of the latest movements: the
Sayano-Baykal inteneive mountain formation, the Transbaykal moderate
mountain formation and rh~ Siberian platform (the re~ion of weak mountain
formation).
Sayano-Iiaykal Region of InCenaive Mount~in Formation
In the investigated territory its greater part enters into the Baykal -
' rifC zone extending alniost 200 km from t~e vicinity of the Khubsugul'skaya
and DarkhaCakaya basins in the territory of Mongolia to the vicinity of
the Tokkinakaya basin in Southern Yakutia. Here we are talking about the
re~ion of development of the standard, morphologically well expressed
riEt structurea. Obviously it is necessary to include the high mountain
ridges separating and surrounding the basins in the rift zone. With this -
interpretation, in structural respects it coincides witt~ the greater part
of Che Sayano-Baykal arch uplift isolated by Ye. V. pavlovskiy (1948b).
The average width of the Sayano-Baykal arch uplift is 200 km. The tops
of the ridges entering into it reach 2000 to 2500 meters with respect to
- the most stable internal parts of th~ Siberian platform. The arch uplift
is nonuniform with respect to irs strike. It is divided into three parts
by transverse reduced peak surface: Eastern Sayan (to the lower course of
the Selenga River), Bayl:alo-Barguzin(from the Selenga River to the sub-
meridional section of the Vitim River Valley) and Kodaro-Udokan.
The rift zone borders the Siberian platform only in its ~aidsection (with
respect to strike}. In the southwest of the northeast it is separated
from the platform by the transitional structures the shield type uplifts: -
Prisayanskiy and Baykalo-Patomskiy (Solonenko, V., 1968b).
_ The large rift depressions usually have a length of 150 to 200 km and a
width of 35 to 45 l:m. The Baykal depression extends to 670 km with an
average width of 40 to 55 km (maximum, 70 km). The interbasin commissures
usually are characterized by lower altitudes than the uplifts surrounding
them. Therefore the basins are joined together, forming extended
branching rift valleys. Th~is, the
n_ aykal basin is joined to the Tunkinskaya,
the Upper Angara and the Bargu~ir. basins, an1 the Chara basin is ~oined
with the Muya and the Tokko Basins.
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The gaykal Uasin is di,vided by the diagonal up1~.~C o.f the Academic Ridge
into the southern and nox~thern ba~i,na. Judging by the gravimetric~ `
seiamolog~cal and elecCropxospect~,ng data, Che th~.ckness of the Cenozoic _
- continental deposiCs in the f~,xst basins reaches 7Q00 meters (.rhe vicinity _
of the Selenga River de1Ca), and in the second basin, 4500 meters (the
vicinity of the mouth of Clie Upper Angara). The absolute elevaCions
of rhe crystalline bed in these areas drop to ~6500 and -4000 meters,
resrectively. '
In the other large rifC basins (Tunkinskaya, Bar~uzin, Upper Angara,
Lower Muya and Chara) the thicknesses of Che Cenozoic deposits -
reach 2300 to 2~00 meCers, a~lthe absolute elevations of the basement
surface, drop Co -1500 to -2000 meters. These thicknesses are characteris-
tic of the inCernal basins which with respect to strike are separated by
the saddle commissures in which the thickness of the sediments usually
decreases b�y 2 or 3 times, There are many cases where within the limits
of the saddle commissures the basement rock is denuded on the earth's
- surface (the Tunkinskaya basin). The age of the sediments filling the -
large rif.ts is from the 0ligocene to Che Ho~ocene, inclusively.
The altitudes of the denudation planation surface to the beginning of. the
latest activation obviously can be estimated at 300 to 600 meters. Con-
sequently, ~udging by the modern hypsometry of this surface, the uplift
of the Baykal arch and the subsidence of the basement in the large rift
basins are absolute and not relative. The full scale of the vertical
movements in th~ rift zone will reach 5000 to 6000 meters, and in the
vicinity of Lake Baykal, even 8000 meters.
It~ addition to the above-enumerated basins, quite broad negative structura 1
forms with respect to area with comparatively small thicl:ness of the
Cenozoic,Neogenic and Quaternary sediments are encountered within the
boundaries of the rift zone. These slowly developing structures include
the Bauntovskaya and Tsipikan basins in which the thicknesses o� the
Cenozoic deposits do not exceed several hundreds o� meters. -
Comparatively small ne~ative structural forms are also developed in the _
rift zone: embryonic basins and basins being born (Solonenko, V., 1968b).
The former have a length on the order of several tens of kilometers with
a width to 5 km. The tt~ickness of the precipitates (predo:ninantly
Quaternary) in them is 100-200 m. The basins being born have begun to
be formed at the end of the Pleistocene and in the Holocene. Their length
is less than 10 to 15 km, the width to 0.5 and 1 km, depth from several i
meters to 100. The sedimentation in such basins is in the initial stage
, (Solonenl:o, V., 1968b).
A characteristic feature of the ma3ority of large rifts (basins of the
Baykal type) is unique asyr.unetry of the transverse cross sect~ons: their
~
northwesterly and northern sides are the larger. For the Baykal, Tunki~skaya
~ Barguzin and Chara basins, this characteristic has been established
~ 76
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[see key on p 99] 98
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[ Key Co 'Cabl e 4 ] ;
1. No 10. Tunkinskiy Rgyon
2. DaCe 11. Bsykal'skiy Rayon
~ 3. Time in the center, hours r minuCes 1?. Bsrguzinskiy Rayon
4. M� 13. BaunCovskiy Rayon
5. Coordinates of the epicenter 14. Verkhneangarskiy Rayon
6. Stress 15. Muyakiy Rayon
7. Compressive
8. Tenaile
- 9. Intermediate
- Note. See the note to fiable 3.
o ~ a =
� 2
� ~ y ~ ~
_ p 0
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t O W ~ ~;9
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Figure 14. Orientati.on of the Stress Axes in the Centers of -
Earthquakes o~ the Barguzin District
1-1A epicenters of earthquakes~belonging to groups :Vos 22~31
respectively in Table 3; 11 seismic station; 12 basin region; -
13-14 compressive and tensi.le stresses, respectively, indicated for
e9cli ~roup in t.he example of one of the earthquakes (the length of the
.~rrows is proportional to the cosine of the slope angles of the axes to
tlie horizantal plane).
Key: 1. Barguzin ridge; 2. Alla; 3. Ikatskiy ridge -
99
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It wna noC isolared by seoingical meChods, the flexure was nnt
- expressed even on aerial photographs obviously as a resulC of tt~e large
radius of curvature.
In the Bauntovakiy Diatrict three groups of egrthquakes have been isolated.
One of them belongs Co the westertt part o� the Tsipa~Bnuntovakaya� Basin
_ and ad~acent regions of the uplifts; two stretch toward Che central part
of the basin. The maiority of shocks in the last two groups are afCer~
shocks of the earthquake of 21 July 19h8 (see Table 4) and Che earthqualces
of the swarm occurrin~ in Se�tember-Decemner 1969. In all cases the
orientation of Che compressive sCresa axes epicenCers is cloae to verCical;
the axes of the tensile and intermediate stresses are near horizonCal.
In the sequence of aftershocks, ~ust as in the earChquake awarm of 1969,
shocks of both types isolaCed in Che central part of the basin are~
1 encountered.
In the Verkhneangarskiy [Upper Angara~ DisCr ict the direcLions of
Che stress axes in the centers are defined for 11 groups; of them, the
processinR is carried out for nine by observations only of weak earth-
quakes. In two cases the weak shocks were invesCigated in combination
with stronger earthquakes for which the individual determinations were _
made. The observation data for group No 35 (see Table 3) made it possihle
more precisely to determine the orientation of the axes in the center of
the earthquake on 10 September 1968. The earthquake of 26 November 1968
was included irt. group No 40 (see Table 3). In addition to the two indi-
cated earthquakes, the individual processing was carried out for eight
more shocks (see Table 4). _
In practice, all of the investigated centers of the Verkhneangarskiy Rayon
are characterized by near vertical orientation of the axes of the compres-
sive stresses and the near horizonta]. orienCation of the axes of tensile
and intermediate stresses. For group No 36 alone (see Table 3) inclined
- orientation of the axes of the compressive and tensile stresses was
detected for the earthquake center of 17 June 1968 inclined orientation
of the axes of the compress:Lve and intermediate stresses (see Table 41.
In the Muy a District,the d+3ta on the stresses in the centers were obtained -
for 17 groups of earthquake~s. One of them (No 56, see Table 3) is
ch~racterized by inclined o~~ientation of the axes of the compressive and
tensile stresses and the near horizontal orientation of the axes of
intermediate stresses. In the remaining cases, the axes of the compressive
stresses are near vertical, and the tensile and intermediate, near hori-
zontal. The individual determinations were made for five earthquakes -
(see Table 4). Three of them are similar with respect to nature of center
mecii.~nism to the basic mass of the weak shocks. The centers of the
Muyskiy earthquake of 27 June 1957 atdthe earthquake of 15 January 1963
were cl~aracterized by inclined orientation of the axes of the compressive
.1nd intermediate stresses and the near horizontal, the tensile stresses.
100
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_ In the Udokan DistricG ~ study ia made of 11 groupa of earthquakea,
the r.entere oE seven of them are charACterized by near vertical orieneation
nE Chc nxeA o~ thc~ compreAAive atresaea and the near horizontal orientation
oE the uxea oP the tensile ~nd intermediaCe atresses. In thr. earthquake
cenC~rs of two groups, near horizontal orientation of the axes of the
compressive and tensile streases was detected ancl near vertical for the
' intermediaCe ones. One of these groups is associated wtth the Muyskoy-
Charakaya [Atuya-Chara) inrerbasin commisaure; Che orher centers of the
other are located in the northeastern nart of the region in the fouthills
of the Udokan ridge. One of the groups of enrthquakes of the Chara basin
is characterized by horizcntal orientation of the axes of Che compressive
and intermediate etreases and the v~ertical, the tensile streases. NorCh
of rlaloye Leprindo Lalce, within Che ltmits of Kodar ridg~, there are
= epicenters of a group of earthquakes, in the cenCexa of which the axes of
- the tenaile and intermediate stresses are oriented near horizontal and the
compressive stresses, inclined. ~
From the presented survey of results it follows that the near vertical
oricntation of tl~e axes of the compressive stresses and near horizonCal
orientation of the axea of the tenaile and intermediate sCresses in Che
centers remaina most general for Pribaykal'ye [the Bayical re~ion] even in
cases where the weal:eat recorded shocks in the zone are included in Che
~ investtgation. Out of 73 groups with established orientation of the _
atress axes in the centers, 57 are characterized by near vertical
_ compressive, near horizontal tensile and intermpdiate stresses. The
tensile stresses basically operate approximately across, and the inter-
mediatc ones, parallel to the s trike of the structures.
The conclusions oi the orientation of the stress axes in the centers of -
ttie Baykal earthquakes were drawn within the framework af the theory of
the center mechanism developed by A. V. Vevedenskaya (1969). According to
this theory, the defining role in the occurrence of movement in the center
is played by the maximum tangential (slip) sCresses
Q1-Q3
ak 2 +
operating in the planes mal:ing angles of 45� with the axes of the greatest
(Q1) and least (Q3) principal stresses. Itt the uced force model of the
center of these pIanes are the bissector planes of the axes of compressive -
.hnd tensile stresses of equal magnitude ~the third principal stress,
intermediate, equal to 0). Thus, establishing the orientation on the axes
of the indicated stresses on the basis of observations~of the shift field,
we determine the orientation of the axes of the actual principal stresses
in the center zone of the earthquake~ However, inasmuch as one and the
same max~mum tangential stresses and, consequently, movements can occur
for various values of ol and o3 (if the difference between the latter is
the same) the established urientation of the axes of the principal stresses
can corresnond to different stressed states.
101
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~ If we assume (Treal:ov, 196f3~ V�vedenskaya, 19691 Chat the directions of
the nxes A� Che compreaeive, tensi'le and intexmediaCe stresses in Che
cen~era of the Baykal earthquakes are determined by the directiona of the
stress ar.es o� CI~e least, greaCest ar~d inCermed~.ate tensions in the
correspondinp volumes of the earth~s cruat, reapectively, then the daCa
obtained indicate that the basic regional �ie.ld of the Cectonic stresses
in Pribaykal'ye is characterized in the horizontal and perpendicular
structurea by or~.enCation of Che axes o� greatesC tension, the horizontal
and p~rallel structures by orientation of the axis of intermediaCe tension, -
And the vertical structure by orientaCion of the axis of least tension
(Fig 15 and 16 ) .
The regional diagram of the atress �ield i3 maintained with high sCabiliCy
almost over the entire exCent of the Baykal rift zone, at least from the
southern extremity of Baykal to Che western part of Che Chara basin (see
Fig 15, 16). The local peculiarities of the stressed staCe of the crust
in these regions making an impression on the mechanism c,f the earChquake
centers of individual groups as a rule do not contradict the get~eral
nature of the stresses characteristic of the Baykal region. This uninue-
ness is disturbed only on the flanks of the zone, in the Tunkinskiy and
Udokan Districts.
The overall resulC of Che investigations of the stressed state of the
crust within the limit of the Baykal rift zone is the conclusion of
unconditional predomina::ce in this territory of the stress field of the
rift type under the influence of which the cenCers of the absolute ma~ority
of r_arthquakes, both strong and weak, are formed.
,
102
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103
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[Legend and key for Fig 15, p:L03]
1,3,5 near horizontal, incl.ined and near vertical stress axes in Che =
earCl~quake cenCers investigated individually, respectively; 2,4,6 tlte -
same for earthquakes combined into groups; 7-- outLines of Ch~~ re~ions -
- encompassing the earthquake epicenters witll a single cenCer mechanism
(orientation of the stress axes is shown in the examnle of one of the
earthquakes. The total number of them within the limits of the region -
is designated near the outline or inside it). I~VI ~ regions of the
Baykal seismic zone; I~- Tunkinskiy Rayon [DisCrict;,Il Baykal~skiy, -
III Barguzin, IV Verkhneangarskiy, V-- Bauntovskiy,
VI Muyskiy [Ptuya], VII Udokan.
Key: -
1. Kitoyskiye bald neaks; 2. Tunkinskiye bald peaks; 3. Khamar-Daban
ridge; 4. Irkut; 5. Irkutsk; 6. Angara; Primorskiy ridge;
8. Baykal ridge; 9. Lake Baykal; 10. Barguzin; 11. Barguzin ridge;
12. Ikatskiy ridge; 13. Ver.khne-An~arskiy [Upper Angara] ridge;
J.4. Verkh. Angsra (Upper Angara] River; 15. Delyun-Uranskiy ridge;
16. Muya; 17. Yuzhno-Muyskiy (Southern ?~Iuya] ridge; 18. Vitim ;
19. Udokan ridge; 20. Kalar; 21. Tsipa; 22. Vitim ; 23. Ulan-Ude
104 `
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CHApT~it VI. ~1ERc,`Y CLAS5I~ICATIOh OF' EARTHQUAK~S
At the preeent time in Pribaykal'ye, juat in the majority of s~ismically -
~Ct~Vp regiona of the USSR, the energy elassification of Qarthquak~s i~
rarried out by th~ proc~dur~ developed by T. G. Rautian (M~TNODS...,
1960). The nomogram constructed by thi~ authc,: with re~pect tn the
nbservation data at the sei~mic statione of C~niral Asia naturally tak~g
into account the dissipating properties of the substrate of the giv~n .
region. When applying this nomogram for the classification of the -
Pribaykal'ye earthquakea, it ie neceseary to b~ certain of the correctnesa
of iC~ us~ in an are~ vith entirely different geological structure. ~or
thia purpose~ f iret of all it ie necewsary to compare the damping laas of
the elastic oacillations aith an increase in the epicentral distgnce in
the corresponding regions.
Damping Law of Seismic Wave~ in Pribaykal'ye
An estimate of the parametera of the damping law vas made by us using
several procedurea. Firat of all, this is the procedure fnr constructing
a free graph developed by'T. G. Rautian and the so-called difference
- proced~re (Gayskiy, Zhalkovskiy, 1971). Along aith them, the procedure
~ras also used which takea iato account the dependence of the energy Eg
defined by the formula of'B. B. Golitsin (1960) on the epicentral distance
(Solonenko~ A., Tatarenko, 1972a~. Experimental data are presented in
Fig 17 for the T. G. Rautiaa procedure.
Fig 18 shos+e the distribution N(n+~egf) for the diffexence procedure
vhich gave the main value of the index of the damping function of the
maximum amplit~ades of the soif displacements (for epicentral distanceR
exceeding 300 km) equal to 1.99+0.07. Calculating n~eff for the energy
flux denaity e in the eame distance range by the formula
lg Am (mk) ~ 0.49 lg e(ergs/cm2) - 0.12 (1)
relating e aad AH (Solonenko, A.~ Tatareni:o, 1972a), ae obtain n*eff~4�06.
106
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T'his valu~ of ~?*eff ~grpe~ huite w~11 (withl~ the limitg of error) with
the v~~ue c~f the index of the damping funetion abtained from the summary
gr~ph (~~p Fig 19). Th~ figure slgo preeenCs the curv~ obtdin~d u~ing the
funCti~n Er~ (A). The comparison of the results obtain~d by Ch~ ehr~e =
procedures ia good, WhiCh permit~ ug to draw thp certaSn c~n~lugidn eh~t ~
che data~ing inw of the energy flux d~ne~ity iB charact~riz~d for
pribaykal'ye by the folidwing aver3ge parem~ters: ~
fo xuCe~ 70 Ku, ni ~4,2:
i0 toti N
w ww
134
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FOR Ot~FICIAi. USE ONi.Y
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riEure 32. Schematic of the northeastern flank of the
Yanchukanelc~yg etructure. Compiled by
- R. A. Kuruahin
1-- alluvial deposita of the continental delta of the
Yenchukan P.iver; 2-- heterogeneous clastic accumulations of
the rubble drain at the foot of the mountain; 3-- upper
Qua[ernary terminal moraine formation; 4-- mountainous
(altitude more than 2000 meters) border of the Verkhneangarskaya
basin made up of granitoids of the Barguzinskiy complex;
5-- debris cones of the temporary streams; 6-- facea of
the divide capes; 7-- divide lines (a) and thalvegs of the
temporary streac~s (b). Seismic dislocations: 8-- faults
and their ~anplitudes (h, m); 9-- tensile cracks and magnitude
of their gaping (s, m); 10 morphologically weakly
expressed sectione of the dislocations.
Key:
1. Yanchukan
136
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Pigure 32. Tenaile fracture cutting the nwbile large-,block '
~ placer granites on a 21� slope.
Photograph by R. A. Kurushin.
137
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138
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~OR O~~ICIAt. U5~ UNI,Y
~ -
'Chr. mddrrn ~ei~mic nc~tlvley of tt~~ ~tructurp ie appr~~i~b1y inw~r th~n
ehnr obe~rved in th~ ad~~c~nt region ~i~ng ehe Severomuyakiy lin~~m~nC.
t1elE of the earChquait~ ~pi~~nC~r~ ~tr~~~hing toward thp ~eructure pt~9)
_ aich ~qu~i probabiliCy ean b~ conn~at~d ~i~n aith th~ ~eeir~iey of th~
l~tter. ~ormally, 29 ~Qrthquak~ ~picpnt~r~ bplong to thi~ gtructur~.
A/3-4. Th~ Kovoktin~kaya [Kovokta~ ~truGtur~ (~ee ~ig 34) ig locat~d in
_ the h~~dqu~rt~rg of eh~ Yanchuk~n gnd Kovokta itiv~re, ~i~ng eh~
~nutheaet~rn ,~id~ of eh~ ba~in With th~ sa~e nam~. The genprai directian
nf th~ di~locarions of rhe atructure i~ northeast 60�, and the total
~xtent is 28 km.
Th~ predominant morphc~logical type of a~iami~ di~locatio~ of th~
Kovaktg etructure i~ the tension ~ointig (.eectonic trench~g). Signific~nt
eegment~ of th~ etructure ~re rppr~~ent~d excluaiv~ly by th~ae dieturbanc~g.
Their trangition elong th~ strikp to th~ faults i.~ ob~erved more rarely.
In the laee caee the limb at the foot of th~ mounta~tn (northwpstern or
narthern) eubeid~d.
The ~ectonic cr~nche~, ge g rule, have V-type transver~~ profile and
- depth and magnitude of gaping varying signific~ntly aloeg the strike.
'Che m.~ximum morphometric indexes of the faults are ordinary at the paint$
oE intersection nf the sp~rse positive forms ~f the relief the crusts
nf the side moraineg, the divide capes. The Width of thp separation 3oints
then reaches 10 to 15 meterg, and the depth, 5 to 6 meters. Often in
auch gections the te~ton~c trenches are complicated by seiamogravitation~l
landslideg up to 3S-40 meters long and 10 to 15 metera Wide.
~aults are observed over a short extent and neceasarily in combination
with tension jointa. The maximum amplitudes of the vertical displacement
of the limbs (S to 7 meters) do not d~pend on the relief intersected by
the fault, but the quickly damp With respect to strike.
In the southWeatern part of the atructure, in the vicinity of the divide
of the Yanchuy and Yanchukan Rivers, the mass development of the seismn- -
gravitational alope proceases is noted. In the vicinit~ of the highland
limb of the etructure over an area of no more than 2 km there are four
concentrated large (approximately 0.25 to 0.5 million m3 in volucae) rock
glides and a large number of small talus piles. The slides have well-
expressed eeparation amphitheaters which cut the divide capes or the
slopes of the divides and penetrate farther do~m the thalWegs of the
slide cone ravines. The planes of the displacers of the landslips are
associated aith the numerous subparallel faults making up the tectonic
zone of the Yanchuy-Yanchukanskaya echelon structure.
The age of the structure is estimated at a feW hundreds of years aith
respcct to the degree of preservation of the fractures and the presence
in them of macure arboreal vegetation. The magnitude of the earthquake
accompanying its formation, ~udging by the dislocation scales, cannot be
less th~n 1-1/2 to 8(force 10-,11).
139
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141
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l-
'Ch~ gei~mic ~ctivity n� the Kov~ke~ gtructur~ ge th~ pr~~~nC tim~ i~
~dnfirmed by 12 e~i~entcr~ af we~lt esrthqualte~. di them, three epicenteirs
with K*~10 ar~ ~roup~d in rhe norrh~gse~rn p~rt of th~ Kdvdkt~ b~~in. On
the whnl~ the mod~rn activiey of Che viCiniCy of eh~ ~tru~tur~ i~
~i~nificantly inferior to the ~d~~c~nt re~ion~ of the V~rkhnegngarsko-
Muygkayg interbs~in commi~~ur~.
A/3-S. Th~ Muyakansknya etru~ture was det~~ted by the a~rigl photngrgphs.
A ground etudy of iC wga not mad~. `~he structur~ ig genetically conn~ctpd
With the zone nf th~ large neoCectonic fault bounding the rtuyakansknya
ba~in from the south~ast. The syatem of dislocationa followe alon~ the =
foot of th~ Muygkanskiy ridge in the we~tern hglf of the b~gin in Che
north~aaterly (65�) dir~rtion. It ie obvioug ge a di~ranc~ of 26 km.
The dislocations defnrm the proluvi~l d~pogits c~f the debrie cone~, the
slide rock cover of the slope and mnre pnggibly, thp basir gr~niee autcropg
of the Barguzinekiy complex. The fractureg with verCical digplaCem~nt
are c]enrly isolated among Chem, th~ maximum ampli~ud~ af which r~gchps _
6 meters according to the ~tereophotogrammetric meagurpmente. Thick mud
fiows, the aeismogenic nature of which is entirely probable, are asaociated
- with the northeastern flank of the atructure.
A/4-1. The Taksimakaya atructure (Fig 35) is located in the western part
of the Muya basin on the left bank of the Huya River~ to the north and
th~ northeast of the village of Taksimo~ The general strike of the -
- gtructure is northeasterly (60�); it extends about 15 km. 'Ch~ atructure
kas detected during chamber deciphering of the serial photographs in 1965.
- Tiie aerovisual (V. P. Solonenko, S. D. Khil'ko, A. P. Shmotov) and ground
(5. D. Khil'ko and S. V. Lastochkin) investigations were performed in 1967.
The Taksimo structure occurred in the zone of contrast tectonic articula-
tion of the bottom of the Muya basin and its northwestern mountain border.
Southeast of the structure there is a broad flat swampy floodplain of the
Muya River with a set of oxbow lakes and streams. On the right side the
river valley has cut into th~ lower to middle Quaternary sandy seri,es -
making up the basin, and on the other side, it is recumbent on the steep
high slopc of the small ridge the Adyanskaya ridge. Thig ridge extends _
in a northeasterly direction from the mouth section of the Kelyan River
20 km With a Width of 4-5 km, and it is separated from the northern Muya
(SeveromuysiyJ arch-block uplift by an erosion-cectonic through vall~y of
the Adyan-Kelyanskiy and Adyan-Paramskiy creeks.
At the southWest end of the ridge (the left bank of the Kelyana and
ltuya Rivers) there is the well-knoWn Kelyana massif of ultrabasic rock
- (predominantly srrpentinites and listveaites). The massif is extended in
che southwesterly direction orthogonal to the neotectonic structures of
the region; it is no more than 2.5 km wide. Then to the northeast along
" t he strike of the ridge, the serpentinites are contiguous along the
tectonic compact with the sedimentary series of the upper Proterozoic:
metnmorphosed sandstones, aleurolites. shales crumpled into linear folds
142
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nf r~nrthw~~t~r1y (1~0�340�) ~erik~~ Af~er 2-~ km th~ ~~dir~enenry ra~k
' ia rrptnced by ~ ehir.k ~~ri~~ of 1~y~r~d 1ime~ton~~ gnil doidmite~ nf th~
- l~n~ki ~e~g~ ~f ehe low~r Gembri~n (eh~ir ~trik~ fg 3~0�335�~ th~ angle~
- df incid~ne~ ~re SO-~i0�)~ `Che carbonate rocke ar~ tr~e~d ~1an~ ee eh~
- Al~k~n Cr~ek. Ae th~ b~~e of th~ ~outh~~~t~rn ~lep~e df ~hp ridg~ ~b~v~
th~ er~~k elong eh~ rtuy~ Riv~r ~rnnitoid~ di th~ Muy~ rnmpl~x w~rp
d~t~ct~d. ~h~ t~~eonir contant of carbon~c~ou~ form~tiong WiCh Arr-h~en
gr~nite-~n~iss ~~ri~~ e~umpled into compiex ieoc11n~1 foldg ~f nor~h~
~~sterly (40-50�) strik~ rung ~long th~ A~akan Cr~~k~
'The ~rti~ulation of th~ ba9in and eh~ Ady~ngkgya ridg~ i~ ghnrply
~xpr~~~ed, rectilln~~r and emphas~z~d by eh~ triangular ~ee~p ~30-.40�)
cut~ of the divide c~p~e located 8lmoet in on~ plan~. 7'h~ ~an~ nf
grti~ul~tion is covQred by ca~reply cl~~tic rn~kgiid~ gnd proluvi~l
deposit~ forming a narrou (0.3~i.2 km) bou~der tr~in gt the fdoe of gh~
mcuntain to 80-9~ meters~
The di~incations of the Taksimo structur~ arng~ ~g ~ r~g~1t of thp
s~i~m~g~nic opening of the pow~rful n~oteetonic fgult bounding ehp
Muya-Kond~ basin on ~h~ nbrth~test and north the 1e~gt bread and deep
of th~ two negative morphoetructures meking up thp :tuya ba~in. '~hp b~~~-
ment of thp begin on the southeagtern limb of th~ fau~t ~ubsided to a
depth of more than a kilometer (2orin~ 1971), at the sam~ timp as thp
elevation of the northwestern limb, judging by the el~vgtion~ of the divid~
line of the Adyanakaya ridge i9 1400 to 1500 merere. Thus, the di~per~ion
of th~ blocks of the lithosphere along the fault bounding th~ Muya-Konda
b~sin in thia area ~xeepds 2000 metprs congidering th~ fl~xur~ comp~n~nt
and the eroaion cue. The analogous ~mplitudes of the vertical movem~ntg
during Neogenic-Quarternary time are characteristic alsn for the sub-
latitudinal segment of this fault eagt of the structure ahere it controls
the intrabasin longitudinal commtssure.
~ The fault zone in the vicinity of the Tak~imo structurp is m~de up of
thre~ gubparallel echelon fractures. The southWegtern echelon formation
fc~llow$ ~long the Muya alope of th~ Adyangkiy blork ~t ~n ~~iselute el~va-
tion o� 800-900 meters approximat~ly from the mouth of the Ke~yana River
tn the central part of the ~tructure. In relief it is clearly ~xpre~sed
by gharp inflections of the slope and deep ~addle~ dissecting the divide
ridges of the left tributaries of the Muya River along a atraight line.
The latter fact indirectly indicates the subvertic~l position of the plane
oC the fracture displacer. Its extent i8 about 10 km, and the general
strike ia northeasterly (65�). The second, central echelon structur~ is
generated 3 to 3.5 km northeast of the beginning of the first, it folloas
nlong the articulation zone of the ba$in and the mountain border to the
Alnkan Creek under the loose depoaits of the boulder train at the foot
nf the mountain. It i~ oriented Along the 60� azimuth. The angle of
S� determines the gradual approach of the upper and lo~+er eehelon
gtructures in the northeasterly direction from 1 to 0.5 km. From che
location of maximum convergence (approximately at the center of the
etructure) to che northeest there ia only one neotectonic Eracture ahich
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t~ ~ C~ntinu~~i~n of dn~ af ~h~ ~~h~lon ~~rueturpr~. tf wp tak~ it ~g ~
continu~~i~n ~f ~he lau~r e~h~ldn g~ru~tur~, th~n ~he e~t~l ~.engeh ~f ~11~
~ra~eur~ ig abnut 13 km~ ~inally, the nnrEh~a~te~l~+, hypgometri~all~+
it)Np~t ~~he1~n ~t~u~tur~, eh~ ~rp~e~r p~r~ ~hich i~ ~oc~~~d be~+nnd
th~ limit~ ~f eh~ gygf~m ~xt~nd~ p~r~il~i Ed th~ e~ner~1 dn~ ~n eh~ l~~t
bdnk di th@ Muy~ ~iver, ndrthea~t af th~ Ai~k~n ~r~~k. ~t i~ p~g~ibl~
th~t it~ ea?~ehwegt~rn ~i~nk i~ ~dv~r~d und~r th~ ~11uvi~1 depo~it~ ~f ~he
river fl~ddpl~in.
'Ch~ m~in aygt~m d~ ~Qiem~g~nic di~locatinn~ di the ~tru~ture fdllc~a~ eh~
~~ntr~l ~chplon ~trureur~ di the n~dtc~c~oni~ fgule. Suppo~~dly, eh~ gduth-
Wp~tprn f1~nk of the upp~r ~~h~lon ~Erueturp ~xpprienehd ~~~iv~ dfi~fl~fl~~
~nd it~ r~mmainin$ p~rt, pa~giv~. prab~bly, e.h~ ~orfh~~ge~rly, i~w~r
fr~eture u~g not touch~d ac ~11 by th~ rpepnC g~i~mdg~nie re3uvengti~n. -
On ehe s~uthW~~t ~nd of the Ady~ngk~~+~ rid~e the di~ld~aei~ns ~re di~ein~
gui~hed by th~ re~ult~ of the dpc~ph~ring of th~ a~ri~l photagrgphg. `~hpir
Edrmntion can b~ ~onn~ceed ~ith p~r~ia1 r~~uv~na~ion o� thp upper echel~n _
grrueture ~f the n~ot~ctonie fracture ~nd eubgpqu~nt tran~ftion c~f the
digidc~tion gygt~m from the upppr echel~n gtrurtur~ t~ th~ iot~er (or vie~
v~rg~). ~n thp ~lop~ of the ridg~ turn~d tnward th~ K~lyan~ Itiv~r, th~
Eault ~ucg and ghifts ~ tQrrac~-lik~ b~nch borderin~ th~ ~lop~ at an
~l~vation of appr~ximgt~ly 350 mee~rs above th~ riv~r flondplain (8S0 m
abeolut~ el~vation). Thp bench is up to 200 meters wide, the gldpe ~n~l~
is 6 tc~ 10� and it is traced in fr~~mentg boeh alang th~ northWest~rn
and th~ south~~~t~rn slopeg of the Ady~n~k~ya ridg~. An an~ld~au~ ~earp
at this ~lcitude ig ob~erved ~1ong th~ periphery of the Muy~ b~gin and,
most probably, is a lacuetrine sc~lptured terrace. On the dcnmthroWn limb
oE th+~ fault, che amplitude of Which is no less than 40 meterg, th~
terrace is not expressed in relief, merging aith the divide of the mount~in
spur dipping deeply into th~ basin. An obvious fragment of it ~pp~ar~ on
onp of th~ divide capes 2 km northeagt and ngain on th~ highl~nd limb c~f
the strueture. From the divide of the mountain gpur made up nf s~rp~ntinites
the disloc~tiona (nbviougly fgult~) inclined slightly to the Qase, are
unrlearly traced downward t~ the foot of che ~outheast~rn alope of the
Adyansk~ya ridge Wher~ th~y are in contact With the main di~loc~tion gyst~m
oE the Taksimo structure.
'the main disldcation system extends on che Whole re~tilinearly along th~
fooe of the slope gt an absolute elevation of 540 to 6~10 m. The diglnra-
tions nre represent~d by a spt of faulcs and th~ tension ~ointa accompany-
tng them (tectonic tre~rh~~). They mase fr~qu~ntly deform the 1oos2
boulder Erom block accumulations of the boulder train at the foot of ch~
mouncain. but thcy are also noced in the carbonaceous and igneous bagement
rock. All of the dislocations, independently of their morphological type,
nre nricneed in th~ northrasterly direction. The largest number of
mensur~ments indicate a gtrike azimuth of 60 to 70�.
144
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145 -
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- 'Th~ amplitude of the faults measured by the diaplacement of ehe peak parts
- of the debria cones flucCuatea from 1~3 to 2~. m. At the base of the -
fault ecarp or on Che subeided limb of tihe fault parallel to it ehere are
one or ~ev~ral Cecton~c Crenchea of eriangular or trapezoidal crose
g~ction (Fig 36). The ~oidCh of the trenchea at the eop ia from a few
m~eera Co 20 metera, moat frequenCly 4 to a meters, and rhe depeh ia -
from fracCione of a meter to 10 meters, predominantly 3 to 6 meters. The
wnlls of Che trenchea are broken, steep to vertical. In the loose proluvial
material, their ateepneas reaches 60�. Frequenrly the part of the trench -
aC the �oot of the mountain rurns out to be more steeply sloping than Che
oppdaiCe side.
UfCen in the boulder Crain at the foot of Che mountain along the base -
of the slnpp a dislocation zone is observed which is made up of 2 to 4
subparallel tectonic trenches and sharp peaked and ~rapezoidal ridges
aeparating them. The difference in alCitude of the oppoaite walls of Che
trenches indicates that in this case there is a system of stepped faults -
- and tension ~nints accompanying them with a total araplitude of the vertical
- di~placement to 6 to 7 meters. Along the strikes some of the dislocations
quickly c~amp and reoccur; others continue Co a more significant distanc~,
but on the whole Che structyral dislocations are traced over the entire -
extent of the cenCral echelon structure of the neoCectonic fracture,
- discontinuing only at the points of their inCersection by the channels of
streams.
M ~~:t,~ ~h,~~~.. ~-~;v ~ ~^3 ~y.i ry r ya L -
~Yl~/."t~ ' ~ 4' I y .
J .4 ' , , t ~ h~~ .
a
rr~.I �V ~ "f '
, '
~,1 . ~ ~ k
r~r :
.c ; ~'~;a
< < i t~
N A93~
f
~t~t ~.Y.:
A: r. r~li,. J
r~ . r~'15, ~t,(~
~
' i~~ J .
.~{,:��r
~ y~., y V .y .
q' ~.li.,t
~~r~a~yi.~~l:? ~~l j -
~ ~~~rt w'i`_ k~" ~ ~ ~ .
. ~4;
t
. y
Figure 36. System of tectonic trenches (tension ~oints~
cutting the deposits in the vicinity of the boulder
train at the foot of the mountain in the central
part of the Taksimo structure. Photograph by
S. V. Lastochkin. -
146
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~Ot~ O~~IGtAi, U5~ t~N1.Y
In the rentt'r~T pnrt o� the ~tru~turp between thp two echeldna di the
E~ult in the vicinity of their ronximum apprnach, there are two chara~teri~-
tic rnck~lides. They nr~ ln~nted in Che low~r Combrign limegtnn~g dipping
6b� n~~rthen~e nt en nngle of 50�~ and rh~y er~! mar{,~ un af ste~~ (~y")
CrtnnF;ulnr f~r.eH ~f nd,~ncene divid~ c~pea. 'Ch~ ~.~rbo~~~~eou~ ~eriee
~uppd~poly occurg in the ign~ous rock of th~ ttuy~ c~mpl~;; out~rdpring dt
_ ehe surfac~ at the ba~e of the e1op~. The Arc-~f~gped g~paration i~dg~~ ef
the l~nd~lide~ gre loc~ted at an altitude of 200-25b meterg from th~ foot
of the root slnp~ of the Ady~ngkayg ridge. In rhe n~ar v~rticgi wa11~
of thp separatidn, no lese th~n 3~ m~ter~ high ~t th~ ~outhu~~t~rn lgnd-
~lide and 6 to 10 metera high at rhe norChe~gt, g rock a~~ep r_over th
2 to 3 meCers thick end light grny limegtone~ in Che rnoC ~ccurrenr.~ are
detacted. In th~ lime~ton~~ at the t~aep of the wall, g erench is trgeed
(sedimentation ,~oint) to 5 metere deep up to 15 mpterg wid~ in th~ upper
p~rr up to 3 meter~ at the bottom ig trac~d. The northeastern flankB of
th~ lnndalide cirques oucline in gently aloping ~rcg the body of th~ land-
glide block, descending Co the foot of the ~lnpe. They a1~o are ~xpre~eed
by the eeperation walle up tn 10 meters high (in thp areeper lendelide).
On the southwest aide the landalide blocks ere bounded by the V-shap~d
valleyg of ama11 temporary streams. The landelid~ area ig approximately ~
- 0.3 and 0.1 km2. the volume of the landglide masges i~ unknown, for Che
position of the slip surfaces has not been determined.
The morphology of the largeat landalide block and ite relation to the
undisturbed parts of the elope indicate the detruaive nature of the land-
- slide displacement. The maximum displacement which is more of a fa~lted
nature than landslid~, was experienced by the upper part of the landslide
block along the s~paration plane coinciding aith tl~e displacer of the upper
echelon structure of the neotectonic fault. Th~ frontal pare of thp land-
slide cut by the central echelon of this fault apparently does not have a
horizontal component of tnotion. As a result, deformation of the surface
of the landslide maes took place: in its rear section, a broad, flat
trough was forrt~ed, and the part above the frontal section acquired a
convex surface (Fig 37).
~rom the two exogravitational phenomena accompanying the formation of the
Taksimo structure it is necessary to note the mass rock talus located
primnrily on the mountain limb of the upper echelon atructure in the
vicinity of its approach to the central structure. The talus makes up the
morpl~ology of both the northeaetern and southaestern slopes o~ the mountain
r.~vines cutting the Muya slope of the Adyanskaya ridge. The area of the
l.~ry,est of them reachea 0.1 km2.
7'hc process of the formation of the Taksimo structure, a~ it appears to us,
Freatly resembleA the *tuya earthquake of 1957. The relief of the stresses
(the initial epicenter of the paleoearthquake) began with the southvestern
flnnk of the structure where [he intersection node of the rift controlling
, f~~~lt with the transsverse Kilyan~kiy deep suture is located. tn practice,
the instnntaneous opening of the fracture occurred in the northeastern
direction, initially along the upper fracture~ and then through the system
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cfi "trnnaitihnr~t" uninherited di.~lnci~tionq, encnmpa~g the rentrr~l ~chelnn
aC che frn~curc. At thc~ gam~ time, nnt dnly th~ ad.~ac~nt reginn dE the
Muyn-Kondn bd~in wa~ involv~d in thp f~ult~d sub~id~ne~, but ai~~ th~
~rogion=t~ectonir rommiq~ur,~ gepar~ting th~ Muye ba~in Erem th~ U1~n-
ttakit~key~ bagin. Simil~r di~a~treug mnvempnt~ of the ~arth'g cru~t
oecurr~d hpr~ durin~ the Haic~eene, dbvidugly more rhan once. in rgreicu-
l~r, thig is indi~aepd by the gr~du~1 migr~tinn nf Che Muy~~ ltiv~r chgnnel
in th~ dir~ction from the center of th~ ba~in td the eouthe~gtern glnpp
, of th~ Adygnakay~ ridge. The 'Cak~imn ~tructure ig ~ elpar ~;;~mpl~ of th~
' ~ontinuing proc~~~ nf de~penin~ of the ~ayk~l typ~ b~ein~ ~nd their longi-
_ tudinai growrh.
~r C3 (1) e~'.'y ! 2 ~ .J
~00
+ ~ ~~`y,j d ~ , ,.r! S
J00~ ~
r .i, ~d ~J,
~ ~4 ~
4~I~'~ ~1,J ~ 'ti
i ~
~
~1 f f ' ,
+ { ~'.~~.I.~~. .
( t + t tF~ _'e � ~ � .
~r' ~ Tr_
0 P00 ~00 ~ 6GC B00 M
Figure 37. Geological-geomorphological section through the
axial part of the seismogravitational rockalide
on the southeaet slope of the Adyanskaya ridge.
Compiled by R. A. Kuruehin
1-- loose deposits of the boulder train at the foot of the
mountain; 2-- igneous rock of the Muya complex; 3--- limestones
and dolomites of the Lenskiy stage; 4-- fracture zone
echelon structure of the neotectonic fracture; 5-- landslide
block and the propoaed position of the slip surface of the
- landslide; 6-- surface profile of the elope before formation
oE the landslide; 7-- seismotectonic dislocations oE the
Takaimo atructure.
Key:
1. northaeat; 2. southeast
'Che time of formation of the structure is approximately determined at
- 150 to 250 years with respect to degree of preservation of the seismic
dislocations and age of the arboreal vegetation growing in the tension
,~oints (pines. larch). The magnitude (~t) of the earthquake was in this
case approximately 7 to 7-1/2 (no leas than force 10).
The modern seismic activity of the Taksimo structure, just as the other
pnleaseismogenic atructures of the Nuya bagin is low. In the 10-year
148
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p~rind nf ehp im~trum~ne ob~~rveeiang h~r~ three ~pieenterg of repr~s~ne~-
- tive enrthqugkeg w~r~ noeed. Almoet eh~ entire zone of th~ neotectonic
fault bounding the t4uyn~Konda b~sin nn the northWe$e gnd north ~lao i~
~omp~r~tiv~ly e~eiemte~ ~aly to the east of the appar~nt dnmpiag of the
~ene, in chp mouth parC of Che M~~~a River appraximately 20 Qarthquakes of
diff~r~nt energy levels~ including the Ust'-Nuya earthquake of 1968
(tt~5-1/2) were recorded primari~y in 19b4 ~nd 1968.
A/4-2. The.Para~mskaya etructure (Fig 38) extending 21 km is located in -
rh~ artieuletion zon~ of the Muya baein (the Paramskaya depre~eion) and .
the arch-block uplift of the 5evero-,ttuyskiy [Northern Muyg] ridge beeween
the S~mokut and Kamennyy Creeks.
The atructure w~s studied in fragmenCs and with a different degree of
det~il. ita eeparate elements were dptecCed and documented by L. i. Salop
at the beginning of th~ 1950's and Ye. A. 2elenskiy, et gl., in 1966.
Accnrding to Che data of Che indicated researchers, the observations of
covorkerg n� the IZK Inetitute of the Siberian bepartment of the USSit
Ac~demy of Sciences S. V. Lestochkin and the results of the etereophoto-
grammetric nrocessing of the aerial photographs, a scheiuatic of this
structure (see Fig 38) has been conatructed.
The northern eide of the Paramskaya [Paramaj depreasion is made up of
thicl: deluvial-proluvial accumulations over almost the entire extent
merging into a solid train of rock waste at the foot of the mountain from
0.~ to 3 km in aidth. Numerous debris cones of small temporary and large
~ermanent streama running off the SE~:ero-Muyskiy [Northern Nuya] ridge '
are clearly diatinguished on its aurface. At the center of the depression,
from under the c~oarsely clastic formations of the boulder erain at the
foot of the mountain, sandy Lower to Middle Quarternary sediments appear,
the thick series of which obviously make uo a significant part of the
Muya basin. The set of floodplain and terrace deposits of the Vitim and
Parama Rivera cu~t in[o the sandy series. Some large streams (Samokut,
Bulunda, Kemennyy) also are accompanied by terraces up to 25 meters high
in the lower aecitions of their mountain valleys. -
The narthern mountain border of the depreasian is made up of nre-Cambrian
sedimentary-volc~inogenic beds of the Muya series, breached by the massive
or gneisa-like b:[otype granites of the Muya complex. The complexly
dislocated eedimi~ntary series have northeasterly (40-60�) or submeridional
strike. According to the observations of L. I. Salop (1964), when the
Samokut Creek leiives the tnountains, the sedimentary-volcanogenic formations
of the Muys seri~as are separated by a zone of cataclasites of sublatitudinal
strike 4~ to 5~ cneters wide from migmatized amphibole gneisses of the
Archean detected a[ the base of the socle terrace of the stream and
aupposedly makin~; up the basement of the depressions. In the Vitim part
of the north sid~~, numerous dis[inctive dislocations of ancient occurrence
have developed wl~ich make up ttse Parame zone of the deep fracture of
north-northvestexly atrike. The introduction of the Parama massif of ultra-
basic rock (serpentinites) occurred along it in the pre-Cambrian.
149
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_
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'~h~ ~ar~mg ~tru~ture aros~ ~a ~ r~gu1C of th~ Holnc~n~ re~uv~natidn of
th~ powerful, 1on~-1Sved ~ublatitudin~l fr~ceur~ which aepgr~C~d Chp two
tectonic structur~g with different dir~ctional movemenC in Che C~nozoic
th~ S~vero-Muy~koyh ~Northern t4uya~ uplift and the Muya baein. In
Cl~p Nrc~~enic-f~uat~rnnry time the amplitude of the vertical dieplacemene of
the blocka of the ~arth'e crueC alon~ it reached 1500 meter~.
The aeiemogenic dislocatidne of Che strucCure ar~ represpne~d by f~ls~ and
t~ngion ~oints (tectonic Crenches). 'I'he latter, ae a rule~ accompany
th~ frgcturee with vertic~l diaplacement or occur independently. Whereag
on th~ Whole the system of eeismog~nic dislocaCiona is ~longgt~d in thp
aublatitudingl (with slight slope to the northwest~ direction, Che
individual fractures or segmentg are oriented differently. The north~
easterly (60-80�) and sublatitudinal (80-100�~ etrikes are most frequently
observed, and northweaterly (290~310�)~ more rarely. The greater parC
oE the dislocations are asaociated with the contact of the looae Quaternary
deposita and the rocks of the ateeo ~lope of the ridge. However, deforma-
tion of the Quaternary formations of the most different age is often
observed. Thus, in the weetern part of the structure, the faulta, except
the terracea of the Samokut Creek, cut and ahifr the terraces of the
Bulunda Creek and its large left tributary (3 l:m to the east) of different
r~ltitude. The amplitude of the vertical displacement here reaChes 16-18 m.
in the baae of the ~ault acarps there is a fault trench from 3 to 10 meters
wide and 1.5 to 3 meters deep. Itg south walls are not always clearly
_ expressed and are usually more gently sloping.
The dislocations of the aestern part of the structure deform the alluvial
denosits of the 25 and the 14-15 meter terraces. The channel alluvium
and low floodplain terrace noted in places are not touched by the fractures.
The relation of the morphological elements of the terraces of the left
tributary of the Bulunda Creek on the opposite Wings of the faults provide
the basis for proposins the presence of a left shift of small amplitude
along the fracture. Further to the east the dislocations run along the
contact of zhe loose deposits and the root slope or, more rarely, along
the slope in such a way that the displacer plains and the steep scarp of
the slope coincide. Accordingly, it does not appear possible to determine
the true amplitude of the vertical displacement. Only in this case is a
system of three stepped faults noted cutting the debris cone of one of the
temporary streams 2.7 km aest of the Vitim River. The total displacement
amplitude along them is no less than 10-12 meters.
The e.~stern part of the structure on the right bank of the latitudinal
segment oE the Vitim River is expressed most effectively morphologically.
- The system of dislocations here extends almost continuously from the
Ozernoye Creek to the Kamennyy Creek a distance of more than 5 km. The
low, flat, divide cape east of the Ozernyy Creek is cut by 2 sublatitudinal
faults which bound the graben about 1~0 meters Wide and S00 meters long.
The fracture bounding the graben on the north has a vertical displacement
amplitude of up to 20 meters, and on the south, to 4 meters. On the
151
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~ox o~~icrnt, us~ orn.Y
upliEt~d limb nf eh~ norehern f~u1t~ 100 t~ 12U m~terg from it th~re is
pnathpr fr~cture par~llel Cn it with ingign~.firane (no mor~ than 3-5 m)
vertical displacem~nt, quickly damping to the flank~.
'Che disloc~tione Eormtng the grab~n m~r~p ineo c~ gingl~ f~u1C in the
eagtern part of Ch~ divide, contin~ougly running along th~ K~mennyy
Cr~~k. In iridividu~l gections it i~ aCCOmpanied by f~ath~ring ~oinC~
forming a gygC~m of ~C~ep fault with a total displac~m~nC ~mplieude nf
up tn 10 metpra. Th~ fault i~ traced hoth glong thp ronCact of th~
st~ep (to 25-30�) root slop~ and th~ loose dpposies of rh~ b~gin ~nd in
the boulder-block proluvium of the larg~ and sma11 debri~ ~oneg. 'I`wo k~n
west of ehp Kamennyy Creek'it cutg acroas the ad~oining debrig cone
270X350 met~r~ formed at the foot of the slope opposit~ the small runoff
trough. The gmplitude of the fault is 9 km, the aCeepn~sa of the fault
g~.~rp ig 35-40�. The scnrp ig completely cut by a temporary gtream, and
~t its bagp g n~W debris cone ia form~d 30X40 meters in size superpos~d
on a more ancienC one.
Between the Kamennyy Creek and the unnamed creek ta the west, Che proluvial
depoaits of their combined debris cone represented by metaeffusive blocks,
snndstnnea and granites are deformed by twa parallel tectonic trenches.
They are 15 meters apart, and the strike is latitudinal. The southern
trench is expressed morphologically more clearly, and its width at the top
is up to 10 meters in depth to 5 meters. The sides of the tre~ch arp
asymmetric: northerly with a slope angle of about 30� and 3-4 meters
above the southern, more gently sloping (15�). The unper trench doe~ not
hr~ve a vertical component, it is not as wide and shallower than the lower
one. In places, the southern walls of the trenches are missing, and the
dislocations are traced only along the scarp of the north wall, the
altitude of which does not exceed 3 meters.
To the east along the strike of the described dislocation, the Kamennyy
Creek changes direction of its current sharply from southwest and
meridional to latitudinal. Its more ancient channels on the south limb
of the struc[ure are of submeridional orientation. By matching some
channels with the tension ~oints of the eastern end of the Parama structure,
the stream has washed out a 25-meter socle terrace in the base of the
slope (on the left bank). The socle terrace made up of alaskite granites
lias been denuded to a height of 4-S meters. It is entirely probable that
part of the height of the terrace is due to the vertical displacement with
respect to the fuult, with which the creek is associated.
The nature and the interconnection of the various dislocations of the
Parama s[ructure indicates that it arose under the effect of tectonic
stresses essentially not differing from modern. For them, significant
tension in the direction transverse to the neotectonic structures causing
the formation of faults in the separation joints was characteristic.
As has been noted, the shearing movement along the shift plain has not
been excluded, for confirmation of which careful ground studies are
required.
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Thc avnilr~b~e mnt~ri~it~ da not permit uniqu~ Q~tim~tion di th~ tim~ ~f
f.~rm~tion o� the ~trurturp~ qn 3te w~st~rn flank eh~ e~igmi~ di~lnc~ei~ng
look appr~~iably o~d~r then on the right bank of th~ Vieim River. It i~
poasiblp ehat in the given c~ee a~ obs~rve th~ result of th~ euperpoeition
af two ec~rthQuakes~ the aeiamic d~slocationg for which grea toward eh~
ea~c, in the direction of ehe ttuya-Chara int~rbesin conanis~urp. Th~ ~
la~t ~f th~se Qarthquakes, the megnttud~ of uhich eould r~~eh 7�1/2
(forc~ 10) ocsurred, ~udging by the pre~ervation di th~ holioW form~ of
thp die~ocatinns, severai hnndred years ago.
Im m~d~rn tim~s thp Parama gtru~tur~ in pr~ctic~ Was gg~ismiC.
A/4-19. The Kemen atructure (Fig 39) ie located on the eouth eid~ of th~
Kemen embryonic bae~tn, in the vicinity of the m~rging of eh~ Naminga ~nd
Kemen Rivere.
2 km above the mouth of th~ Namin~ftivpr on the right bank g~arp, ~
Erncture zone wng diecovpred. The layer of gleciel bouldere orcurring on
the granites and underlying the seri~s of boulder loems wag shifted
12.5 metere here. The etrike o� the ahifter Was northeaeterly 30� at an
angle of ]5-80�. The interlayer of boulders on the subsided limb npar th~ ~
~ dieplacer~ occurs on a alent WiCh a dip to the eaet ~t an ac~gle of ZO�.
In the southeast along the gtrike of the fault in the glacial depoaits,
_ gently gloping scarps up to 3-S meters high are obeerved frequently
becoming broad trenches to 8-10 meters deep, cutting the mor~ine crust
and the dumped moraines. On the right atde of the Kemen River 5 icn Erom
the channel of the Naminga River, a scarp deforming the terracPd moraine
is noted by the aerial photographe.
The second fracture of the northeasterly (60�) strike folloWS along the
right bank of the Naminga River Valley and close to the right bank of the
Kemen River. Locally, it is isolated in the form of scarps on the slopes
of the valleys or stepped trenches with a difference in wall heights of
10 to 12 metera. The rock which has been crushed to the maximum is
8 meters thick. By the fracture. the glacier-WOrn rocks and other glacial
Eorms are deformed. The fault With an amplitude of 15-20 meters shifts
the debris cone of the emall atream; the cone overlaps the lateral mc~raine.
The displacer dips to the northwest at an angle of 50-70�. In the loose
. deposits the f~ult is expresaed by a low scarp ~ith a steepness of 28-30�.
The root denudations Which carry large (to 15 m) fragments of 8iir
surfaces, emphasize the fault displacer.
Tl~e total extent of the traced seismic dislocations is 4 km, and the
widti~ oE the zone is up to 0.5 km.
The a~e of the seismic structure is determined by the deformations of the
glactal and proluvial fonaations and by the comparative preservation of
- the dislocations in the last hundreds and first thousand years. The ~
153
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~a~ o~~tctnt, trs~ orn.Y
intcn~iey af the pazthryu~ke ~r~~ting :h~ ~~i~mi~ diginc~etong wn~ n~ 1~~~
th~n Enr~~ 10 (~ty7-~1/~) ~
A/4~20~ `fhc Cbgnl.hlir etruetur~ i~ ~s~driat~d wieh thp nutsid~ di the
. 't'~kkin~k~y~ b~~in.
tn Che ~~etion b~tw~en th~ Puri~hik~n and ehe ~bga~hlir ~iv~re~ the
cr~gt~d divid~~ arp cut by see~p ~ed 40�) faule ~earp, a r~~u1t of
which ~lmoffit r~gula~r triangul~r fac~tg ar~ formpd. In eh~ ba~e of on~
oE th~m, thpr~ i~ ~~t~pp C60�) ~earp from 4-5 to 15 m~tpr~ high mgktng
up che morpholo~y of th~ ba~ie disloc~tion wich ~ br~~k in ~ontinuity
- ~nd emphasizin~ itg lgter r~~uv~narion at a digt~nc~ of ebout 5 td 7 km.
In th~ p~~k ~~c~ic~n of one of th~ largest hanging cdrri~s ae ab~nlut~
~l~v~tiong of 1300 tn 1400 me~ere, in th~ gn~igs~B, th~ ~~paraeion w~il
nf the powprful roek ~lide ie fix~d. Th~ entir~ valum~ c~f the l~nd~lid~
ma~g "gplagh~g" ~ndth~ hanging cgnyon in it~ mouth se~Cinn Where modprn
d~pogics of the debris con~ dv~rlgp. Th~ 1and~lide front is cdmplicge~d
by l~rg~ and gig~ntic block acute-anglp mat~ri~l gnd rocky bloclc~`. Th~
~pprnximat~ volwne of the lende~.ip mas~ is 4.5-5 million m3.
_ Judgtng by the nature nf variation of the rock slide mass and the tectonic
srt~rp by the ~up~rpog~d erosion-denudation processea, the age of the
strurture daeg not exceed a fe~r hundred years.
A/4-21. The ttedved' etructure (Fig 4~) ie located in ehe eastern pgrt
of th~ Verkhnekalargk~ya [Upper Kal~rJ basin, on the left bank of the
Chitkanda River (the left tributary of th~ Kalar Rivpr).
The basic seismogenic dieturbances occurred along the Chiticanda f~ult
With northeasterly (45-SO�) etrike. The displacer dips to the northWest
at an attgle of 58-75�. The amplitude of the vertical displacement (15 m)
is establiah~d most exactly by the difference in levels of the bottoms
of the hanging valleys and their continuation in the do~mthrown side.
The outcrop of pre-Cembrian rock surrounded by Cambrian deposits is
deformed by the fault. A trench extending up to 2 km Was formed along
the Eault zone. The trench controls the faot of the ~~paration Wall af
the large seismogenic landslip of basement rock 400 meters long (along
the foot of the separation Wall) and more than 150 meters high. T'he Well
preserved separation plain aith enormous step surfaces drops to the norch-
wesc r~t nn angle from 58� to n~ar vercical.
The tot.~l extent of che traced seismic dislocations is 4 km.
The .~~e of the dislocations is deterrained on the basis of the defot~ations
oE the ~lacial, cumulative and erosion forms as Holocene (the first
tiiouaands of years).
The dislocation parameters indicate the force to an intensity of the
enrthquake creating (it~7-1/2).
154
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~9 ~1D ~ll ~/1 ~!J ~l4 lS
Figure 39. Seismogeological schematic af the Kemn basin.
Compiled by M. Dem'yanovich.
1-- granitoida; 2-- sedimentary-~metamorphic formations of the
i.ower Proterozoic; 3-- glacial deposits of the first glaciation;
4-- glacial and aater-glacial deposits of the se~ond glaciacion;
5-- glacial-proluvial dia~ointed dislocations; 6-- proluvial
depoait; 7-- alluvial Upper Quaternary and modern deposits~ `
8-- ice �ielda; 9-- Holocene fractures and amplitude of vertical
ahift (bergscrich in the direction of the subsided limb); 10
fracturee activated in the Cenozoic; 11 pre-Cenozoic fracture~;
12 eei~,i~ trenches; 13 glacial-cectonic trenches; 14
_ glACia1-tectonic acarpa; 15 glaeial trenches (relica of multi-
story valleys).
Key: 1. Kemen; 2. Naminga
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- ~~tt O~~ICIAL U5~ ONLY
_ ~ _ _ _
.
- � .
� � e
L e~~ i r ~
e s.r~ ~ ` e
e ~ ~
s e s �
e � s
~
~ e /
z~
1~ e
r .
~~d`'~' ' ; � . r
~ , rr r rr
a � � 'i' h=/ M
~ 4~~'~' r~r~r r~r
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~ ~8 Ql0 ~/1
- ~igure 40. Plan vi~ of the ttedved' aeigmogpnic gtructure.
Compiied by M. Dem'yanovich. _
1-- modern and Upper Quaternary alluvial depoaits;
2-- Niddle and Upper Qua~ernaty glacial deposit; 3== terrig~nic-
carbonaceoug rock of th~ Pgle~zoic; 4-- pr~-Cambrian s~dimentary-
metemorphic formation; 5-- granitoide of the pre-Cambrian;
6-- gabbroids of the pre-Cambrian; 7-- seismogenic fractur~
(bergstricha of the direction nf the sub~ided limb); 8-- pre-
Nolocene fracture; 9-- landslip,fault plaina; 10 direction
of ancient vall~y; 11 aeismogenic trenches; h-~- amplitude
of verrical displacement of the landslide-fault; the arroW aith
the numb~r ia the dir~ction and engle ~f incidence of the
di~plac~r
Key:
1. Kalar; 2. Chitkanda; 3. MedvEd' Creek
A/4-22. The ArguP.en structure is traced to the east of the river of same name
on the south gide of the Tokkinskaya bagin. The seisa~ogenic deformations
(nbout 3.5 km long) are accompanied by a crushing and schist-formation
strip (100-2(10 mpters) in th~ Archean granite-gneisses. The rock haa
been strongly broken doan and is intensely jointed. An abundance of
small cleavage jointg are noted Which can be connected yith shearing
displncement. Thia ia confirmed by noticeable lefthand achists of the
nxinl perta of the sa~all dividea.
156
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~Ott d~~ICIAt, U3~ Oi~fLY
`C1� vereie~l digpi.~~pm~n~ wieh re~p~et tn th~ ~r~~ture ~eh~ dd~mehrawn
uplnhd gidp) i~ ~xhibit~d in th~ ~xi~i g~~tion~ of th~ dir~id~ wh~r~ ~ru~h~d
gr~ni~~-~neie~~~ ar~ uncdv~r~d along eh~ ~oine~ At ~u~h pl~~~g, ~
"eorn" ~eper~Cian ~urfec~ ie ob~~rv~d aiong Whi~h pune~ur~ ~f individu~l
hlnr.kp enk~~ pinre. Th~ ~npin~ ef ch~ ~ointe r~~r.hp~ 4 t~ 5 mc+t@r~ in el~i~
en~c. Un th~ cfivid~~ wlihr+~ g~hick e~lu~~~luvi~l Covet' hag developed, ehis
~one i~ u~uaily tr~e~d in eh~a fdrm of ~~h~11d~~ Ct~ O~ S-1~ 5 m~t~rs)
~r~n~h 2-5 m~t~r~ widp. ~n plac~~ th~ tr~neh ig ~ompl~t~ly ~tr~~n aith
talu~ ~~terigl. a n th~ ri~ht gide of ~h~ traugh vali~y of the At~~uk~n Riv~r,
~meli rockelid~~ end i~nd~lidee of th~ t~lu~ ~ov~r ~re conn~c~~d uieh thi~
zon~.
A/5-l. The Kuduli atructure ia lo~~t~d at th~ fooe d� the nor~h ~id~ ~f
th~ Kuduii River vall~y (the right tribueary of th~ Oi~kma Rtver) ~nd i~
~~edei~ted with thQ line of dielocation~ with ~ break in continuiey of thQ
~ubi~tieud~nal ~trike~
The geigmog~nic r~~uv~n~tion is repr~e~nt~d by ~ tWO-m~Cpr faule ~e~rp nf
n~rthae~terly (2~0�) 9trik~ ext~nd~ng 0.5-1 km and c~~arly ~xpre~e~d in
ch~ r~lief. A xone up to 3~4 m~tpr~ aide of gh~rpiy diglocated b~dding
nf Jura~~ir flaggy eandst~n~ is traeed. Ingidp this xon~ ~ v~rrical
~ rdgitidn of the individual platforms ~aving ~n ~r~a ~c~ 2 r~2 i,~ nbted.
nn the upthrnwn 1imb, sma1~ roclcel~de~ ~rp norpd in th~ dir~ction of the
doanthro~m limb up to 40 m in area. Over th~ entir~ extent, the
~tructure i~ ~ccompan~ed by a strip of felled for~~t. The fa11En tree~ are
ori~nt~d to the ~outh.
The Eora?ation of such a dislocAtion occurr~d, judging by the fractur~ of
ch~ gnil end vegetgcion layer~ r~rpntly (d~cadeg ago) ~nd could be ceused
by an earthquake of force 9 intensity (by comparison vith the geismic
dislocations in the case o# the Olelana and the ~Iyukzha earthqu~kes (1958).
c (3)
. :i . ~
T ? slwM�A:?r ~
I
a P~3~'~~S
Figure 41. Plan of the Sarkhoy seismogenic structure.
Compiled by V. Nikalayev.
1-- Cambrian carbonaceous rock; 2-~ sceep (50~60�) erosion
slope of the Sarkhoy River valley; 3--~ brow of the erosion
scarp; 4-- plane of the sheared peak; 5~- faults
Kcy:
t. Sagnn-Ula; 2. south; 3. narth
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g/1-1. Th~ 5grkhdy ~eru~eure (~~g 41~ ig ~.tlC~Ep(~ dn fhe i~~e b~nk df ehe
r~v~r Wieh ehp g~m~ n~mp, fh~ right tribut~~y di th~ Ti~~~ ~i,v~r, at
3~g~n-U1~ Moun~~in (2437 m~tQr~)~
`~h~ ta~ p~r~1~p1 f~ults pxt~nd fn th~ naeehe~~E~rly dir~~~ian (~5~4~")
~nd ~tr~ obvinu~ly ~xpr~~g~d in th~ fd~n of ~t~~p ~e~rp~ dipping e~ eh~
~nu~h~a~c ~t an ~n~i~ ~f 65-70�~ Ttti~ f~~lrg ~hif~ Wieh eh~e ~h~iW~~~ of
thp t~mpor~ry ~ere~m~ ~nd thp divid~~ ~~p~r~eing ~h.!~~ `Che fr~ctur~ ~dnpr~
~r~ n~comp~ni~d by light gr~y, w~~kiy e~mpne~d br~~ei~g Wieh ~ia~~i~
r.?~t~ri.~l frdm O.S tn 5 cm in gixe~ 'Th~ Mdge pxtend~d ig th~ ldw~r r~~arp
h~ving ~ l~ngth nf 2 km ~nd ~ vprfi~~l digpl~eement ~mplitude nf 2 meterg.
pernlipi to ie 200 m~t~r~ highpr ~1ong th~e glope~ cam~~ ~h~ g~cond fraeEur~
1.5 km lon~ Wi~h n v~rtir~l digplac~m~nt ampiieud~ of 0~5 t~ 1 met~r.
'Ch~ fir~t ~nd ~~eond Eault~ ~rp ~eeampani~d by f~~th~r fr~eEur~~.
` lt 0
1, A~10-/SM
~
'p A�1,3-2,0~+
1
, a~
.
�.I
~ , 1
. y,,,~. to~ro:or
~l ~l QJ QS QB `~7 R~~ 9 r' +
figure 42. Scheroatic of the Tologoy structure. Compiled by
M. Dem'yanovich.
1-- levelled surfaces of the peatcs and their brovs; 2�~ slop~;
3-- flattened part oE the divide; 4�-- side of the Tissa River
vnlley r~nd the broW oE ~he divide; 5�-- r.ival cirques; 6--
acarps oE th~ bald peak terraces; 7-- alluvial-proluvial
d�posit; 8-- vy~ypka (rock fragmeats scattered sho~+ing the
presence of bed rock) of large block material on the divide;
9-- proposed dielocations ~,�ith a breek in coetinuity;
h vertical dieplacement ~mplitude.
Key: 1. Bnruun Dabaeta; 2. Shuluuk Tologoy
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f~n Ch~ noreh~a~t~rn ~nd o~ eh~ ~~i~mog~niC ~oint ~yeCpm~ ro~k,y seripping
df eh~ eop~ ~f eh~ ~~climpnt~ry ~nlumne noted glong the pl~in (aboue
4000 m2 in ar~~) di,pring at an angle of 25-35� eo the eouthwest 230-~40�. ~
Judgin~ by the acal~e of Holocen~ re~uvenaeion o� ehe 5arkhoy fault, ie
- ig po~e~ble,to propos~ th~t th~ form~tion nf th~ S~rkhoy srructure is
eann~cted with ~n ~arthquake w3th an ine~n~i.~y ~o force 9. The eime of
ferm~tian of the erructure ie determin~d wi~h a large proporeion of
~onditionaliCy. Th~ geofl preaervation of the fgult scarpe in Che ehalwega
~nd on th~ dividee of the emall r~vines indicates thgt the age of rhe
gtructur~ ie a f~w hundred yeg,r~ oid,
The mod~rn activity of rhe a~cructure ie emphasized by ehe epaCial
coordination wiCh the Sarkh:oy block of I~r~l'ehoy Sayan of ewo epicenters
of ~tr~ng earthquakes with, K~12 end 14 cforce ~-6 end 7-a, reapeceively).
tl/1-2. Th~ 'Tologoy gtr?acture (Fig 42) is locat~d nn the left bank of ehe
Tt~ega Riv~r betaeen thE~ Shuluuk~Tologoy (absoluCe elevation 2328 meters)
nnd the Zholgyn-Sar'dag Peake (abeoluCe elevation 2442 meCera).
Th~ bnsiC disloc~tian is expreseed in the form of a scarp with northwesterly -
strike 1.5-2.Q metprs high on Che flat divide of Che Sentsy and Tisss
� Riv~rg. The gently sloping scarp (lesa than 30�) is traced at a distance
of gbout 5 km. In the individual extended aections it is emphasized by
linenr concentration of the abundant brushwood vegetation. -
"Che goutheaetern end of the dislocation with a break in continuity in the
- divide part of the side of the Tisea River valley is expre~sed by a
tr~nCh from S to 12 meters deep and up to 15 meters wide becoming a ravine
dipping into the Tis~a Itiver valley. Along the sides of the trench,
silieified and ferrugittized epidote-chlorite shales are exposed. The
rocks are sharply ~ointed with a large number of slip surfaces. A scarp
about 1.5 meters characterized by the same attributes runs from the basic
dislocation to the east. In the upper part of the root slip of the valley,
the scnrp is traced in the bedrock at a distance up to 200 meters.
On the gentle slopes of the adjacent levelled peaks, linear scarps are
observed which are similar to the basic one, sometimes extending more than
2 km~ coinciding in indiv~dual sections with the slopes of the bald peak
terraces. On the right bank of the Baruun-Dabaat River, an erosion-
tectonic acarp of aubneridional atrike is traced. On the surface it ~
becomes a linear strip of finely clastic material with dense vegetation.
'Chis zone extends more than 5 km. Cases of it are noticeable on the
raot divides, in the levelled bottoma of the saddles, and on the gentle
slopes.
It is poasible to propose that some of the above-described deformations
could be �ormed in recent decades the �irst hundreds of years ago
during an earthquake with force 9 intenaity.
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v v V ~ ~
~ ~ v . y yi .
v ~ ~ v
v ~ . ~ ~ , .
~ / v . I ~ . -
i' ~ 1 ' 'II � . ' � � :
~ v v v ~ ~ ~ .
. Y hm G.T-20n~.; . .
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~ ~ v V ~
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~'1 V V
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Figure 43. Visual plan (with refinements by aerial
photograph) of the Dugaray structure.
Compiled by M. Dem'yanovich
- 1-- sand-shingle channel and floodplain deposit; .
2-- bottom moraine deposit; 3-- debris cone deposiC;
4-- Neogenic basalts; 5~- pre-Cambrian epidot-chlorite shale;
~ 6-- faults activated in the Cenozoic; a-- established, '
b-- proposed; 8-- brows of the seismogenic landslip; ~
9-- formations of th~ landslip facies; 10 brows of erosion,
scarps; h-- height, R-- total length of the landslip zone
Key:
1. Tissa
- B/1-3. The Dugaray structure (~ig 43) is located on th~ left bank of the
Tissa River between its tributaries Terp,ete and Dabaat. ~
On the slope on the left side several fresh landslips are noted traced
for a distance of 350 to 400 meters. The landslips are located in the !
tectonic disturbance zones oriented on the northeasterly and near
latitudinal directions. The west landslip has an area of 100X50 meters.
It is undoubtedly the case that the outl.ines of this landslip were greater,
- but the annual mud flows have reworked it. Along the rear o� the debris -
cone, a trench of sublatitudinal strike about 2 to 2.5 meters deep and
about 200 meters long can be traced. On ~he slope along the strike of
the trench, erosion cressts of temporary streams are complicated by
transverse scarps and saddles.
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Fa~ ~~~ictat, u$~ oxt.Y -
'the lyrow o� the g~p~rati.on wall of the uest land~lip Co the ~nutha_~gt
coinci.des with the li,n~arly ori.~n~t~d e~arpe to 3 meC~rg high~ To the
north~ast there c~re two sm~ll close lgndgl~p~ with g total l~ngth of
bbout 250 m~Cers. The height of the eeparation walls of the landsli~s is -
to 30 meters. The deposits o~ th~ proluvial debris cone in the eurface
of the Cenozoir basalte o~curring in the valley arQ covered with landslip
materigl.
, It is posgible to determine the gge of the geigmic etructure by the over-
lep oE the landalip formationa on the glacigl depogiCe and the faults.
During preglacial time~ the cover of the basoltg Wag deformed and shifted
wiCh rpspecC to a step aystem of faults r~f northeasterly gtrike. During
che glaciation, ihe surface of the doamthrown blocks Was prepgr~d, and
the baealt cover was partially deetroyed. a typicgl exaration relief wae
, cre~ted in the area. buring the poatglacial Cime the tector?ic mnv~mpnts
led to furrowing of certain faults. Accordingly, the formation of the
seismic landslips which covered the accumulative and exaration glacial
forms took place.
Judging by the par~meters of the seismogravitational phenomena, they could
occur for an earthquake of force S-9.
' B/1-4. The Zabit atructure is located on the right bank of the Zabit River ~
2 km north of the mouth of the right tributary of the Sakhyurta River.
On the south slope of the mountain With an absolute elevation of 2414 m,
an erosion-tectonic acarp is traced Which runs c.o.the northaest into the
linear zone intersecting the highland terraces, divides and individual J
bald outLiers. _
The age of the formation of the tectonic disturbance ia provisionally
established as the Holocene on the basie of. the deformations of the fora~s
of b~ld peak planation Which are formed intensely from the end of the
Upper Pleiatocene to the present time. The total extent of~the fracture
reaches 3 l.m, the maximum amplitude of the vertical displacement reaches
nbout 2 me[ers. These deformation parameters can char~cterize the intensity
_ oE the earthquake generating them at force 8-9.
- D/1-5. The Shulun structure (Pig 44) is l.ocated on the south slope of
- the Kropotkin ridge which borders the Oka basin on the north (3 km north~
wer~t of Khuzhir) .
At the foot of the mountain With an absolute elevation of 2887 meters,
a fault of sublatitudinal strike aas uncovered with vertical displacement
of the ~ralls of the fault to 25 meters. The south Wall at the foot of -
the mountain was dovnthrown, The fault scarp is most sharply er.pressed
in the dlvide of small streams (the tributaries of the Oka P.iver) Shulun
and Bulag-Shebey, s~here the fault cuts the Upper Proterozoic granites
for ~ distance of about 2 km. On the surface of the moraines in the
trough valleys, the traces of the fault are noted in the form of
161
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twc~ comparatively ~ently eloping egymmetrir crench~~. In the mndern
c~rnpton cut in the ~lttrinl depositg under the trenchp~, an inciined
Htrip i~ obeervcd which correepond~ to the dieplacee in which thp mo~t
conreely claetic mat~ri~l i~ ~oncentrgted.
. f
.
' ' ' / ' '
~ i � Y �r ~ ��r J~
~
; ~ ~ ~ ~ , ' . Y
~ ~ r~ ` : e ~
' , =
- ~ ~ I / 1'
-r,, 2 ~ : ~ ~ _ ~ ee~. ; ~ ~ ,
~ '
~ ~ ~i s
( _
~ ~ ~ w ~ 4 � ' 1 ~ � ~ '
:
_ ~ ~~�p � r ~ ~ ~r
~ i �
e e . ~ a_ ~ y a~alnr~
- ~ � ~ ~ ~3}~ �o -r
~
e h� tO~ MJO?~ a~ e E � r
I r ~ s s ~ ~ ~r
so � � ~ ' y ..i .�:r
~ 0 � � . . e - ~ ~ \ ,
~ ~ ~ '
� � ~ O~ O ~~1~�
_ � 1 � ? ~ ( ~ ( ~~0/~ / 0
~ ~ . ~ i . . ~ ,r, xy 61(7p
� / � ~ � ~ ~Mt~ i ~ /
~ ~ ~ O
j a ~ � f ~ V ~
~ ~ ~
~ ~IS N f\
V
~ y v V~-~ V
~ ~i P
I ~1 v v v r v v
~ ~ V v y v V v / _
v y v
v v V V V vV V V V '~~..r~ ~ `
1 V y V V V V V r ~
_ ( V V V ~ V V -i ~j ''f
~ V V V V V y J ~ ~
~ V~ V V V r ~ -
( V V V V V V ~ r j/~ r 'i 'i '~f'
V V V V V 'i , ~
~ r-� ~
o~o
~
~l~P l~J~ ~ ~v~ S ~6 -r 7
' y 9 'O ~ 9 f0 Q 1 f ;r;~:� f2 '~M fJ 1~I
Pigure 44. Plan of the seismogenic Shulun structure.
Compiled by M. Dem'yanovich.
1-- alluvial depcsit; 2-- seismogenic landslips; a-- deposits
oE landslip facies, b-- separation wall; 3-- deposits of the
boulder train at the foot; 4-- glacial formation; 5-- Holocene
basalt; 6-- Pro[erozoic scarned rock; 7-- Proterozoic graniteids;
8-- faults active in the Holocene (bergstrichs in the direction
of the doWnthrown side: a-- reliable, b-- proposed); 9-~-
fnults active in the Cenozoic; a-- reliable, b-- proposed; -
10 ancient fault; 11 erosion-tectonic scarps; 12 zones o�
intense brecciation in the scarns; 13 hei~ht of the fault
~carps; I4 a-- direction of dip of the displacer, b-- pro-
posed limit of spread of the landslip mass.
Key: 1. Saylag; 2, Ikhe-Sagan-Sayr; 3. Bulag~Shebey; 4. Shulun;
5. Oka; 6. Khuzhir _
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a
~ The Enrm~ti~n~nf the ge~.~motect~nic dieldcetinns of the Shulun gtructure
wns ~ccompnnied by num~roue seiemugrnvit~tional ph~nomena, primarily
rockslidea. Th~ larg~ ]nndRlipa occurr~d direcCly in the zone of ~,reak
cectonie dieeurhunce (~he right aide of the 5hulun River vallye and the
= leE[ gide of Chp Bulag-5hebey River valley)~ The two sma].1 lan~del.ipa in _
- the mouth part of the Khara~Zhalga River~ Che right tribuCary of Che
5aylag River ar~ ~esociat~d with the Saylag fault. The divide cap~ in
th~ vicinity of Che pmergence of the 5aylag Riv~r in the Oka basin was
deformed by the landslip. The landalio material covered the moraine
depo~it,. The outline of the landalip amphitheater is drawn along the
large-lump material on both banka of the Saylag River. The maximum land--
slip masa wae concentrated at the aeparation wall over an area of 0.7 km2.
The separation wall with a total area of 0.8 km2 oriented along the long
axis to the souCheast ia sharply eroded. Carbonaceoua roc~: in~ected with
- gneisa granitea is~exposed in it~ The rock is intensely crushed and
milonitized.
All of the seiemic dislocations of Che Shulun structure are within the
boundariea of the large Oka fracture zone branching from the Main Sayan
fault. The nature and the dimensions of the seismotecConic and seismo~
grnvitational deformations of the earth's aurface permit estimation of the
interisity of the earthquake of more than force 9 creating them.
?
The age of the seiamic structure is established by the deformations of the
glucir~l, erosion and other forms and by the superposition of the formations
of the landslip seismogenic faciea on the glacial and alluvial deposits
_ (the latter occur on the Holocene basalts) in the Oka basin. The age of ~
- the seismic structure is hundreds of years according to the abovP-presentea
data. There are reasons for assuming that epicenters of the strong earth-
quakes of 1858 and 1859 could be associated with this structure,
especially the strong earthquake of 19 Noveaaber 1859 when the force of _
the earthquake reached 8 in the Aliberovskiy mine 90-100 lun from the
Shulun structure region.
B/1-6. The Khazalkhy structure is located on tlie divide of the Oka River
and its left tributary, the Khazalkhy River 14 1�.m south of Sorok.
~ I[ is a rectilinear zone about 2.5 km long traced in the metamorphic
shales dipping to the northwest 350� at an angle of 65-78�. The stril:e
of the geomorphologically expressed line is northwest 280�. In the
terrain it is a acarp ~.5 to 1.5 meters emphasized by abundant grass and
moss vegetation. The impression is created that the modern denudation
surface of the divide is deformed. The ampli[ude of the vertical displace-
ment of the denudation surface is lowered from the center to its edges.
On the slopes, the scarp is lost in the deluvial deposits.
. B/1-7. The Tustuk structure (Fig 45) is located in the valley of the
middle course of the right tributary of the Oka P.iver of the same name.
The geomorphologically proposed seismogenic rejuvenation is expressed by
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~hnrp rectilinear scarps. At their base �requently gently sloping
gubaidenceg are observed wiCh whi.ch the small lakes elongated in the
lntitudinal direction are asaociated. This entire sublatitud3nal zone
of struCturxl forms expreoaed in relief is 6 kr.~ lnng~
The eroaion-tectonic (7) acarp to 3~4 meters high is traced moat clearly
along the left side of the Tustuk River valley above Che mouCh of its
left tributary, the Dooda-Unagan Creek.
A second,clearly expressed fragment of the structure is associateci with
its eastern f2ank and is located along the right side of the Tustuk River
valley above the mouth of Yakhoshop River. This ia also a linear scarp
5-6 meters high superposed on the glacial forms of relief. It is identi
cally obvious on the surface of both the bedrock and Che loose rock. This
ia expressly well expreased at the termination of the fault scarp where
it ahifts the debris cone of the unnamed right tributary. The amplitude
of the vertical displacement ia 3-4 meters. On the north, upthrown wall
of the structure, Che stream is cut into the debris cone, and on the
downthrown wall, accumulation of the loose material is observed, so that
a young debris cone of smaller dimensiona is fnrmed on the older one.
_ ~ ~ ~
y un . ~ ~ i
. I i .1_~ . _
. y�.'Yt:
- ~1 ~i~y [~s
Figure 45. Plan of the proposed seismogenic Tustuk structure.
Compiled by V. Nikolayev.
1-- slopes of the Tustuk River valley; 2-- alluvial channel
deposits; 3-- debris cone; G-- faults: a-- established,
b-- proposed; 5-- stripping of the eluvial-talus material�
Kcy:
1. Tustuk
- The clear expression of the scarp in the loose deposits of the debris
cone and its good preservation indicate that this formation is quite young
within the limits of the first hundred years. Whereas in the process
of the farthest, mo~t detailed seismogeological studies the seismogenic
nature of the young fractures can be confirmed, the Tustuk structure can
be certainly coordinated with the seismic dislocations formed during the
force 10 earthqual:e.
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_ The mod~rn lev~l oE eeiemic activi,ty o� the vicinity of the Tustuk
ia determined by the cnordination of the weak ~K~6-11) and moderate
(K-12-13) earthquakes wiCh it.
g/2-5. The IaCokakaya aCructure (Fig 46) occupies the Sor Cherkalova
Bay (rhe Istokskiy Bay) [the underwater portion of the partially aub-
- merged river basinJ and the lowland and aharply awampy sections of the
ahore ad~acent Co it. The bay is located within Che shallow part of the
souChwestern edge of the Selenta River delta and has a maximum depth of
up to 12 meters, gnd over the larger area, no more than 3 metera. The
Istokakiy Sor is separated from Baykal by a aubmeridional elongated
barrier of sandbars (the Karga Lemeaova Peninaula, the Bab'ya Karga
Island), and on the southeaseer it is bounded by the narrow (0.2-1 km)
strip of lowland awampy shore ad~acent to the rectilinear~scarp 10 to
12 metera high, the gncient Fofanovskaya (third Selenga) terrace. In
the expoaed acarp dike Che fine-grained sands are revealed.
According to the data af the geoohysical work of A. P. Bulmasov and
the prospecting holes of V. V. Samsonov and G. P. Ponomareva, the
vicinity of the large Del'tovoy fault in the crystalline basement
_ coincides with the acarp line on the surface. Another fault bounds the
bay on the west, being placed in the basement on the sandbars separating
the bay from the Baykal water. Thus, the structure in plan view is
approximately equilateral tectonic wedge with approximately 10-km sides.
On the norCh where it smoothly joins the floodplain in the surface
terrace of the Selenga delta, the wedge is about 5 km wide.
It is proposed that the terraced section of the shore outlined by the
Eaults was downthrown under the level of Baykal as a result of the earth-
quake, similarly to the Posol'skiy Sor (Solonenko, V., Treskov, 1960, p 4)
and the Proval Bay, and subsequently was buried under the beach sands and
bed loads. The Kudara (second Selenga) terrace, fragments of which were
preserved on the southeast shore the bay and, possibly, the part of the
Fofanovskaya terrace next to thc: lake were involved in the seismogenic
burial. The maximum deformation of the earth's surface appeared in the
southern part of the bay, in the vicinity of the 3oining of the faults
bounding it. The ar~plitude of the lowering here is no less than 10-12 m.
The great similarity in morphology, size and structure of the Istoksskaya
[IstokJ structure with the Posol'skaya [Posol'sk] structurel and the
obviously seismotectonic formations of the Proval Bay permits consideration
of common genetic roots in their origin. The subsidence permits
iThe calculations performed by A. A. Rogozin (1974~ with respect to the
buildup rate of the sandbars in the Posol'skiy Sor indicate that they
_ ~ppeared for the first time in the bay annroximately 500 to 600 years ago.
In the Sor, the older residents still remember the flooded trees, stumps
and logs. Consequently, the age of the bay is about S00 years.
I65
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~
c ~~0:: .
- ' ~,;:;.;;s:
~o . ~ ~ ~ ~ -
(s) ~ ( ~
~ ~ ~
~
s ~ � �J2
I '+c, + , /~/i
I : o %f rigure 46. Ptan of the Istokskaya
I and the Posol skaya seismogenic
~ structure. Compiled by A. Abalal:ov.
/
1~- scarps of the terraces of ~
tic o// suopusedly seismotectonic origin and
1 their hei~hts, meters; 2-~ fault
' ~ zones in the cr stalline basement;
~ y
\ 3 sections of seismotectonic _
~ ~ " subsidences; 4 Kudara and
\ ' ~ ~ ~ ' ~ ~ ' ~ Fofanovskaya (Middle to Upper
~ 'y~~~�'::'.;,..~�
Quaternary) terraces; 5 floodplain
's and f irst terrace above Che f lood-
plain; 6-- gas and thermal mineral
O \
ss r water shows; 7-- epicenters of _
~ ~ 1 force, 7, 5 and 4 earthquakes,
~
alD respectively.
~ J ` /loeonacrs
~ 4 Key�1. Povorot~ 2. Posol'ski
~3~ 1 ~ ~ v
~ S 1~::;�.;;~; Sor Bay; 3. Posol'sk;
e '6o~'~~y � 4. Bol. P.echka; 5. Istok;
s 1,�ti~: 6, Istol:skiy Sor Bay;
~ ,5,8 7. north; 8. south
~ �1 ' ~
O a s
- ~
~ � o
~ ~
~
~o^� ~ ~
o t~ /
I7o.opo~n
~1) s ; j
~~1~~~~~~~~~~~~~:~.
~~.5 ~1~:~~~~: ~
L ~
166
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r.ongid~r~htion nf Cnmmon ~eneCic rooCs in th~ir nri~in. Thp Igtnkskay~
atructure is prababiy ydunger Chan Che Posol'gkgya sCructure. 'Thig ig
indicated by thp gr~at~r depehs o� the bay, the ~mnller ~mnu~t df erosion -
uf the shor~s, ~nd compnr~tively weak isolation from Che lnke.
t3/3-4. Th~ Svyntonosskaya (Svyatoy Nnsj structure ~ig 47) ig locaCed on
the Svyntoy Nos Peninsula (the east shor~ nf the central part of L~ke
Baykal).
The peninsula lies on th~ northeastern continuation of the O1'khonsl;aya
br,anch of Che Obruchevgkiy fault.
'Che seismotectonic dislocations of thp structure are rehreseneed by fau2rs
~ynd separation ~oints. Th~ basic system of seismogenic faults was
revealed in the headwaters of Che Markovo River where Chey are traced
_ more th~in 5 l:m in the form of clear rectilinear, subparallel and inCer-
secting fractures. The lengCh o~ the individual dislocations is up to ~
1.5 km. On the top of the mountain which is made up of granitea, the
lon~esC segroent of the fault forms a 30-50� scarp up to 10 meters high.
'fhe eastern wall is downthrown.
In the snuthwestern part of the investigated area on the gently sloping
divide of the Dolgyy and SneZ::~.yy Creeks there are two subparallel step
faults bounding the block inclined to the southeast.
_ On ttie northwest slope o~ the left divide of the Dolgyy Creek there is a
seismotectonic graben. It is 320X17C;0 meters in size. Here along the
system of step faults (northeast strike 45-50�) a peak part of the divide
crest was downthrown. The wall of one of the faults at the foot of the
mountain Eorms a tectonic dam 4 to 5 meters high and about 1 km long
intersecting the bottom of the ravine (Fig 48).
The gravitational-seismotectonic disturbances are r~presented by landslip
faults and fractures with significant gravitational components. The
formation of this type of deformation is connected with movements along
- the E~zults with simultaneous removal by the gravitational forces of the
- mount~lin masses dismembered by them.
'('lie seismogravitational phenomena include landslips, landslips-slides,
l;~nclslides and talus creating seismogravitational amphitheaters on the
~I~pe, hummocky and swell-sinkhole microrelief on the surface of the down-
tlirown root blocks and among the landslip masses. The largest seismo-
~;enic landslide-landslip is cc,ordinated with the steep divide crest at
the I~c:~dwaters of the M.arkov River. The volume of the landslip reaches
42 million m3. The displacement of the rocky massif occurred in the
- n~,rtt~westerly direction to a distance oE 300 m. In plan it is circular
in shape (350X200 m), 25 m hi~h. The smaller landslide-landslip wi[h
- respect to tlie dimensio~is occurred on a steep divide cape of the left
trihut.lries of the Dolgyy Creek. The surface of the separation wall has
a slope of 35 to 40�, and the size is 250X500 meters. The total volume
oE the landslip mass reaches 26 million m3.
167 ~
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~dR f1~~tCiAL U5~ nNLY
� r � 1
. 6 r ~ ~'C5 ~J
~ z ~ Q ~
(1) o ' 2t,/i ~ss~.. i
4 i o~~~ , t~ s
i/y / e.~e i
Q y~~~ G~ l96Be. U s
� 1(6)
0 3 r8/x ~9s,., i . r
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� / i ~~P/XI J869t, � 6 _
16,~V ~9J9e. J ~i~ ~ 9
(3) � s~'o~ ` ~ �
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i A NKA n~CKOE ~~P~ ~ 6~' f;~�~ J ~p P1'~c
H a r o o b c ~~N ~~oN ~ v E �b ~,Q' A~
. . ~ . o.~, o ~ =
� � .AN~AV~ ~ � ~0 fi ~ � s !
- _ _ ~o~"` o . e~�~~ � m,,~rE6 ~ '6 E ~
E '
~ ~ eq~ ~ .�C~~ ~ : o. ~ P ~ .
Q ~
I ~(lE1 0 . : .
~ .b ~ ~d~ ~ '
~r` ~ ~ I~
i O � ~ ~ ~
~ ~ ~ ~ N., . ~ O M ~ ~
\r '
� ~ ~ ~
8 ~o~. 4 � ~ ~ ~ .c,~
= b~ ~ r . ~l~`b ~o . ~ � S
. o 1 ~ o � 0 ~
d~~ ? . ~ ~ ~ o
- . . ,e . e tg~ ` ~ ~ , ~ o ~r ~1,~~ a � a.~ I `~t
< 16 ) o i~ � ~ 0 P I P 6 6 ~
. Q O o ~ ~ ~
q o R~ .
~ . ~ , C ,
~
'
~ . ~ A ~ (15 ) ~ � ~1~~.
�
nA~ r b~yfAti o, b~, a~
~.r, , o. o
o , ~ ~ Q ~ p0 .
0
r � Q~" o
~ . (13) 60 (11) I
~o e o . ~ ~x B e � ~ ,
o ~ 0 ' . _
, D . o '
� ,A 6 n !i2>� � � ~
,
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a � � ~
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O
o ~O � � �
- _ ~
(K~9). The numbera in the notation correspond to energy clasaes of the
- earthquakes. ISee key on p 226J
225
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rox o~~~c~nL crs~ orn.Y
~Kr.y cr~ r~~ ~a, rr 22aM2zs~; ~
1~ Northt~rn gayk~l Hi,~hland; 2~ Upper Anggra r~dg~s 3. Delyun-Ur~n~kiy
ridg~; 4. Kodar ridg~; 5~ Southern Muya ridgej 6. Udokan ridge;
7. Kalar ridgp; 8. Vitim plateau; 9. Vitim~ 10. Ol~kmn Seanovitc;
11. Bnr~hchovochnyy ridge; 12. Y'~Ulonnvyy ridge; 13~ Chita; 14~ Khilok;
1S. Ikatskiy ridg~s 16. narguxinskiy ridge; 17. Baykai; 18. ~aykgl rid~e;
19. U1~n-Burggey ridg~; 20. gAN; 21~ Ulan-Ude; 22~ Primorgki,y ridg~;
23. 'IrkuC; 24. Irkutek; 25. Khgmar-Da ridge; 26. Gueinoye Lnke;
27. Dzhi.da; 29. Dxhldinskiy [Dzhida] ridge; 29. Seleng~s 30. guren-Nuru
31. gulnay Nuru r3dge; 32. Khubeugul Lttke; 33. Voetochnyy Sayan
[Eegtern Sayan~; 34. 2ya; 35. Oka; 36~ Angara; 37. Lena~
The manifeatations of Che seismic proc~~s in the Bgyknl sei~mic zone are
v~ried~ Thp e~rthquake acoarms o�ten occur in the Barguzinskiy ~taynn, in
the Kodarn-Udokangkiy Rayon, in thp viciniCy of Ch~ Upper Piuya-Muyakan
baein~, along the Obrucheskiy fault zones in Central Baykal and the
meridianal part of the Shurmaneko-Shutkhulayskiy fault in ehe extreme
southwest. The earthqunl:e ewarm in the Ikatskiy ridge lasting several ~
yenra is unique. Ag a rule, th.e locations of the awarme did not repegt
durin$ the instrument ~~ismologic~l observation times. Sometimes the
awarme occurred in practice at the same places where at anoCher time -
. seismic proceas developed fifferenCly a atrong earthquake was
accompanied by a series of afterahocks (GoleneCskiy, eC al., 1973).
Depths of the Pribaykal~ye Earthquake Centersl
On the basis of the quite broad obaervations of the earthquakes of
Pribaykal'ye, it is posaible to state with certainty that their centers
are located in the earth's crust. However, the exact establishment of the
depths o� the centers within the.limits of the earth's crust encounters
great difficulties primarily as a result of insufficient density of the
seismic station network. As a rule, the depth of Che center of an -
individual earthquake with the existing network of seismic stations in
Pribaykal'ye cannot in the majority of cases be establiahed with the
necessary accuracy. Therefore it is necessary to be saCisfied with only
a few average eatimates. There are several paChs for obtaining such
estimateg. .
1. Comparison of Average Hodographs of the Head Waves P for Explosiona
and Earthquakea
By the observations of more than 20 industrial explosions from the areas
of Cheremkhovo and Zhele~nogorsk~ the apparent velocities and initial
orainates of the average hodographs of the head waves P were determined.
.
1The oreater part of the factual data for the given section was prepared
by E. A. Tret'yak.
. 226
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.
FOR OF~~CIAL U5~ nNLY
'Chey Curn~d ouC ed be equal Cn ?~9~h0~05 km/gec g~d 6~9+0~4 sec r~~p~ceively.
Th~ c~lGUlntion~ nf the hodogr$phe o~ thp ~ame wgv~e for tihp earthqu~kee
with nn intene~,ty of mor~ th~n 200 in v~ri,oue yereione (~.n particul~r,
for differenr parts nf the eeiemic xone) g~ve ~c~m~whet different values~
but valuee ~loee to thos~ that were obta~ned by rhe ~xplosione~ if we
conaider that th~ ~v~rage thicknees of ehe earth~g cru~t aiong th~ rout~~
in Pribayka'ye doeg not change ~h~rply according to the eeismologic dgC~
~nd th~ deep eeiemic eoUnding date, ehen the indicated cloeenese of th~
elemEnt~ megns thet the cer~t~re o~ the Qarthquakp~ are ehallow for the -
mnst parr (they ~re loc~ted in eh~ upper S to 10 kilnmeter layer).
2. The construction of the earthquake dietributiions wieh respect to depths
according to the formula for the travel time of the head waves ia
.
~p _ h~ , /'v""�'~~ e' -
p Mp vP
- Key: (1)
t. m~bn
or excluding the center time, b~ Che formulas for the differencea in tim~
of nrrival of the direct wave (P or S) and the head wave p:
.
~-p~ � + -(2N-l~, ~ ~ ~ e,
y~ ! ~--~p-~~
Pcp
" o~+~ i t e
S-1~~-, _(2N-la) z - Z -
s v~p Yp y-P~
where h is the desired depth of the center; VP is the mean velocity
mean
of the longitudinal waves in the earth's crust; Vp, Vg, VS are the known
propagation rates of the P, P and S waves; e is the epicentral distanceg
determined on establishment of the epicenter, H is the mean thicka~ess of
the crust in the region (N=38 km is given for the calculations).
The distributions obtained indicate the small mean depths of the centers
. and the very signiEicant dispersion of the results as a result of the
rnndom errors (~ig 79),
The cnlculations encompass the obaervations for January-June 1971 of the
enrthquakea from the varioue parts of Pribaykal'ye, The propagation routes
of the seiamic waves Were not differenti$ted in this case, ~uat as the
data from the individual etations aere not isolated.
227
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I
~OEt d~~~C~AL U3~ ANLY -
~/~~,~.r
0 �
.a~' ~
O O O
o o ~
A
""~"~~r~' � y~`' p ' C ~ ~ ~ l!1
. � ~ ~ as
. ~ � � p ~ x ,
. ~
o , ; . ~ a~ ~ a
I~h ` ~ ~
' ~ Y~ r~/ ? ~ V �O .~.~~r~.w ~
l~ ~ ~ , ~ ~O O f ~ ~
~ ~.ti~~ ~ ~
~w J ~
p ~
� O $ �
~ " .r
_ ~ n a
o ~ �
. ~ . . c~
~ � ~ , . a.
. . _
~ ~ ~ : f o_y,~ ~ ' ' ~ . o " ~ p ~
- , �r�v ~ iK O , ~ , ~ ~
M ~
~ ; ~ ; � ~ '�o b ~ o
. ,1 1 ~�~p O o~ ~
` �
. : ; ""'ti~ * ~ .ti : a� . ~ . ~ nr
~ ~ � ..a, r. } � a
� ~ �
. . .O ~ ~ ~ o � p .
� . +h. ~ ..r . ~ O ~ ~
~ . I. S
~ : . . i.~' G � '
� ~ ..o o . �
� � t O ~ ~
~ ~ ~ ~ ~ ~ ~
~ = t ~ ' ~ p ~ ~
~ '"�r� ~1 . CS., , ~ ~ ~ ~ ~
w.~+.. � d ~ ! M
' . 1f ~ ! O ~ ~ ~ .
� ~ ~ ~ O ~ ~
. ~ . p a
.
.
� i Q t ~
. ~
: : ; u
. ~
~ ~ .
ll~a~ . b ~ ~ : ' : d
. ~ ~ ~ ~ ~ � ' !
I~~~, 0. � ; ~
I ~ ~ ~ ~
i ; .
C� ~ ' u
1 .
� d
F , o� ~ -
~
� o
O , o ~ co -
l = � o o o :
~ p ~ 's
~ ~ ~ v~
- ` ~ . . . ~ ~ J t
t+1 ~ ' ~ a
pO '~1+w~~) ~.e;~
. , O O ~ ( .~t ~ O.
, ' q ~ -
A~'~'~ O
. ~ ~
. ~
_ Figure 75. Earthquake epicenter denaity mep for 1962-1971 vith R~9.
228
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~Key Cn ~ig,75, Pp 228-229~; ,
1-- Uda; 2-- Iy~; 3-- Oka; 4-- Irkutek; 5--� Lake Kaeogol ;
6-- Orkhon; 7-- Selenga; 8-- Khamgr-Daban ltidge; 9-- Ul~n-Ude;
10 Ulan-Burggey ridge; 11 Primor~kiy ridge; 12 Angara;
13 Norrh~rn ~~yk~1 Highlgnd; 14 Lena; 15 Angar~kiy ridg~y
16 Virim; 17 Delyun-Urgnekiy ridg~; 18 Kodar ridge;
_ 19 Udokan ridgp; 20 Baykgl'~kiy ridge; 21 Uda; 22 V~,Cimskoye;
2~ plo~kogor'ye; 24 Khilolc; 25 Chikoy; 26 Y~blonovyy ridge;
27 bnnn; 2g Ol~~g; 29 0lekmingkiy; 30 Sianovik;
31 Shilka; 32 Gaximur; 33 NErchinakiy ridge; 34 Argun';
35 MNR; 36 KNtt
3. ConeCruction of th~ dieCributione bgsed on observationg of the
- rravel time of the head wgves Co the individual gC~tione, as in the
preceding iCem, but using more eubetantiated values of the mean Cl~icknese
nf the crueC with respect to the deep seismic sounding profile of the
Central 8aykal to the Barguzinekaya basin~
The htsto3rams conetructed by the data for 1962 to the middle of 1972
(~ig 80) are similar tn the graphs from the precding item.
Obviously,' the greateet accuracy in eatimating the depth of the center
c~n be achieved by uaing the known values of the thickneas of the cruet
(for example, according to the deep aeismic sounding data) and observa-
tiong of the wavea reflecCed from the top of ite foot. These estimateg
of the depths of the centere turned out to be possible for the ~fterahock
of the Central Baykal earthqrjake of 1959 for which in many cases reflected
transverse wavea were recoraed at the seismic atation of Bayanday, and
in the region cloae to it where the wave reflection pointe were located,
an independent determination of the thickness of the earrh's crust was
made by the deep seismic sounding procedure. The calculation of the
depth of the centera h were performed in the given case on Che baeis of
the exprnssion
(2!1' - h)' ~s ~ rV r3t v~ Y~,
~ Y"9 ,
Where V is the mean velocity of the reflectsd wave in the earth's crust,
dt :s t~ie difference in timee of arrival of the reflected and direct
wnvea. Th~ results of the calculations Were �ormed by the histogram
(see fig e), and they ~ndicate that the depth of the aftershocks
oE the Central Baykal earthquatke of 1959 i.s quite shallow.
229-230
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_ FOR OF~ICYAL USE ONLY
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q
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- 231
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232
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- 233 -
FOR OFFICIAL USE ONLY
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t~01t O~~ICIAL U5~ ONLY
n
I~0
~
I~0
n ~
100 !00
~
90 �
90 60
~-P S-P ~ =p
so sn
_ ,ra
,
-SO -A~ 0 0 60 ~ 0 -AD 0 PO 60 c'0 p 0 6O A~KM
; Figure 79. Earthquake distribution in Pribaylcal'ye according to
, center deptha h ueing the differences in ti~mes of
arrival of the P and (S) wavee and the head Waves P ~
and abaolute travel times of the head wavee P(tP)
at individual atatione, n is the number of cases.
4. The calculations of the deptha of the centers of the earthquakes (along
with the establiahment of their epicenters) by the observations of the
direct waves in the presence of a seismic station at a short epicenCral
distance (,10 Wn). A similar rare possibility occurred, for example,
when studying the a�te~~rahocks of the Uat'-Muya earthquak~ of 1968. The
calculationa performed on the computer on the basZs of r~inimizing the
~ eums of the aquares of the errora in the travel times led to the inclusion
of shallaw depths more 0.5 km than 6-10 lan.
The distribution of the ehocks of the Ust'-Nuya earthquake of 1968 with
respect to depth is preaented below;
Depth of center Waves
h+ ~ used
S P
� ~ 5 12
S 2 3
10 4 1
15 0 0 -
_ 5. The eatabliahment of the total statistical distribution of the depths
of the centers of the entire B$ykal zone by the obae*vations of the direct
wavea at the seismic statione wtth epicentral distances to SO l~ (for the
defined, fixed poaitiona of the epicenter and values of the center time)
from the center-epicenter-station right triangle.
234
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~01t n~t~ICtAL US~ ONLY
n ~ + ,
60 ~
, n 60 '
~tl ' ~0
d?0
JO JD
TiIPNM r0 .
~1~ YeN.?~?CZ'
-~D -?0 80 ~D 60 -~0 ~d 0 p0 ~0 h,nM .
- 6owMBs,i '
n ~o C3,
. " '
c po soaoN (Sj d po Q po
f0 6ep~y~~M~ 6 ~ !0 Awn~r '
(4) ~o
-40 - 20 ~0 -~0 PO 20 ~O -!0 0 PO h,K~
Figure 80. Earrhquake diatribution with respect to depths.
a-d by the obeervaCions of Che longitudinal head wavea P~
e-- by reflected tranaverse waves
Key:
1. Tyrgan; 2. Uakit; 3. Bayanday; 4. Alla; 5. Bodon; 6. Barguzin
As an example of the distribution we can use the histogram constructed by
952 depth determinations for 1967 (Fig 81). The histograms for the other
time periods differ somewhat with respect to external appearance; however,
fcr all of them g large number of cases of determin'.ng the imaginary depth
of the center and Wide range of variation of it are characteristic. This
is n~tural if the actual depths are ahallow (a few kilometers), and the
accuracy of the individual deCerminations is low, which actually occurred.
6. Use of macroseismic data for strongest earthquakea.
An estimate of the center depths was made for the ten strongest earthquakes
of Pribayka2'ye by the rreviously constructed isoseismal maps. The
calculntions were performed on the basis of the known macro$eismic formulas '
(N. V. Shebalin~ 1968) using the numerical parameters both specially
determined for Pribaykal'ye and averaged over the various seismically active
regiona. According t~ theae calculations, the centers of the quite strong
earthquakea can aleo be located at ahallow depths (to 10--15 km), but as
n result of low reliability of determinations only auxiliary significance
can be attached to them. The only reeult in this case indicatea significant
deptf~s, but they do not find confirmation from any other seismologic -
observationa.
235
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~oR o~ic~ai, us~ o~~r
n
~d
~o
_ ~
I
t ao ,ro ~+v ,o o "
!0 20 JO l,~ , ~
Figure 81. The dietrihution of the dppthg of renterg of
Prib~ykal'ye earthquakes in 1967 in ~ccordance
with the o6gervatione of the S v~ves
(n ig the number of deCerminations)
Sunnning up everything that has been eaid abov~, it must be recognized th~t
on the modern level of underetanding of earthqnakes in Prib~ykal'ye, the
depth~ of the centers of the me~ority of them ~wpak, cnn~tantly recorded
_ eArthquAkes) can be congidered to be shellov, that ig to gay, provieionally
equal to -5 km. The correctness af thia aesumption i~ confirmed, i~n particu-
lar, by the fact th~t at thia depth of center, the estimatea of the cruat
thickness mgde by the observations of the reflected ~+aves during the earth-
quakes agree in a number of areas of Pribaykal'ye aith the data obtained by
deep seiamic soundinge. The conclu~ion of the ahallow depths of the centera
also ~:,grees aith the results of the modern etudies of the seiemicity of
other rift zonee, for exemple, the Eaet African rift in Kenya (Molnar,
Agaewae, 1971), the Central Atlantic, ~n Iceland (i~iard, et al., 1969).
This, c~f courae, does not mean that there can be no smaller number of earth-
quakes With deeper centers in Pribaykal'ye. It is possible~ for examnle,
that the Kodar earthquakEa of 1970 aere somewhat deeper. On the Whole, in
solving the problems of eatimating the depths of the centers it is necessary
to find additional patha~ in particular, obviously it is necessary to con-
gider rhe posaibilitiee of the diacovery of the type pP (sS) waves at amall
epicentrnl dis[ances,
Recurrence Rate of the Pribaykal'ye Earthquakes
The averdge recurrence ratca of the earthquakes of different force !s one of
the moAt important characterietics of the seismic condition. It is of
interest to study the average recurrence rate of the earthquakes both in
all oE Pribaykal'ye and in individual sections of it isolated with respect
to aeismic or other eigna. Por this purpose, a number of linear recurrence
rate graphs were calculated by the earthquake catalog data for Pribaykal'ye
236
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~o~ ~~~tcr~t, us~ ortt.Y
in recent ~?eare (the ldgari~hm d~ ~he number of ~arthqugk~g n~ ehp
~arregpc~nding ~nprgy ag d fun~tinn d~ th~ iagariehm ~f eh~ ~n~rg~+)+
'Ch~ r~~uit~ o# tl~~ ~~~~u1~t~on~ p~rform~d by eh~ i~~~t ~qu~r~g mpeh~d er~
pr~~~nt~ed in ~~bip 13. ~3,~ ~2 ~hoa~ eh~ ~r~~g fnr whi~h th~ ~gl~ulation~
wer~ med~. '~h~ ~npr$y eia~~~~ of eh~ e~rehquak~~ K in ~11 G~~~~ a~re
de~errninpd u~ing th~ known 'C~ G. ttgutian namogr~nr by thp ~b~~rvgtion~ nf
th~ ~~igmiG ge~tion n~twor~C for ~ribayk~l'y~.
`Che mn~c important paramee~r of th~ r~curr~ncp rate ~r~ph it~ ~ngular
eo~f Eiei~nt Y-- fdt~ 1~rg~ ar~~s (A11 ef Priba~yk~i ~ye, ehp rift rp~ic~n)
i~ d~te~mined quie~ etably, and it~ numeri~al value (-O.S) eurn~ ~ut td bp
~clo~~ ea eh~ ~ver~$p for th~ other regions. Mor~ov~r, fnr individu~l
p~rtg di th~ regidng ehe va1u~ of eh~ angul~r coeffieipnt~ dtff~r nnti~e-
ably, indi~~Cing the knds~m nonunifermity of rhe geiami~ pra~~gs. `Thig
be~ing to bp ehown ~lready nn c~mparison of th~ two ~rbier~rily ~elected
halveg nf ehe rift rpgion; northea~tprn ~nd gouthwe~tern, th~ b~und~ry
betW~~n ~rhich p~s~es along the meridian b~tw~~tt ehe 5vy~edy No~ Peningul~
~nd che ~arguzingkiy ridg~ and glong the pera11e1 north of the U~hkgn'i
I~land~. Now~ver, h~re the differ~nc~ i~ aithin rhe limits of pngaible
error: the an~ular coefficipnt is higher in the norrh~astern thgn in th~
gourhNeatern part of th~ rift znne. Making th~ trattaition to gm~ller
regiong, entirely definpd difference~ are detect~d. Thug, in the vieinity
of the 5elenga River delta and the adjacent parCs of B~yk~l, rh~ ~ngulgr
cd~fficient ia reduce (�-0.4).
_ bbviously, the angular coefficie~t of the recurrence rate graph in the
vicinity of thp Tunkinakiy basins and the southeastern part of ~astern
5ayan is low. This lowneas, hoWever, is less defined, for When calculating
the angular coefficientg for the last S years (1967-1971) ie is true that
by ~ smaller number of obs~rvations it was not a loW value that was
obtained but a high one (--0.62, ocrdinate for K=10 equal to 0.3). Hawever,
this recurrence rate graph doe~ not agr~e aith the facts knoWn for this
region inasmuch as then it would be necessary to expect repetitions of
earthquakes of the 14th energy claes every 100 years, the 16th class every
1500 years, and so an. According to the actual data, earthquakes of
�16th class occurred in the region in the 19th century and in che roiddle
oE the 20th century. The recurrence rate graph with smaller angle of
inclination (see Table 13) agrees better with these facts. The high values
for the coefficients Were obtained for the local r~gion in the central
part of the Ikatskiy ridge (the long-lasting Ikatskiy earthquake sWarm).
It iR interesting that for the seriea of aftershocrs of the Mogodskr~ya
19fi1~ Tas~Yuryakh 1967 and Kodar 1970 earthquakes the angular coefficient
of the recurrence rate graph has an entirely normal value close to the '
menn for the zone. The reaults �or the earthquake aWarm on the northern
part of the BarRuzinskiy ridRe (the end of 1966 to the beginning of 1967)
nr~ scattered~ In this c4se the very las~ value of the angular coefficient
is determined~ but it is necessary to note that this conclusion is
obtained by the least number of obaervations and its insufficiently high
ob~ectivity is not excluded.
237
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~d~ h~~�ic~nL us~ ot~,~r
~
r~
�is ,~i ~
~
~
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. r ~
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.
. ~ ' ?i " ~ L:J~
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j ~ j , ~o~Q=' ~ ~ a` ~b)
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:~4~ ;;1 9~ Y~ Qe~' o r'~'"
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~ .
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, ,
. c,~'~~(1 14 r
_ (16) ~1 .
r J vf
ti.'f` .
~ i
(
Figure 82. 5chematic of the regions of calculation of the
earthquake recurrence rate grapha. Th~ numbers
correepond to the numberg of the regiona in Tabl,e 13.
Key:
1. Irkut; 2. Irkutek; 3. Oka; 4. Ang~ra; S. Vitim; 6. Olekma; ,
7.�Tungur; 8. K~?rengn; 9. Nercha; 10. Shilka; 11. Argun';12. Lena;
13. Chita; 14. tngoda; 15. Onon; 16. Xhilok; 17. U~an-Ude;
18. Selenga
~t is knoWn that the difference in angular coefficients of the recurrence
_ rgte graphs can be connected aith a difference in properties of the
destroyed medium.
On destruction of leas unifora~, fractuxed material, higher values of this
coefficient are detected~ Posaibly~ the med~um in the vicinity of the
Selenga River delta, in the regio~n of the Upper Muya-~Muyakan basins:and ~
to some degree in Central Baykal and obviouely in the Tunkinskiy basins,
i~ characterized by some+ihat d~fferent distinguiehing propertie8 by com-
p~rieon, for example, aith the wici~ity of the Barguzinakaya baein and
the Berguzinekiy ridge. Let us note that in all of the enumerated
- regione with loa value of the angular coefficient of the recurrence rate
238
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-
~ox n~~rcinL vs~ o~t,Y -
~raph ~1r~~dy durin~ th~ hi~tdr3,~ p~ridd, ~trong ~~rehqu~k~~ oeeurr~d,
bue eogether with them the number o~ af~~r~hoek~ ~~e~r eh~ ~i~nific~trt
~ho~k aa~ o.ften v~ry great~ Thig probl~m, how~vQ~r, i~ noe ~impl~, for
ehr~ deppnd~n~e o~ Y~1go on eh~ d~f~t~natidn ratp ie pd~~ibi~ (with an
iner~~~e in rat~ th~ v~1ue o� Y d~~reae~~~,
The r~~ult~ o~ ehp ~~leuigeinn~ by the r~curr~n~~ r~tp graphg obtained
forth~ m~an ine~rv~1~ b~tw~en thp ~~rrhquake~ of rh~ highest c1~es~e
(~Qe Tab1e 13) can of cour~~ hav~ only approxi,:natp significancp inaemuch
chey ~~re ab~~ined with ~i$nificant ~xtrap~lation of th~ ~uppo~poly
lin~ar fun~ti~n ~nd und~r eh~ ~~nditinn that ~he eei~mic pr~~~~~ i~
~t~bl~, th~t i~, it i~ correcely d~g~rib~d by the nbgervations in rpc~nt
y~~r~. t~oW~ver, compari~on of rh~m With the hi~toric informati~n (thp
la~t d~c~d~s ~nd 100 tn 200 years~ on thp stron~ e~rthquak~g af
p~ribaykgl'ye not used in the calculation~ indicaee~ thnt th~y da not
contrec~icr th~ge data. Anoth~r reason in favor of eh~ pog~ibiliey of
~uch approxim~t~ ~s~eimgepe ~s th~ ~gct of ~~tiafactory agr~~o~nr with th~
recurrence rate graph con~tructed for the rifC zon~ by th~ in~trum~nt
information (Fig 83), th~ data on th~ pgleo~elamodislocationg obtained
Eor syet~metic aeiemogeological etudiee in this region.
The summary of the pal~oeeigmodisldrationg giv~s the following distributian
of their number:
~orce 12 11~12 11 lt?-11 lb 9-~10 9 8-9
No of Qarthquakes 2 1 3 1 41 8 17 1
The indicated data referred to a aignificantly longer time. It is of
course impossible exactly to pstabliah the ti.me tnterv~l which these
data repre$ent. Beginning with the eeiamogeological ~igns, it is poseible
to estimate it approximately at a thousand year$.
,
Obviougly, the earthquakes of 16th class (force 9) for this time period
turn out to~be already nonrepresetative: information about them is
incomplet~. The initial data gre plotted on the graph (see Fig 83) also
under the aseumption that the encompassed time p~riod is tWice as great
(equ~l to 2000 yeara), which i9 not excluded. Here, someWhat better
agreement With the continuation of the recurrence rate of the graph ia
detected. On the whole, it is necessary to recognixe th~t the number of
known paleoseismodislocations agrees entirely satisfactorily with the ~
cnlculated recurrence rate graph for the data of this type. A similar
picture is aleo observed in the cese Where the investigation Was performed
not fer the enti,re zonp but for the northe$stern and southaestern halvea
of it geparately.
i
239
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~UR O~~~CIAL US~ ONLY
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263
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~OEt n~'~ICIAL U~~ ONLY
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~Oit d~~ICIAL US~ ONLY ,
Le is pn~gibl~, hnw+~v~r~ eo ehink ehee rh~ ~.ndi~~eed inc~eage in '~c~lc ig
~m~ll. Strang ~e~rChqu~keg ~re qUite r~r~ (~nd only Ch~y e~n giv~ eh~
rorr~~ponding hu~ki.ng ~t the di.~rances)~ ~n any ca~e, when cglculeting
TC~~~ f~r forc~ 5 and high~r in Irkut~k the ~trip betiw~en eh~ par~11~1~
df 44 and 4B� noreh laeitude and 51 to 96� ~agt longiCud~ 1ncaCed to eh~ _
gouth drnpppd nut of rh~ inv~st3gation. Analogou~ly, f~r K~b~n~k, -
~imilgr sCrip~ wer~ between 44 and 48� noreh 1~tiCud~ ~nd the meridigne
nf 93.5 nnd 98� east lengirude~
In p~rticular, this can exp~ain the tecC thgt ~egLe for Irkuegk (7 y~~rg)
turn~ out to be gr~at~r ehan To~g ~4 y~are), glthough oeher caue~~, ~bove
~11, ehe ~r.rorg in d~t~rm~nations, gre pdsgibl~ here~ The differenc~ far
force 6 in T~b1e 17 fnr irkut~k (20 ~nd 40 y~arg) can easily occur a~
_ n result of the errors in psCimating th~ force of Ch~ individugl earCh-
quakeg. On th~ other hand, Tob~ for rhe earthqual:es with force 5 in
- Kabanak perhape turned ouC to b~ high~r by compar3son with Tcalc if
cprtain shocke are not taken inCo accounC for thp inveatigated interval.
According to Table 17, the quake~ of force 7 and higher in Irkutsk must
be very rare, end force ~ and higher, in practice, are absent in general.
However, ~udging by the historical information, it is pogsible to think
ChnC over the last 250 years up to 3 force 8 earthquakes have been
observed in Zrkutsk in 19742, 1829 and 1862. This somewhat reaembles
the regultg obtained for Taehkent (Zakharova, Seyduzova, 19~1) and it ig
possibly explained by the fact that the calculation for the high force -
earttiquakea ia unreliable in the given case. On the maps of the higher
force seismic vulnerability Irkutak is in the marginal zone. However,
probably thia is caused by other reasons, above all, failure to conaider
the peculiarities of Che damping of the quakes in this case. It should
not be ~orgotten thaC the performed calculations of the seismic vulnerabil-
ity in Pribaykal'ye are the firat effort; they do not pretend to Che final
= solution of the problem and must be aiven in more detail and more precisely
defined hereafter (in particular, it ia necessary to consider the peculiar-
- ities of the damping of the quakes under various conditions, and more pre-
cisely to specify the variations of the graphs of the recurrence rate with
respect to area). Therefore the estimates obtained for the seismic vulner-
ability are expediently used more for conclusions of a general nature but
not for detailed conclusions as applied to the local areas.
Discussin~ the accuracy o~ the calculated estimates of the seismic vulner-
ability, it is necessary to note that an error of 1.5~2 times is entirely
possible here (Riznf,chenko, Zakharova~ Seyduzova, 1969; Zakharova,
Seydua~va, 1911; Fedotov; Shumilina, 1971~ Dzhibladze, Riznichenko, 1973).
The seismic vulnerahility depends linearly on rhe seismic activity~ that
is, on vari,at~.on of the sei.smic activity everywhere in the zone by two
times. the vulnerability also varies by two times.
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l t 1 4
Th~ num~ri~al v~lu~~1'of th~ vuin~rab~.lity obtain~d �or Prtb~yk~i'y~ ~r~
comp~rabl~ to Ch~ r~~ultg knnwn for oeh~tr regidns~ Similar reaulta h~v~
be~n obtained ~arli,~r for Italy (~ti~nichenko~ pr n1~, 19~0), ~nd gom~wha?:
l~w~r or th~ eame vuln~rability tg cha~acteri,etic of ~e~tern Uzb~kigean ~
(Zakhsrova and S~yduznvg, 1971) and Ceorgi~ (D~hibladze, ~tixnichenko,
1973)~ Th~ luw~r vuln~rability of the Crim~an r~gions (Riznichenko,
Bun~, et a1., 196~) nnd thp Carp~thian xone (brumy~, Popov, St~panenko,
1971; Urumya, Popov, Resh~tnikov, St~panenko, 1971~ than in Prib~ykal'ye,
end higher vulnerability in Kamchatka (~edotov, ShumiLina~ 1971) ig
entirely natural, however, Ch~ ~xce88 is not ~o great as cou18 b~ ~xp~ceed
at first gl~nce. The calculations of the aeiemi.c vulnerability ehus
d~termine the place of Pribaykal~ye with r~gpecC ta th~ degree of geigmic
d~nger among other regions of the Soviet Union.
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CHAPTER X. ~A1tTHQUAK~ FOR~CASTING
Peculiarities of Che bevelopment of Che Seismic Process by the Observation~
of Weak Earthquakea (in ConnecCiott with the Search for Diagnostic
Attributes of Stxong Earthquakes)
In nature thQre are aets of earthquakes, about which there ia tio doubt
that they belong to a single center zone; foreshocks and aftershocka.
The intermediate poaiCion (if it is posaible to call it that) between the
- "independent" and "related" earChquakea ia occupied by awarms and groupa
of earthquakea combined by a defined commonneas of territory (space)
and, obviously, somehow interconnected in time.
The invegtiga2ion of the apace-ti~e laws in the distribution of seta of
~ earthquakea ia of unquestioned interest, for during the course of the
investigationa it is possible to obtain data on the peculiarities of the
development of the seismic procesa.
Thus, the atudy of the nature of the manifestation of the aftershock
activity provides information about the development of the process in
the center, the dimenaions and configurations of the center zone. The
analysis of the geographic distribution of the ahocks in the awarms and
groups permita esCimates to be made of the effect of one earthquake on
another; the tim~: apace analysis of the distribution of the weak earth-
quakes ia of interest for studying the process of the preparation of a
strong earthquake, and so on. The results are presented below from studies
_ of the enumerated and certain other aspects of the seismic process in the
Baykal seismically active zone performed to discover the possibility of
- estimating the occurrence of strong earthquakes.
The basis for the investigations is the data on the 2500 earthquakes
with K38 recorded by the Pribaykal network of stations in 1965-1968.
- In addition, it turned out to he possible to ~.nveatigate the seismic
conditions of r~�~ regt,on of the center of 20 strong earthquakes (rt>5)
and one signifi.cant fflrm occurring in the zone for the 1959~1968 period
(Table 18). Aa a rule, the energy estimates for strong earthquakes were
real�'L~ed by the known relations between K and M derived by T~ G. Rautian,
the application of which is entirely adm3~sible for Pribaykal'ye
(see Chapter VI). �
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~o~ o~xicini, us~ orn.Y
Th~ ebe~rvation~ indi,cat~ th~C for Che earehquakes of inedium strength
(~t to 5) the coord3nateg of the a�e~r~hock~ ~nd eh~ b~~iC ghdCk grp
indi,etingu~eh~ble withi,n the 13mi,tg of accuracy o� th~ obgervations. ~
Wieh en incre~e~ in energy o.f th~ main e~rthquake, the area occupied by
the afterehocke increngee~ Ueually in ~ribaykal'y~ areae of the aftpr-
ehock zonee have elongated ahape; eom~timee the eric~ntera of the -
repeared shocke are elongated 3,n chains.
As a rule, in the areas of "normal" seiamic conditione the earthqunke
dietribution in space and in time followa the Poiseon diatribution, that
is, each earthquake ie a random independent evenC. '~he deviations, ~g
wae demonstrated by varioue researchers~ are connect~d with th~ occurrenre
of afCerehocks, ewarme and groupa of earthquakes. By the grouping
phenomanon we mean Che slgnificant deviation of the distribuCion of the
ahockg in time from Poisson in areas characterized by a constant mean
recurrence rate of earthquakes and not connected with the afterehocks and
awarma of earthquakes (Borovik, 1972). In order to �ind the shoclcs making
up the group, it ia nece9sary to select the critical values~of the size
of the region and the time interval, falling into which will indicate
- grouping of the_shock. The radius o� this region would be logically given
as equal to the radius of the center of the earChquake. However, for
- earthquakee of energy class 8~13 in Pribaykal~ye the poasible errora in
determining the coordinates of the centere are appreciably greater than _
their dimenaiona. There~ore the radius of the area of nossible grouping
was taken equal to 30 km. The calculation of the time criterion of. the
grouping reduced to finding the time interval such that the probability
of appearance within Che limita of this interval of one or more shocks is
equal to a defined given low probability, in the given case P=0.005,
for the correaponding average number of shocks for the grouping area.
For Pribaykal'ye, the graups include shocka occurring an area of 2800 km2
and aeparated by time interval of leas than 0.35 days. During a single
test, the random realization o� the event with the probability of 0.005
is in practice imposaible. However, when isolating group e~rthquakes,
we make not one test, but can accidentally havQ some number of eo-called
false groups. In Pribaykal'ye, excluding the falae groupa, 18.2~ of
the earthquakes belong to the groups.
Groups were isolated with values of the probability from 0.001 to 0.07
(see Fig 93). The results are the most stable for the probabilities of
0.005 to 0.01 which is expedient to use in practice. Now let us return
to the dependence of the grouping effect on the dimensions of the area.
- The following aizes o~ the areas were selected 80, 314~ 1200, 7800
and 2X105 kmz. For each case $ study was made of the number of true
Rroups and the group~ng eoefficient X~--, the ratio of the number of
group earthquakes to the total number~ The grouping coefficient increases
with a decrease in size of the grouping area until inaccuracy begins to
be felt in determ~n3ng the position of the epicenters, that is, when
isolating the g,roup earthquakes it is possible to use any value of the
grouping area not exceeding 3Q00 km2.
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~Ott O~~ICYAL U5~ ONtY
`~~b1~ i~
D~t~ on the S~qupncee of ~tep~a~~d Shnck~ o~ prib~ykgl~ye
Earthquai:~~ ~n 1959~1968
' ~ 2
.
~ N~�~ ~ ~ ~a~+ 0~ wr~ N ttprrev~ru (3)
~ .
~91Vllt i9S9 52~8 lOT~~ 61/~ 80 l800 >4000 ~ a21 .
fllXi f~62 bb~9 :fia,2 8 ~ AO f2pp ; 33pp !~9 ~
80IVii1 f988 bf~7 f0i,b i W/~ 1 Zb f. "~~ppp ; b'~p �~~~4)
, , ' ~ lW
~
~ ' { gltt 1tu0
BflVtti i988 ~8~4 fib,8 (i~ (f3p) (2ppp) 87
f3/V11t l982 b3~7 f09,5 5~/~ ~,~80p~ ~pp ~
221t l98Z~ b2~4 f00~3 . 511~~ ' - , 8
28?Xi f9E8 55~9 lff~5 5~8 !8 (gp) (app-41,p) 4
f111I f98~ 52,0 l08,~ b~/~ (~b) ~ _ ~ , 3 -
31?XI1 l988 55~8 fiO,B ~?b � ' gpp ~pp 383 Poi} ~e?ur (5)
, ~ ' TQIItl~
l51I f98~ 55~8 ff0~8 ~ 5~/~ _ _
lOllt l983 52~8 'f08,8 5 f5 , 90 750 9 -
2f/VlI 198g SS,2 1f3~4 S f8 80 (85p) 89
. l1X11 f983 b5,9 1fZ,0 ~~/~-S . ~p ~pp~ ~ (f000) 6
251Vt l98i SZ,4 t08,5 4~/~-b 5 _ 2�
271Vt1 !98! 54,i ff0~0 4~/~ ~ _ _ 5
8/1 l983 5f~3 f0t~9 4~/~ f0 (Sp) ~ - 3
ff/X11 fo84 52,4 ~f08~3 .41J~ fS - 4
~ 911 i98.3 5~~7 !!!,8 4 i0 (70) - 2
fIVII f942 5f~7 f0f~9 3~/~-~ f2 - - 3
lOIX f963 Sf,B fOS~f 5'- - g~
Key:
1. Date
2. Coordinates
3. Notes
4. I'or determination of S there are few data.
5. Earthquake swarm
Note. 1. n ia the number of shocka in the series considered during
procesaing; R is the extent of the a�terahock zone; S is the
area of the a�terahock zone; Q are the dimensions of the region
of preparation of the earthquake. ~2. The values of M were taken
from the sei,amologic bulletin of the seismic station network of
the USSR and the collect~,ons on "Earthquakes in the USSR."
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Y
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Pravi,ou~ly it has alree~dy b~en pe~,nted out thgt rhe groupg, ~ust ae the
~e~~,es o� afterehocke belong to the lo~g1 aete of interconnected events.
'~he aftexshocke are related by commonnese o� ~he area, in groupa thia
rpl~Cion 3e expreeaed by the e�gect of the centere thar are cloae to each
nther. IC ie poesible to define the limita of this e�fect approximaeely. -
In~ide each set of group earthquakes 3solated for varioua values of the
grduping area, a atudy ia made of tHe $roup diatribution with reapect to
the maximum ~istance beCween ehocks in each individual group. In addition,
the earChquakes of which energy, clasaea consCiCure a group was taken
inCo accounC. I'or this purpose, the difference (K1~KmaX) was determined,
where K1 is Che energy clase of the firet ahock in the group, ICmax is the
maximum ~nergy clasa noted in the given group~ From ehe comparison it
follows ChaC groupa are moet frequently encountered with a apacing
between the most remote ehocks not exceeding 10 km, that is, the mutual
effect of Che centers of the weak earthquakes appears at this distance.
A more detailed analysis, un�ortunately, is impossible, �or the epicentral
region of the earthquake center of the 8th to llth energy classes is
smaller than the region of poaeible poaition of the epicenter.
Therefore, for the Pribaykal seismic zone data wer.e obtained on the
extent of the regiona, within the ?imits of ~vhich the centers of the group
earthquakea are locaCed and the linear dimensions of the center zones of
the atrong earthquakes have also been approximately determined. There-
fore hereafter it turned out to be possible to perform the studies of the
seismic conditiona in the regions occupied by the centers of the strong ~
earChquakea before the occurrence of the earthquake and after it. The
study was made by the following diagram: 1) a study was made of the
earthquake distribution over a si~nificant area, including the future
center of the strong earthquake long before its occurrence; 2) the epi-
central zone of the isolated region was investigated during the period of
- maximum activity of aftershocka~; 3) the development of the seismic process
in the isolated zone after the end of Che series of aftershocks was
traced; 4) the discovered epicentral fields were compared.
The titn~ intervals during which a study was made of the space-time
distribution of the earthquakes before and after the occurrence of the
series of aftershocks were selected usually the same, lasting several
years, sometimes months, depending on the quality and quantity of the initial
data, the density of the epicenters at the given point and the strength -
of the earthquake.
The series of. aftershocks of the Central Baykal earthquake of 29 August 1969 -
(M=6-3/4) are presented ~,n ~i,g 94 as an ~,llustration of the processing.
Tl~e distribution of the representative earthquakes in the vicinity of
Central Baykal for the periods of 1 January 1952 to 29 August 1959 is
presented in Fig 94~ a; the per~.od o� maximum activity of~the aftershocks
(29 August 1959 to 30 June 1964~ is presented in Fig 94, b. From July 1964
(Fig 94, c), the activi,ty o~ the aftershock zone in practice compsred with
the average activity of the region. The region of reduced seismic activity -
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^m.,t ' /~ln~ n"'�* Jn
~
�
,i~~ ~n ~1~ . ~~~n ~1~
!00 ~ ~~~~uem !0 / n ~2~
i ~ ucm
~2? o .
~l~J~~ ~J~~~r �
, nm, J ~~n.s
i ^c
,
!0 ~ ~ ~n/
~ ~ n~ ~ / ~
SO ~uem ~'''".r 'I.' nucm ~2~
nA ~J~J~J~
o `"^1 o 000 o P
0 00�, ~ o o~o o`
o o' o 0 0 0~ o
Figure 93. Grouping of weak earthquakes for various values
~ of the probability of random occurrence of an event.
n~ is the total number of isolated groups; ntrue is the number
of true groups; n is the number of f alse groups; m is the
- number of groups ~.the numbers 2, 3, 4,~5 are the number of
shocks in the group)
- Key:
1. nR
2� ntrue -
isolated when comparing the epicenter maps (see Fig 94, d) including the
center of the earthquake, has an area on the order of 4000 km2. Let
us note its "region of preparation." The sizes of this region exceed
by approximately two times the area of the aftershock zone. ]:t is true
that in the northeast the boundary is drawn uncertainly as a result of
the absence of data. For comparison, a region is isolated (see Fig 95, a),
the area of which was selected for convenience equal to the area of the
preparation region. ~
The data on the variation o~ the activity in the region of preparation
of the earthquake and the ad~acent compaxison region are presented in :
Fig 95 (the number of observat~,ons ~,s plotted on the y-axist and the _
observation time on the x-ax3,s). As is o~iv~ous, the "period of quiet"
o.f the prepa,ration region lasted at least 7 years; at the same time in
the surround~ng areas the backgxaund of se~.smic activity in practice
did not change.
273 .
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~Oit 0l~I~ ICIAL U,~~; .O~yLY
1~� ~ f,~e
~ / 6
~ % t
~ i ~ ~
/
~ � � ?~i V i
1 ~ / /
� ~ X / \
1./G ,~i .
�1 i~ ~ � ~l
~ ~ /
Ir~
:4 ~ , y B~'~J1~~' + _
% 6~ � ~ ~ r1/ ~ M??/~f
~~1~ ~ ~ .
� �
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~ ~ � o ' o
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C~~~~~ ~ � ~a~2, .
.
J~~
101 � pg� s jpS� 709�
�
A 2 ; ~ ~:3,`j
~ ~ ~ I -
i
~~K ' ~ / -
~a o
~~?h
_ S1~ ~ J.!� ~i~7~� ~
/ / \
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6 ~ ~ ~ /
/ ~
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. o tio
i~ i~
C~� (2) ~~r
JI ~ S!
J09' JOS' ~py
Figure 94. Analysis of the enicentral field in the vicinity
of Central Baykal by the data on earthquakes
with K;10 for 1952-1970
a-- epicentral fie:d of the region for Che period from
1 January 1952 to 29 August 1959; b-- epicentral f.ield of the
region for the pQriod from 29 August 1959 to 31 becember 19Ci0;
c-- epicentral field of the xegion ~or the ~eriod from
1 Januazy 1961 to 30 June 1964; d eoicentral field of the
region for the period ~rom 1 July 1964 to 31 December 1970.
1~~ limit of the investigated regi,ont 2-- epicenters of the
earthquakes with K~10~ 3.M- boundaxy of th, aftershock zone.
[iey :
1. Lake Baykal; 2~ Selenga River.
274
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I~'Ult (tt~ I~ iC t A~~ titit~. f1Ni~Y
s~�
a / -
6
~ '
. _ . ~n�aI
^
' ~ i 2 ~ ~f~o ~ 10
~ 3 � r? ~t-
~4 ~ %
/
~
~ ~ i~ -
~ ~o
.
:
~ ~ , ,
t �
CEr~ ~ ~ ; ~ ~
\ A f~1 1 ~ ~ ' ~
1 ~ ~ ~
_ ~ ~I ~i 11 ~ ~
�
!J ~q� ~ p~s l960 ~965 l970
' T,toda ~3~
Figure 95. Seismic conditions within the limits of the region
- occupied by the center of the earthquake of -
29 August 1959
_ a-- afterahock zone, region of preparation of the earthquake
and region of comp~rison: 1-- boundary of the aftershock zone,
2-- boundary of the preparation region, 3-- comparison .
region; b-- development of the seismic proceas in time in
the region of preparation of the earthquake (the solid line)
and Che repion of comparison (dashed line)
Key:
1. Lake Baykal
2. Selen~a
3. T, years
The series of aftershocks o~ 12 etrong earthquakes in I959-1968 were
r.rocessed by the sante scheme. The results were found to be analogous,
- that is, it is possible to propose that a strong earthquake is preceded
by ~ prolonged preparation process which develops within the limits of
the significant area (Borovik, 1971). .
The preparation regions have been isolated most reliably for earthquakes
wi tti magnitude t4=5-1/2 and more.
Thus, for Pribaykal~ye, the pzenazat~on region of an earth~uake of defined
magnitude can be characteri.zed hy the parameters~ Q, TQ, nQ, where nQ `
is tlie number of shocks in the region Q for the period TQ. Under the con-
dition that the process of the occurrence of a strong earthquake is _
275
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~Ott O~~ICZAL US~ ONLY
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276
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Huhc~rdi.nrttr ta .luwH cl,lHC:nvcr.ad when ~.nve~tigatin~ the seixm~.r, conditione
ot the re~;ion~ c~f the centera o~ stz'ong eAxCh~uAkes in the pnst and rhe
se~,smi.c equivalence of the ind~,vidu~l sect3,ona of the Baykal seismic zone,
the attri,huCes Q, TQ and np can be used to discover the xegion~ of
increased aeismic danger it~ Che near future ~Borovik~ 1974)~
The region of low activity can be isolaeed by conserucrion of the m~ps
of the distribution of the epicenCers of ~aeak earthquakes by the defitted
Cime-space areas where the spattal parameter is the dimensions of the
preparation region of an earChquake of corresponding magnitude, and the
time parameter is the duration of the preparation peri~d of the earthquake
of the same magniCude.
Then rhe isolated regiona must be checked for the criterion nQ. �
The approximate values of Q, T for the correspo~lding magniCudes are
indicated above. Tt is necess~ry to find nQ for which the quiet can be
nssumed connected with Che formation o� the preparation region. For
t}iiA purpoae, selecCing the value of the low probabiliCy of Che random
rculizntian of the event within the limiCs of the defined region, let us
find the probabiLities of occurrence of 1,..., nQ shocks. If the
number of shocks n inthe.region Q for the period Tp is less than that
- selected by us (n,n~), then the quiet can be considered nonratYdom.
For probability Pa0.005, the possibility of isolating Che regiun where -
e~rthquakes of magnitude M~5-1/2 are probable was discussed under the -
condition that the average number of shocks in any elementary space~time _
area is identical for the entire investigated zone.
The annual distribution maps for the earth~uake epicenters with K>,8 are
constructed with respect to areas of Q=4000 km2 for 1964-1968. Within
the limits of this area, during the year earthquake~3 of energy class 8 -
an~ higher r.*.ust be absent, that is, nQ=O.
- When c~mparing the maps obtained, 1G years were isolated corresponding -
ro the parameters Q, TQ, n0� I, III, VII, IX~ !{II, XIV, XVII, XXXI,
XXXIX, XXXXII, XXXXIII, :{XXXVIII, XXXXIX, LI in Fig 96. All of the
strong earthquakes of M35-1/2 noted for 1964-1968 occurred within the
limits of the isolated areas (III 1966; III 1967; XXXII 1968),
that is, for Pribaykal'ye the probabil~ty of the occurrence of a strong _
earthquake with M?5--1/2 w~thin the limi.ts of the section with anomalously -
low activity is hi.gher (0.2~ than the probabi.l~.ty o~ a strong earthquake
within the limi.ts of the area of noxmal or increased activity. -
The simple divi,sion i.nto elementary areas and calculation of the numher _
of epicenters following into each area do not permit suf~iciently `
reliable determination of the d~,mensions of the regions of low concen- ,
tration of epicenters. Therefore, another density map was constructed:
~ an area 0.4� north latitude X 0.6'' east longitude was shifted by 0.1�
latitudinally and longi,tudinally, and ~n each of these shifted areas
the number of epicenters was calculated (Fig 97). Agair~st the background,
277
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- ~OR OFFTCZAL U5~ ONLY
of uniform norm~l density d~.stxibution (aee Figure 97, 2) areas of
reduced density were isolated (see ~ig 97~ 4)~ The atrongest enrChquakes
or significant swarma in the near ,future are more probable within tne
11m1CA er on Che boundariee oE the defined regione and in the regiona of
nnrmal or increASed ehock deneity~
It is natural thae the 5-year observation interval which we could analyze
is insufficient to obCain reliable forecasting attributea of a futur.e
atrong earthquake. The moat reliable resulta can be obtained when
analyzing the aeiamicity of the area for the longest time interval possible.
Unfortunately, we do not have the poesibiliCy of performing auch an
analysts. Only indirect estimaCea can be made,of the seismicity of the
isolated regiona of reduced density; analyais of the earthquake epicenter -
map with K^S for 1964-1968~ diatribution of strong earthquakes for 200
yeArs (1771-1971), centere of paleoseismodislocationa and achematics of
the basic fault syatems. The comparison confirms Che correcrnesa of the
possible appearance of st~ong earthquakes in the isolated regiona.
Within the boundariea of the I region on 28 March 1970, a strong earthquake
occurred (Mm5.5); in May 1970, a strong earthquake was noted (M=5.6)
within the limits of region V. In 1973 an earthquake wiCh Pi~4.5 and a
significant awarm within the limits of regions II and IV were observed.
Thus, a detailed analysis of the seismic information for a quite short
- observation period made it poasible to obtain results that deserve atten-
tion:
1. On Che basis of the investigation of 20 series of aftershocks and
one swarm, the relation was establiahed between the maximum linear dimen-
sions of the aftershock zone and magnitude of the main earthquake.
, 2. The investigation of the grouping of the earthquakes not belonging to
- the series of aftershocks and swarms demonstr~ted that out of all of the
earthquakes (K=$-11) recorded in 1964-1968, 18.2~ belong Co groups.
The mutual effect of the grouped earthquakes on each other is exhibited
at distances not exceeding 10 km. -
3. On the basis of the investigation of the regions of the centers of
12 earthquakes with M=5 and more it was established thtit before each of
them there is some region of calm, the dimensions of whtch are proportional
to the ma~nitude of the eaxthquake and ~~hich can be consaidered as the
preparation region.
4. The i,nvestigation of the ~,nverse law the re:lation of the ~'empty"
regions (correspond~ng to the parameters.Qt T, n 1 to tfie subseqiient -
occurrence o~ strong earthquakes demonstxa~ed ~hat the regions of calm
cnn be const,dered as reg~ona with ~,ncreased probability of the occurrence
of strong earthquakes or s~,gn~,~~,cant swarms.
278 -
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FOtt bFFIC'~AL U5~ ONLY ,
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279
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Long-Rnnse Forecaeting o~ the Se~,am~,c Activ~.ty Accnrding to the
Geophyaical Dara =
The b~~aic materiuls for permiCt~.ng charactexization of the aeismiciCy of
one region ox nnother are the resulCa of the procesei,ng of inatrument
ohservationa of earthquakea. However, the uni�orm se~amoat~tistical
m~teriAl for the southern part o� Eastern Siberia hae been accumulated
only since 1962. In accordance with the fact that the obaervation rime
is short, this material characterizes both the lon6-eerm and ehort~term
(random) components of the aeiamic process, In a number of regions, the
- random componenC can predominate. Therefore it ia difficult to forecast
the future seiemic activity with reapect to seiamoatatistica~ To a known
degree the indicated deficiency in atudying the seism3city is filled by
the paleoaeiemogeological method~ Seismogeological studies in the southern
p~rt of Eastern Siberia revealed a large number of paleoaeismodislacations,
and an approximate estimate was made of the force of the earChquakea as
a result of which the 3ndicated paleoseismodislocations were formed, The
material obtained indicates that the increased .s~iamiciCy was c-bserved in
individual aections of tha deacribed territ~ry hundreds and even thousands
oE years ago. However, as a reault of intense effect of the denudation
processes up to the present time, traces only of Che strongesC disastrous
earthquakes have been preserved by which, of course, it is impossible to
obtain a complete repreaentation of the manifeatation of the seiamic
process in the entire inveatigated territory of Eastern Siberia.
The information about strong earthquakes in the 17th to 19th centuries
that has come down to us, the broad material on paleoseismodislocations
in accordance with the seismastatistical data permit us to state that Che
increased seismicity during the prolonged period is characteristic of a
comparatively clearly located area in the Baykal rif~ zone. The continua-
tion of the proceas of tectonic activation in the Baykal rift zone is
indicated by numerous earthquakes 3000 or more per year.
The phenomenon of seismicity of the Baykal rift zone cannot be considered
isolated, separated from the various geological-geophysical characteristics
of the re~ion. The deep geophysical studies in re~ent years have estab-
tished that the zones of the latest tectonic activation both oceanic
~1nd continenta]. rift systems have a num ber of specific features:
_ contrast of the forms of modern relief, the existence o~ large rift basins
- f:[lled with thick Cenozoic deposits, increased heating of the earth's depths,
tl~e Presence of a zan,e of reduced velocities in the upper mantle and many
ot}ier characteristics. The Saykal rift zone, according to the data of
numerous studies (Bulmasov, 1959~ Zor~.n~ 1971; Gornostayev, et al., 1970;
Mishar~,na, 1967~ 1972; Novoselova, 1972 a, b; Puzyrev, et al., 1974) is
also char.acterized by surface and deep structure of the earth~s crust
significantly different from the border~ng territoxies and by the
specific peculiarities of the geophyat,cal f~elds respectively (see Chapter IV).
_ Thc variation oP the surface anci depth structure of the earth~s crust
caused by the riftogen~c process takes place sluwly~ and the characteristics
280
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of t}~e r.elief, C}ie HCructure o~ the e~trth'~ cru~t and rhe ~eophyeic~l
fi,~~IfIH riv~~llr~hl~~ r~t tl~r ~irr.~ant eimr. nrc+ tlic raAU]t nF ~~r.c~lnngr.ci dnveto~~mene ~
c~f tlie rekion~ Jn+~Hmuch uN ehc~ mocl~rn s~ipmiciCy of the Ddyknl rifr zone
- and coiCh peculiarities of its surfACe and deep strucCure characCerize
verinua aspecrs of the same CecConic process, the theoreCical poesibility
of ahraining the representation of the long~rerm componene of rhe seismicity
from a comparison of the seismoaC~ttiisCical data with the di�ferenC geologi-
cn1-geophysicnl parameters characterizing the lates~ tectonic activiCy is
noted. However, for extrnpnlation of the bae~.c per.uliarities of the lon~- _
rnnge component of the aeiamicity in the modern srage of development of
the region, proofs are needed of the preservation of the main trends in the
uppearance of the tectonic procesa~ We have certain proofs of this at our
disposal. First of all, this ia the manifestation of increased aeismicity
in almost the same frame of the region of Cenozoic activation where a
special surface structure of the ear.Ch and iCa depths is observed~ Then, -
comes the preaervation of the basic peculiarities in the development of
upllEts and basins. The farmaeion of the generated basins in the Kodar,
Udokan and Khamar-Daban ridges, the variation in rates of sediment accumula-
tion are pt~enomena of a local order.
Thus, huvin~ information ~lvailable about the long-range component of the
, tectonic process in the form of geomorphological parameters and the
charlcteristics of the geophysical field and data on the mode?-n seismicity
(we are talking about seismic activir_y), it is possible to try to establi.sh
quantitative relations betcoeen them and, in the presenct: of the latter, to -
determine the long-term comnonent of the seismicity~
Ttie study of the relations of seismicity to various geological-geophysical
parameters has acquired broad scale at the Present time. Quite frequently
the researchers have alerted themselves to the establishment of the
qualitative relations of the investigated parameters (Gamburtsev, 1954, _
1.955; Gamburtsev, Veytsman, 1956; Ibragimov, 1970; Drumya, 1973;
_ Kuznetsov, et al., 1971; Karagityan, Manukyan, 1971). The works aimed at
obtaining, quantitative characteristics of the relations of the seismicity
to the geological-geophysical parameters are of significantly greater
intereet (Riznichenko, et al., 1969; Tal'-Virskiy, et al., 1971; Butovskaya,
Sokolova, 1970; Gorshkov, Shenkareva, 1970), However, only in the papers
by V. I. Bune, M~ Ye. Artem~yev~ N. Sh. Kambarov (1971) and -
N. Sh. Kambarov (1971)~tvas an effort undertaken to estimate the seismic
dangcr of the territory on the basis of the quantitative relations of
seismicity, isostatic anomalies o# the gr.~avitational force and their ,
~;radients. ,
In I'ri.haykal'ye, the stud~es of the quant~tative relation o~ the seismic ~
sctivity to the relief and the grav~.tational �i.eld were begun by
Yu. V. Rizn~,chenko~ Yu~ A~ Zor~.n and K~ V. Pshennikov (~iznichenko, et al.,
19G9). The seismic activity map rompiled by K~ V. Pshennikov by the
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method af summ~?tion of the eArthquakea us~,ng a conatane averaging area
for the period from 1962 to 1966 wae compared wiCh the altitudes of the
uver~ge xelief (.Che dimpneions ot' the averaging area were 30X30 lan),
the moduli of the alri,tude Rradi,enC o~ Che ~verage relief (the dimensions
of the averag~.ng area arE 45X45 lan) and averaged isostatic anomaliea
calcul~Ced by Yu, A, 2orin by ~he eimplif ied meChod proposed by him.
The pair correlation was fulf illed for the enCire rerritory of the Baykal
rift on the whole and aeparately for iCs flanks and cenCral regions~ Iti
turned out that over the enCire territory there is no clear quantitative
- interrelation beCween the altiCudes of the average relief and the seismic
~ctivity. The pair correlaCion coefficient ia close to zero. It
increases to -0~34�0.15 only on Che flanks o.f the rift sysCem. _
The modulus of :he altitudF gradient of the average relief is correlated
- with Che seiamic activity somewhat beCter: rm0,36+0~09 and preaerves the
order of magnitude both in the individual aecC3ons of the terriCory and -
_ on the whole throughout the rift zone.
'The re.lation between the averaged isoatatic anomalies and the seismic
activity turned out also to be reliable, but weak (r=0.23+0.09~. On
making the transition from one section of the x�ift to the other, the
nature of the relation did not remain constant. The results obtained led
to the conclusion that the quantitative relations between the seismic
activity and some of the ~eomorphological-gravimetric parameters in the
_ linear and quadratic forma exist reliably, but they are weak and cannot be
used for forecasCing the long range average aeismic activity.
The further study of the interrelation of seismic activity and the geologi-
cal-~eophysical parameters was continued by Ai. R. Novoselova and
Yu. A. Zorin in the direction of finding an improved form of the relation
and the set of parameters which would have a closer relation to the
seismicity. For comparison, a map of the seismic activity is used which -
was constructed at the Seiamology Laboratory of the Institute of the Earth's
Crust of the Siberian Department of the USSR Academy of Sciences by the
neChod of constant accuracy on seismostatistical data for 196~-1968. The
dimensions of the averaging areas varied from 96 to 18,000 km , and
accuracy of determining the seismic activity turned out to be equal to 35%.
The seismic activity was calculated by the generally accepted formula in
the shocks of the neCworlc with a step size of 0.2� wi;h resoect to latitude
and lonsitude. All of the earthquakes were used beginning with the
8th energy ~:lass. The lOth class was taken as K~. The angular coefficient
of the recurre~ce rate graph �or using the set of earthquakes is 0.485.
- The clesr.ribed map of seismic acti,v~,ty is in genezal �eature similar to
that in the paper by Yu. V. Rizn~chenko; et al, (1969), but it differs
in detail~ This difference i,s caused by the use ef the seismostatistical
- material for various years and the applicat~,on of various consCruction
procedure, It is necessary to note Chat the correlat3on coefficient
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berwc~en the valuas of Che aeiem~,c act~,vity o� the Cwo maps ia 0.6. How-
_ ever, when repe~tinQ the correlation o~ Che aeisnic activity with respecC
to rhe new mnp ro the ~radiente of the averaged altitudes and isoatatic
~nomnlies, estimntes were obtAi,ned for Che degr~ of linear And quadratic
rcinttona linving tlie snme order as in the earlier paper (Riznichenko, et
n1., 1969~.
The modulua of the alrieude grad3ents of ehe upper Cretaceous to Paleogenic
planation sur�ace deformed by the latest movements, the modulus of Che
horizontal gradients of the gravieational anomalies in the Bouguer reductions
~nd the isostaCic and also the values of the graviCational anomaliea in the
Bouguer reduction were used as the new parameters wiCh which a comparison
of the seiamic activity was made. The maps of the moduli were constructed
by the general principles described in Che paper by Yu. V. Riznichenko,
ee al., (1969). The gradients were calculated by the averaging areas on
the order of 9000 km2. The latter value was obtained as the arithmetic
mean oE the dimensions of the earth used to calculate the seismic activity.
'1'he pair correlation coefficients.characterizing the linear form of the
relation turned out to be reliable, but low~ -
Then the seC correlation of the seismic activity with the sets o� geological- _
geophysical parameters was carried out. Several versions of the combination
oE the correlated parameters were tested, but the values characterizing
_ the dismemb~rmenC of the relief, the variability of the 1oca1 component of
the gravitational field and the values of this field themselves a1~-ays
parCicipated here. In addiCion to the linear relation, the quadratic,
cubic, logarithmic and semilogarithmic forms were also tested. The best
form of ttie relation turned out to be the semilogarithmic (the logarithm
of the seismic activity was conaidered to be a linear function of the
geological-geophysical parameters). With this form of the relation, the
maximum set correlation co~fficient (0.75+0.05) was obtained for the seismic
activity, the altitude gradients of the average relief, the gradients of
- the isostatic anomalies and the Bouguer anomalies respectively,
The regression equation has the forml
A1~ = 2.3 exp {75.58� Igrad h~p~ + 0~1� ~grad giz~ - 0.01� gb - 4.Q2} (1)
A map of forecast~,ng the long~range component o~ the seismic act~.v~,ty was
constructed hy th~s equat~,on~ The an$lysis of the map is presented in the
paper hy Yu. A. Zorin and P1. R. Novoselova (1972~.
`All oP the calculations connected w~th the correlation analysis and
determination of the coef�~,c~,ents of regress~,on equations were performed on
the a~Srl-4 computer of the Eastern Geophysical Trust (Yrkutsk).
_ F
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In 1972 S. T. Calenetskiy and G~ L~ Myl~nikovd conetructed d new map
nE thr. ecei.smic activ:Lty by the method o� ~ummetion of Che earthqualce wiCh
r~ cc~nHtnnl� nvern~,ing nrrn (the proviei.onnl dimeneione of Che area remained
constnnt). Its eimilqr ch~tracterisCic ia presented in Chapter VIII~ Here
leC us note that the unqueationed advantage of the new map, in contraeC
to the previously compi,led onea, is rhat it encompasaea a large $mount of
seismostatiatical material (.1962~.1971).
NaCurally it could be hoped that this map would give a more ob~ective
. characteristic of the seiamic activit,y and would be more advahtageoua -
for determination of ita long~term component. The map was consCructed in
two versiona: considering all of the earthquakes and with exclusion of
the siaarma of weak ahocka ~
In view of the fact Char the averaging area has appreciably amaller dimen-
sions (988 to 1321 km2) by comparieon with the average area used previously,
the necesaity arose for transformation of the maps of the geological and
geophysical parametera reapectively (to present Che dimensione of the
parameter averaging areas in accordance with those which were used for
calculation af the seiamic activity).
The carrelated valuea of the aeismic activity and the geological-geophyaical
parameters were aelecte8 in the ahocke of the 45:{15 km n~etwork. The
- set correlation coefficient turned out to be equal to 0.75+0.05, The
regression equation has the form ~
A10 = 2.3~exp {80.03~ 18rad h~l~ + 0.07�~~rad giz~ - 0.013~gB - 4.90} (2)
A comparison of equations (1) and (2) indicat:.,s that their coefficients
are close to each other, Thus, in spite of tne different initial seismo- ~
statistical material, the operation of planation of Che series using
stab ly defined geological~geophysical parameters leads to close results.
_ This permits the conclusion to be drawn that as a~result we obtained the
description of the actually stable (long-term) component of the seismic -
process. _
I~ must be more precisely determined that the presented equatton (2) was
obtained as a result of comparing the geological-geophysical parameters
with the total values of the seismic activity (that is, with those which
were obtained when considering all of the earthquakes beginn3ng with their
given representative class). Using the maps of the seismic activity with
the excluded earthquake forms, in practice the same equation is obtained
(the differences in the coefficients are statistically reliable). This
_ means that the proposed proced~~re automatically insures exclusion of the
�orms o� weak earthquakes if these seism~,c events are random~
Let us try to explain the ex~sting rela[i,ons of the seismic activitv to
each of the parameters enter~.ng into equations (1) and (2). The modulus
of the altitude gradient of the averaged re~ief is dirQCtly proportional
- 28~,
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to rhe modulua nf the horizontal velocity gradienC of the laCegt vertical
movements~ T}ie physical meAning of the relatiun o� Che lASt value eo rhe -
= seiamic conditinns i~ generally known (Czovakiy, 1959, 1963). Under
~ natur~l conditions, for nonuniformity of the earth's crusr, this relaCion
is entirely naturally of a statistical nature; therefore in individual
secCions its vio].ation is entirely admissible~
T}ie physical essence of the relation of Che seismic activiCy to the gravi-
taCional field is not so obvious~ The .Eollowing argumenta help to explain
it. In Chapter TI it was pointed out Chat the Baykal rifC zone in the
Bouguer anaomaly �ield corresponds to ehe extended regional minimum (more
precisely, the system of minima) which, ~udging by the deep seismic sound-
ings, is cau~ed by the presence of the region of dispersion of th~ upper
mantle (see Chnpter IV). The riae of the dispersed material from great
depChe obviously is Che baeic caus~ for riftogenesis (Artem'yev~
_ Artyushkov, 1968; Zorin, 1971), to one o� the manifeatatinns of which the
incrcused seismicity of the region belongs~ The intensiCy of Che rifto-
genesis obviously is directly related to the volume of material accumulated
under the crusr. On this level the correlation of the seismic activity
to the inCensity of the Bouguer anomaly becomes understandable.
- The relation of the seismicity to the horizontal gradients of the local
_ ~nomalies is assumed to be exolained by the fact that the maxima of the
latter fix the fracCures. However, when using the gradients of the iso-
static anomalies of the averaging area on the order of 40 lan in diameter
for the calculation, the peaks of the gradients can only in individual
cases correspond to specific large faults. The analysis of the map of
the modulus of the gradients of the isostatic anomalies indicates that the
increased values of this param~ter are characteristic of the entire rift
zone as a whole, that is, in generali~ed form it reflects only the degree
- of contrast of the local anomalies (the regional component of the field
is completely excluded by isostatic reduction}~ The contrast of the local
anomalies is caused primarily by the presence of a thick series of
Cenozoic deposits in the large (but comparatively narrow) rift basins of
the A~ykal, Barguzin and other types. Therefore the relation of the seismic
activity to the moduli of the gradient of the isostatic anomalies indirectly
reflects rhe inheritance of the modern tectonic movements expressed in the
seismicity from the movements of the entire latest stage. This is valid
also with rzspect to the remaining used parameters~ The contrast of the
local gravitational anomalies is caused, in addition, by increased
heterogeneity of the upper layer of the earth~s crust. As t4. R. Novoselova
(1972) demonstrated, this is a speci~3c feature of the Baykal rif t zone
by compar~son w~th the border~.ng territories~ The direct consequence of
thig is a reduction in the mech$nical strength of the crust material -
which under the conditions of the tectonic activation promotes destruction
oE the continuity of the mater~,al and~ consequentlyf an increase in -
seismicity~ Ye, V. Karus and I~ Ye~ Rezanov (1971~ indicate that the
- sections of articulation of the materials with different physical proper-
- ties are most favorable tor the man~festation of seismicity~
285
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' O,l !
~
~ ,
~
~9) 0~'~ e 12) .
C ~ 1,~~ w
-
_
i
f =
~ (8) ~ 13)
p ~ , 5 '~'e
~ 7 ) ' ~ a �p ~ *
:
� ~ Kr.M ~
6) e~ ~~,~p'`' :,y ( et .
~ e oi
~ ' ~~f �
. a� ( 0) t~~ ,
~ ):'~f ~21 ~ ~
t ~aN \
~ a ~0~ ,�,r~t r4
~ 5) ,g'~�, o+ ( 24 ) c~e
~ ~oF 9�`~(23) 3' 25
, 04~ � ( 3
~ (27) .
\2~ Qp~~. . 4NTA ~i
; nPnrrc'~ ,.;~'a~32) (26~
. 4,,j. ~ ~ ~o
.rM~ ~`L. : ,.yf' � OR 0/ _
N~r~ � ~J~ 31~ p~0~ . !
. ~
( ) �'a~~~ a,os-~ (1) / 9) (28) ' ~
a~ ~ ~ ~ -
~ r
.
I'igure 98. Map of the long~term seismic activity of -
Pribaykal'ye. Compiled by M. Novoselova.
_ 1-- isolines of the long~term component of the seismic
activity; 2-- boundary of the Baykal rift zone
(accord3ng to Yu. A~ Zorin~ 1971)
Key;
1. Selenga; 2~ Irkutsk; 3. Irkut~ 4. Kimoy; 5. Angard; 6. Kirenga;
~ 7. Chaya; 8. Gre~ter Chuya; 9, Lena; 10. Upper Angara; 11. Chara;
- 12. Olekma; 13. Nyukzha; 14. Kuandat 15. Muyakan; 16, Muya; ~
t7. Tsipa; 18. Tsinikam~ 19. Kalar~ 20, 1Ca~akan; 21. Tungir~ -
22. Amalat; 23. Vi,tim; 24~ Nercha~ 25. Shilka; 26~ Argun';
_ 27. Chita~ 28. Onon~ 29. Ingoda~ 30~ Chikoy; 31. Rhilok~
32, Uda; 33. Barguzin; 34. Lake Baykal.
286
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Ueing equation (2) dnd 'che valuea of the above~menCioned parameCers~ we
c~lculated Ch~ long-Cexm component of Che seismic activity (~ig 98) for
the cntire terriCory of the Baykal rift zone~ It appears useful to us
to compare the ~icture obtained w~,th the initial data CaeiAmostatistical.)
on the Aeismi,c ncCivity~ In this compaxison three cases are theoretically
possible: . ~
- 1. Complete coincidence of the init3al and forecasting maps. This
indicates the absolute preservation of the�trend in the development of _
the tecConic process and the uncondiCional auitability of Che initial map
oE the seismic activity for Che long-range fcrecasting of the place and -
tt~e strength of the earthquakes. However, the sections for comparison of
the initial and forecasting map are few. They have small area and are
~ arranged primar.ily around the periphery of the Bayl:al rift zone~
2. The values of the long-term seismic acCivity are higher than on the
iniCial step. Beginning with the statement of the problem itself, in this
case we can show that the reduction in setsmic activity in such areas is
- a temporary phenomenon. IC is impossible to guarantee that this reduction
will last a long time in the future. On the contrary, the teceonically
active sections in the recent geological past in which the last 5 to 10
years the activity is relatively dropped, can correspond to the preparation
- zones of strong earthquat:es. This conclusion agrees well with the data of
- N. S. Borovik, et al., (1971) regarding the formation of such zones in a'
few years before the strong earthquakes. ,
The repion: with such relations of modern a; , ~ f3 'r'~ ,C _
" . ~ ~ ~ ~ ~ y ~
~ �V ~r.~ al
N. �i~� i~ M O
V ~ : ^
^`j ~ + ' ^ W ~ ~
!1� ~ ~ \ ~ ~ ~1
~+r� r n
? ~ 1 v~
~ ~ ; u w A eN
� ~ ~p p
~ - C ; aQi ait9 a
~ ~ '/S v ~ 'C: 1"~ ~
~ f ' V fJ 01 �
^ tn A ~
~
11 ~
~ ~
'b
- ; r^i t ~ ~ �
v ~ ~ v � � "+y v O ~
^ ~ e"y rl
N ~ ~
V ~ ~
~ , 1~ ~
~ C ~ ~ ' ~o d
~7
0~+
324
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~L~g~nd ~nd key fnr ~i.g 106, p 3~4] ; ~
1-- Sy~ehmg of f~u1C~ ~nd Cheir abbreviat~d n~m~s; 2~~ f~uleg ~nd Cheir
,~umbpr~ on th~ li~ts 3-- boundaxy of the Baykal rift zonp; name of ehe
~yetem nf F~ ult~ and the components of their individual dielocations with
bt~eaks in eonrinuiCy; GS Ma3.n Sayan daep �gult: 1-- ttai.n Sayan,
2 Biryusinekiy [Biryunen~, 3-~ Okin~kay~ [Okn], 4-~ Kitoyekiy,
99 Dototgkiy, q-- Obruch~v; 5-~ Tunkingkiy- 6-- primor~kiy,
7-- NorChprn ~aykal, 8-- K(?)icherakiy, 9-~ Tyya-Abch~dskiy, 10
Gramnin~kiy, 11 Pogrnnichnyy, 12 Akiekanekiy, OV O1'lchnn~kgyg
(n1'khon) br~nch of thp Obruch~v syet~m, 13 bl'khon, 14 Svygtnnng~kiy
~Svyaeoy NosJ, 15 Chivyrkuyskiy, 16 Kabeniy, 17 Bo1'~her~ehen(7)ekiy.
Ch --Cherekiy; 18 Cherskiy, 15 R Ue1'tovyy, 20 Bezymyannyy (unngmed~,
~ 21 ttgCkov ekiy, 22 Nalimovskiy, 5T Selpnga-Turkinskaya br~nch of
th~ Cherekiy syaCem: 23 3elenga, 24 Khamarekiy, 25 Turkinekiy,
n-- Barguzin: 26 UlyuChikanskiy, 27 Sh~manekiy, 28 Turaki, VA
V~rkhnean$argkaya (Upper Anggra]; 29 Verkhneangarskiy (Upper Angarn~,
~U pravomanekiy [l~ight Mama], UK Ukolkitakaya; 31 Uknikitskiy,
32 Knvnktinakaya, ITs Ikae-Tsipikan~kgya; 33 Maraktaknnakiy, _
34 G~~r~inskiy, 35 Ulan-Burginskiy, 36 nzhargnlanCa N~rungdingkiy,
37 Tsipikgngkiy, 38 Gorbylokskiy, 97 IkaCgkiy, BV gar~uzino-
Vitim; 39 Yambuyekiy, 40 Marekta-Mukdekenskiy, 41 Vitimkanskiy,
bV Uzhida-Vitim; 42 w- bzhida, 43 Khambinskiy, 44 Uda, 45 Amnlat- -
skiy, 46 zgxinskiy, 47 Verkhnevitim~kiy [Upper Vitim~, TT
Tugnuyskaya: 48 Tugnuyakiy, 49 Zaganakiy, 50 Kichingakiy,
KhK Khilok-Karengskaya; 51 Khiloksl;iy; 52 Yuzhnokhilokskiy
[5outhern Khilokskiy~, 53 Beklemeshevskiy, 54 Karengskiy, MO
Mon~olo-Okhotsk deep fault: 55 Kudarinakiy, 56 Chikoyskiy, 57
2achikoyskiy; 58 Pravo-Ingod inskiy [Right Ingod~], 59 L~vo-Ingodinskiy
(Left Ingoda~, 60 Shilkinekiy (Shilka~, Nizhnenerzhuganskayn branch of
the Mongolo-Okhotsk system: 61 Nerchuganskiy, 62 Verkhnetungirgkiy,
OT Onon-Turinskaya: 63 Ononskiy, N-- Ptuyskaya [Muya]; 64 ttuyakanskiy;
65 Verkhnemuyakiy [Upper Muya~, 66 Ulan-Makitskiy, 67 Nizhnemuysl:iy
(Lower Muyaj, 68 Peramskiy [ParamaJ, MT Muya-Tokko: 69 Mudirikanskiy.
70 Yuzhno-Muyskiy [Southern Muyaj, 71 Syul'banpkiy, 72 Kodarskiy
(Kodar~, 73 Tokkinskiy (Tokko], ChKh- Chitkanda--Khaniyskaya branch of the
Muya-Tokko syatem: 74 Chitkandinskiy, 75 Khaniyskiy. TsB Tsipa-
t3~untovr~kaya: 76 Tsipinskiy [Tsipaj, 77 Bauntovskiy; 78 Kddurskiy,
79 Tilishminskiy, 80 Bnmbuyskiy, 81 Taksima-Dzhilindinskiy,
U-- Udokanskaya (Udokan); 82 Namarakitskaya, 83 Konda-Eymnakhskiy,
84 Dovochanskiy, 85 Lurvinakiy, 86 Emetachi-Kemenskiy, 87
Chin.~-Vakatskiy, 88 Katuginskiy, 89 Chepinskiy, K-~ Kalarskaya
(Kalar]: 90 Ust'-Tsipa, 91 Nizhnekalarskiy [LoWer Kalar], 92
bzh~lo, S--- Stanovoy deep fault; 93 ~ Tas-Yuryakhskiy, 94 Imangrskiy,
95 Stanovoy~ 96 Yuzhno~-Stanovoy [Southern StanovoyJ. Individaul faillts,
98 Gazimurskiy~ 100 T~ssinskiy [Tisea), 101 Fofanovskiy.
(Key to Fig 106, p 326~
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(K~y Co ~ig 106, p 324];
1-- iliry?u~c~; z~- GS; 3 M~ Uda; 4-~ Nizhneudingk; 5~~ 'Cu1un; 6~- Iy~;
7-- Alygdzher; 8-- Oka; 9~~ Cheremkhovo; 10 M-~ Orlik; 11 Ziea;
lz Upol'ye-Sihir~kn~?e; 13 G5; 14 Mendy; 15 Slyudy~tnkn;
1h t3nyk~t'~k; 17 UV; 1~ Z~kam~nek; 19 L~kp Khubsugul; 2b
KyekhCt~; 21 Gu~ir~dt~~ersk; 22 U1an-Udeg 23 ST.; 24 Selenga;
25 Ye18nC~y; 26 Irlcuegk; 27 Use'-Ordynslciy; 2B Kachug; 29
Uge'-Kut;, 30 Kir~ngk; 31 Vieim; 32 Lena; ~3 VA;'34 UK; 35
Kumora; ~6 UK; ~7 B~rguzin; 3~ ~Iarguzin; 39 8V; 40 Sosnovd-
Oz~rgk; 41 Yer~vninskiy Lake; 42 Romanovka; 43 gegd~rin; 44 U~kie; .
_ 45 PPT; 46 Vitim; 47 N~lyaCy; 4E Kalars 49 C~ntrgl Kg1~r;
50 UV; 51 Lake Baykal; 52 KhK; 53 Karenga; 54 Bukach~ch~;
55 Nerehinak; 56 Khepcheranga; 57 ~M Borun-Torey Lake; 58 Borzya; -
59 Argun' ; 60 Shilk~; 61 ~orn;+y 7.~renCuy ; 62 Ar~ur; 63 Tun~ir;
64 Tupik; 65 r~ogocha; 66 Mo; 67 olekma; 6A Tokko; 69
C1�ra; 70 Ol~kminsk;; 71 Chita; 72 Nyulczha; 73 Chikoy;
74 Nizhne~ngarsk; 75 VA -
- The mnin (trunk) ncCivated faultg are oft~n acaompani~d by shnrt (ro the
fir~r ten~ of kilometers) feaCh~r~ng and accompgnying fractureg pl~ying an
imnortnnt role in the development of the fine block etrucrur~a in the
secttons near the fgults. ~he amplitud~g of the vertic~l di$placements
~long certain faults ~re different, ~nd they depend both on the age and
the morphogenetic type of the strucrures than on the speed and direction
nE the latest tectonic movements. Here the Ereatest amrlitudes of the
vertical displacement (to 3000 to 7000 meters) are noted by the activared
faults bounding Che mature morphoatructurea of the Baykal basins maintaining
n stgbl~ trend toward subsidence during the enCire period of rift formation.
The least diaplacpment amplitudes tena to a few hundreds of inetera) are �
noted with respect to the activated faulta of the youngest basins of the
evolutionary geries and a:.~u in the aections of inverted infantile rift and
_ subrift basins.
With re3pect to degree of inheritance of the pre-Cenozoic structural plan
and alt~rntion nf it by the latest tectonic movements the mounCain bele of
~astprn Siberia is extremely nonuniform: along with the areas of prolonged
inherited development here~ the zones of eharp and singl~ structural re-
arrangement are widespread. Analyxing the strict apatial loca~.ization of
tl~e basin~ oE the Baykal aite~ the syscems of activated faults controllin~
theae nxial ~tructures and Che ratio of the Cenozoic and ancient strucCural
plnna, N. A~ ~'lorensov (1960a,1964, 19~8) showed that the rift zone extend-
ing apatiAlly to the ancient marginai auture of the Siberian platform is
distinguished by sharp Ruperposition of the substrate structures, to -
Tertinry.
Tl~r ~pinion of V~ P. Sulonenko regarding ~he genetically independent develop-
m~nt of tl~e Baykol riEt system aith reapect to the ancient structures is
atill morr deEinit~. "The Baykal rift zone is ad~acent to the marginal
- 326
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puuthern rro~ecCion of Che S~,ber~,~n plati�orm only over a ehort segment,
nnd th~n it defl~cta sh~rply aw~y from it~ in ~pite of ehe presence ar e;he
plnt�orm boundary oE powerful mnrg~,na1 tecton~,c suCurea~��~ the Sayan fault
zone~ Th~ ~econd~ry role of the Siberian platform and the pre~Baykal
deep fra~Curee i~ Craced quiee clearly here~.. The basins, Kosogol'skay$
~nd Barkh~rekaya, in general go from th~ �ield of Baykal folding ro the
. C~ledonian.~. The Barguzino~8auntovekaya and Upper Angara brgnchea of t'he
bneine are sti11 mor~ removed from ehe Siberian latform.
_ ~QCtor the rifC zone inCerAecte the ~y~Cem of Baykal �old3ngn ehe tT~y~ov~oy
cpntrol maseif~ the Chara b1o~k, and 3t cuta by one branch intn Che Aldau?
ehield and by Che other, into the reg3on of Proterozoic folding of Stano~vik...
mhe deep gnd large re~ional faulte of the pre~Baykal occurrence form a
dense network in the region of Cenozoic orogenesis. It is eneirely natu~cal
that 8ome of them~ ~u~t as the weakened zones of the earth's cruaC~ are
~ncompassed by rifC formaC4on, but ehey hAV~ only promoted and have not
rredeeerminpd Che place of occurrence of the rifte.,~ Therefore in Che FieismoM
~eoi~gical e~timaCe of Che ,fault zone it is necessary to discover in deta,il
tt~e degree of their ~articipation in the rift formaCion and "aceive"
tecCOnics~ The powerful fault zone ie well expresaed geologically and even
geomorphologically, can turn out to be aeiamically passive, and ehe
unexpressed young or pre-Ba~+kal faults, recently involved in re~uvenation -
(for example~ in the embryonic basin zones), highly'~acCive" (Solonenko,
V., 1968a, PP 69-70).
Th~ morphostructures located outaide the rift zone have inherited to a
significant degree the structural-tectonic plan of Che preceding ategea of
dev~elopment, and the principle of inheritance on the whole is maintAined both
with reapect to the ancienC and young faults and with respect to the folded
complexe~. All of this is felt to one degree or another in the variety of
structural forms which are the result of the prolonged hiatory of geologic,al
development of the mountain belt of Eastern Siberia, and in the final
analysis it finds itg expreaeion in the peculiarities of the manifestation
of seiamicity. The moat highZy aeismic regions are isolated in the axial -
part of the Baykalo-Stanovoy zone where as a result of predominant extensi~~n,
there is complex block differentiation of the earth's crust with the fot~na~-
tion of an extended syetem of rift basina and the block and arch-block
upiifts bordering them. The intensive seismotecr.onic development of this
zone in which the primary role is ~layed by Che systems Of activaCed fault~;
inEluences the bordering terri.toriea and cauaes increased aeismic potentia;l
ef the Ad~ncent zones of act~vation of the southern part of the Siberian
pl.~tform and the Mongolian-~Okhotak fold~d belt.
The seismogeological relations are varied. As the basic relations it is
possible to i,nd~cate the relgtion of the earthquakes to the zones of
~ctivated faults~ the blocks of shazoly di�fer~ntiated tectonic movements,
the sect~ons o~ local re$xxAngement of the Cenozoic and more atncient struc-~
tures of the plans by the r3ttogenic procesaes, the marginal parts of the
regiona of stnble subsidence or uplift, the interbaain and intrabasin
� 327
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m~~unCnin commiesuxes, Ch~ ar~ae of the ~.ntersectioa and echelon cyne
r,xeir.ulnrion o~ rhe lntesC morphosCructures, especially rhe large fracture
zones to the embryonic basins, the aect~,ons of *~anifeatation oE Che lateaC
volcnniem, and so on. _
Tn many papera on the varioue seismicdlly r.ctive regions when discovering
the laws o� the relation o~ earthquakea and the geological atructure, not
only the se~.amological but also ehe ger..log3cal~tectonic criteria of the
oncurrence of earthq~akes are given. In recent times studiea have been made
from th~ae anmplex seiemotectonic p~.~nts of view of Che seismically active
regions nf rtongolia and Pribaykal~ye, Central Asia and the Caucasus, and
gbrond Southern CaliFornia, Alaska, Japan, New Zealand and so on _
(Gubin, 1960; Solonenko, V,, et al~, 1960b; Petruahevskiy, 1960, 1964;
Cobi-Altay..., 1963; ACTIVE TECTONICS,.., 1966; SEISt�tOTECTONICS..., L968,
1975n, b; Kuchay, L969; Medvedev, et al~, 1971; A1Len, et al., 1965;
anc' eo on). H~re the main role was given Co the deep and crystal acCivated
faults having important si~nificance in the seismotectonic development of
~he morphoatructural elements and i~n esCimating the level of their potential
seismicity.
In thc different atages of their development and depending on the morpho-
~enetic type of bounded structures, the seismotectonic role of the acCivaCed
faults can be different. For example, they ~can be zones af release of the _
mose powerful seismic stresses, buC in the case of "transitional" tremors _
usually part of the energy of the seismic waves is absorbed, causing an
irregulAr decrease in strength of the earthquake. In one way or another the
zones of activated.faults, which are extremely mobile and connected with the
deep parta of the earth's crust, react moat extraordinarily to all of the
geodynamic changes occurring in iC. Although in differe~.tt parts they have
different level of modern seismic activity, nevertheless the individual faults
controlling the development of the penetically united mo��phostructures (for _
example, the individual rift basins) must be considered ~;-?otentially seismically _
active over their entire extent. Here the maximum intensity of the earth-
qual:es (the potenCial seismicity) must be determined by the scales of maximum
seismic dislocations detected at least in one section of the fracture zone,
for the seismostatistics do not always or everywhere reflect the upper level =
of seismicity. However, in th~ cases of complex internal structure of the
large basins and uplifts, the zones of activated faults separating them into
different sectiona can have different seismic potential (for exa.mple, ?.tain
Sayan, Tur:kinakiy, and the Obruchev faults).
The seismogeological mater3.als available at the present time are permitting !
us to isolate 22 systems of the latest ~aults in the ~aykal~Stanovoy zone,
including more than 1Q0 �racture structures (see k'~g 106~ undergoing modern
~ seiamic rejuvenation or carry~ng traces of paleose~smodislocations. All
of t~~ese zones correspond to the above--enumerated common morphostructural
ai~d seismotectonic peculiari,ties o~ the activated ~aultst therefore below
- We shal]. preaent the character~,stic of only two fracture systems typi~al
of the Baykal~Stanovoy zone of intensive arch-block and ri�togenic movements; -
328
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xo~ otrnicin~, us~ nrn.Y
the wpll-known primdrgkdye (~xuchpv) ~~u1t Which p~ct~nda a1nn~ the ndrth-
weatern ~hore ef gnykal in the Uddk~n ~y~rem d~ gceivgtpd fnult~ in th~
northea~t di the Baykal rift zon~~ U~~gi1~d de~criptt~ng nf the m~~nrity
of the fauitg ia eh~ mountain bplt of ~a~tern Sib~ri~ ~re p~r+~~ene~d in the
publicatione nf r~c~nt y~~ra ~~i~r~n~ov~ 1460e~ b; AC'CtV~ '~EC`CON~GS~.~,
1966; SLISMOTEC'CONICS.~.~ 1960a~ i975~, b; ~oldn~nko, V., ~t gi., 19~1;
Sherm.yn, er nl~~ 1~7~; ~nd gn ~n).
b. i, ShChtrb~kov (1951) propng~d thgt th~ fauit b~unding the ~ygtem ef
munkin~kiy ba~in~ and the Bayk~1 rift iC~~lf dn eh~ Sib~ri~n plgt~orm ~id+~ -
be Cniled the Obruehev f~ult~ it i~ mad~ up nf e numb~2r of ind~p~ndpnt
_ branche~ of the gyetemg df faulte ~ Tunkinskay~, primor~kaya, (~1'khon ~nd
Northern Baykal (Flor~ngnv, 1960b; S~2SM0'T~C'PONIGS..~~ 1968; Zorin, 1971).
The Tunkinakiy scrikp�~lip fQUit (~ig lOG~ e~e ~ig 102j i~ the $en~r~l
~tructure of the pntire ch~in of Tunkinekiy baein~. A~ eh~ C~noznic diglncg-
tion, it inheritpd thp ancient ~uture fnrmpd in th~ Lrn+~r P~l~nzoir
(~lorensov, 1960a) or in eCill. ~grlier agea. It ie not ~x~ludpd that thig
rejuv~nntion occurred in the Centrel to Upper Plioeene durir?g eh~ period of
the mosc energptic downWarping of th~ bottomg of the d~preegion~ (ltu~hieh,
1922). ~~ing diaeoncinuous, the Tunkinekiy fracture ig n?gd~ up of g~ver~l
aections, in the damping of which the mountgin epur~ nccur (Nilovgkiy,
Yelovskiy) tranev~ree gnd diagonal intrabasin commi~sures having a
reduced gection nf Neogene-Quaternary geri~~ (Logachev, 1958). At the
point~ where the main feult line benda~ bunch~g of tranaverg~ and radigl
fractures appenr (Florensov, 1960a).
By the observetians of A. p. Shmotov (1972), east of Arshan th~ bran~h ~f
the Tunkinak:y fault inheriCg the ancient (Tubotekiy) overthrust. I[ is
trgced from the Tsagen-Ugun' River from the Torskaya basin to the Tubata
River valley through the Yel~vakiy spur to the Kymgarga River and then to
the northWest (see Pig lOx). BetWeen the Tunkinskiy bald peaks and the
Yelovskiy epur the zone of ancient overthruet is morpt~ologically expreased -
in the form of a linear chute-like depression running a distance of up to
15 km (aee the vicinity of the Arahanskaya etructure in Pig 102).
in the inveatigated region th~ ancient overthruets are mapped at many places
(see ~ig 102), but the linear sinl:hole in the relief is expreased only by
the Tubotskiy overthrust. Inasmuch as it ia locat~d in the zone of
- contrast articulation of the i~ntensely developing rift basina With their
mountain bord~r, there are grounds for considering that the morphological
rxpresRior~ of the ancient fr~cture ~n the modern r~lief is obligated to its
C.enozoic r~juvenation and conversion to the Tunkinskiy atrike-~slip fault.
The tiiKhl~tnd scarp Which replacea this sinkhole in the west and obliquely
i,ntersecting the anc:Qnt series on the slope o~ the Tunkinskiy Alps
dirrctly indicatea the stepped sagR~nE of the blocks ~n the vicinity of the
Tunkinakiy t'ault (Shmotov~ 1972s Solonenko~ V.~ et al., 1971). The compara-
tive yo~ngness of the Tunkinakiy atrike�~elip fault is indicated by the
~ fractures of thr Pleietocene terraces in the vicinity of the health resort
329
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Figure 107. Schematic of the seigmotectonics of the central part
of the Ikatakiy ~IkatJ arched uplift.
Compiled by M~ Dem~yanovich.
(See legend and key on p 331)
330
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F01t OI~~CIAL U$~ nNLY
~LE~~ttd end k~y tn ~ig 1~7, p 330~;
Seigm~[city; 1�- ~picpnt~r~ c~f th~ ~~rthqu~ice~ with reep~~t ~d ~n~r~y
maeae:3 -w Ks e~~, b-~ 7, 8, d�~ 9~ 10~ f r~ 10~5 eo i~, -
g-- :11.5~ h~-~- 12; 7,4 group~ df ~~rthr~uak~~ by eh~ +center m~chaniam~,
2--f1r~e ~raup; 3--~~c~nd, 4--third; 5--dir~~Cian of gtr~~~ ~x~~,(e--compr~~~ive
b-~-~ teneion~ c-� int~rm~diate~. Seiemotpctonicgt 6-~ mosC m~bil~
block of mod~rat~ upiift; ~
' 8-- wegk uplift, 9-- pro~ect3nng di the bas~ment in th~ b~8pm~nt nf the
_ tran~it~dn t;?p~; 10 outcropg ef G~nozoic baea~ts; 11 pgrt of the
Karguzin basin of th~ Baykal typ~; 12 ~mbryonic bagin~ (1 M~rektinekgva;
2-- f~odik~t~k~ya, 3-- Marektakan~kaya, 4-- Verkhn~i~C~t~kaya ~Upp~r IkatJ,
S-- 11~hilindin~kaya); 13 bagin~ of th~ Cran~itionai (from Tran~b~yk~1
to gaykal) type; 6-- Vitimkan, 7-,- Nizhn~ikie~k~y~. The disloceeiong of
chp brenk in eontinuity: 14 ~~ismiceily activ~: a-- e~tabl3~h~d, b--
nrorn~ea (I-t Ul~n-Burginekiy); 15 active in ehe C~noznic (a
establish~d~ b-- propo~ed); II-II Marektanakiy, III-III Garginekiy,
IV-tV bzhorgolant~-N~rungdinskiy, V~V Vitimlcanekiy, VI-VI
ikatskiy; 16 rteeoc~nozoic (a e~Cabliahed, b-- propng~d): VII-VII
Podiknt~kiy; 17 pre-Cenozoic (g establ~shed, b-~ propo~~d),18
a) normal faulte, b) overthruets.
Key:
1 t 1c~ t
? Vitimkan
~ Carg~ .
of Arshan and Yelovskiy spur, the triangular facies along the front of
the Tunkinskiy bald peaka and the line of mineral springs at their foot
(~lorensov, 1960). Recent and modern eei,smic Activity of the Tunkinskiy
strike-slip fault is confirmed by the association of an entire seriea of
epicenters of weak and atrong earthquakea and ~lso seismogenic structures
with ics zone.
The Tunkinskiy fault has feathering and accompanying fractures of gignifi-
cant extent. The southern branches of them are buried under the loose
series oE the bt~9in (SEISMOTECTONICS...~ 1968; Zorin, 1971). The morpho-
logical expression of some of them in the cryatal bottom of the depression
� ran indicate their Cenozoic activati.on. This pertains primarily to the
lar~esc transversc~ Kyngargskiy ~ratcture Which obliquely cuts the Tunkinskaya
br~sin with respect to the Arshan meridian (Sherman, pt al., 1973). The
Irkut branch oE the Tunkinsk~,y faults separatinq the mountain massif of
*iunku-S.zrdy Cape (abs~lute elevation 3493 meters) from the lowland Western
side of the Tunkinskiy bald peaN.s has cleur traces of Cenozoic re~uvenation.
One of the feath~ring ~ractures has a crushing zone of up to 200 meters.
1t is br.~nched from the Irkut fault in the section near the fork of the
Chernyy Irkut and Belyy Irkut Rivers. Extending along the northeastern
331
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I~OIt OI~tCIAI, t15t ~DNLY
apurg o~ t~tunku-5~~rdyk mdunt~in, the f~actu~re ig clearly ~xpre~g~d in th~
relief ~nd h~g n gtrtke td the narth~a~t 7bd. At gn ~l~v~~ei,dn ~f 2000 td
7SOtl mee~rs ehe fr~rture i~ rnot~d glnng the ch~ing of num~rau~ 1~nd~lipg
and ~lg~ pxe~ndpd ~e~r~s and er~n~h~~ (Shmotdv, 1972~ Shconenko, V� et ai.,
1971; S~iSMnT~C'CONiC5.~., i975a)~ On ~ne~rin~ eh+~ Mondy ba~in, ehe Irl%ut
f~ult bran~hea. One of i~~ brenehe~ i~ tr~c~d ~long th~ north ~ide ~f thp
b~gin, th~ ~ther, judging by th~ C~cConi.c gr~rrg, ig w~11 vi~ibl~ on eh~
~~prini photo~r~phg. ~t ~xt~adg to the gdu~h~~se ~o fhe faot nf th~ Kh~m~r-
U~ban ridg~. `Che trgcp~ ~f th~ 1~t~~t mdvementg h~ve b~en ~gegbiighed
pr~domin~ntly in ehe northe~rn fodehill s~~ti~n of th~ bg~in. g~gittnin$ with
Kh~rn-Uab~n ~nd tn the w~st~rn pxCremity r~f the Mondy ba~in, ~ldng the fout
t~f the mountain~ th~r~ i~ ~ chute~lik~ d~pr~~~ion (gtrike ~ximuth 300�) frnm
1d0 ta ~OU m~terg wtde whi~h follaws the Mondy-Khare-Daban ~nciene fauit.
Itg re~~ne r~~uvenation is pruv~d by ~~Wath of mod~rn ser~~m~ end ~h~in~
nf gmn11 lgk~g (Shmotov, 1971; Solon~nko, V., et ~1., 1971; S~~SMOT~C'~dN~C~...,
1~75n).
The spries nf recciline~r gc~rpe and trenchps up ~0 80 m~C~rg depp ~nd up Co
5 km long ig obg~rved in th~ mountgin cnmmi~gure between th~ Mnttdy ~nd the
Khoytngol'~k~yg bnsins. Int~rsecting, the riftog~nic f~ultg which brpak up
thig mountain commiesure converge her~, gpproaching from oppositp directiong.
There is no doube of the increased eeismic dang~r of such aectic~ng
(ACTIV~ 'f~CTONICS..., 1966; S~I5MOT~CTONICS..., 1968, 1975a).
On the left side of the Irkur Riv~r valley near Khara-Dgbgn, Che superposition
- and ir~tersection of the ancient overthrUSt by the riftogenic jointg is
clegrly observed, Which demonstratea the n~ot~ctoni~ r~arrangement of the
gtructural plan exigring here (Solonenko, V., et ~1., 1971; Shmotov, 1972;
S~I5MOT~CTONIC5..., 1975a). It wag noted above that in the eastern pgrt of
the Tunkinskiy basin the fault With the same name follows the zone of the
ancient overthrust.
In the vicinity of the eg~Cern closure of the Torskaya baein, the Tunkinskiy
fault has not been morphologically established. Betaeen the Vystrinskaya
(Vystra) and the Soythern Baykal basina, the zone of the Obruchev fault alsa
is not expressed in th~ relief, and in the Southern Baykal basin, the main
i rou~e of this fracture has an underwater continugtion.
The study of the underwater rclief of the bottom of Baykal Was undertaken by
B. F. Lut (1961~~ b~ 1964) by the method of deep water echo sounding, which
macle it possible to discover an entire geri.es of gernoorphological ~eculiar~ ~
icies of the bottom of the lake caused by the neotectonics. In particular,
~he large, a Lnost cantinuous extent o.f the sh$rply expreased sinueus under-
w.~[er scarp around the West bank of the Southern Baykal Lasi,n was confirm~d.
The steepness o� the deep xatex slope of the lake fonaed by the displacer
surface of the Gbruchev fault reaches maxir~um nagnitude (60-~70�) in the
vir.inity of Kolokol'nyy Cape, The gravimetri,c data interpreted by
Y~~. A. 7.orin (1971) indicate the same thing, in accordance With Which the
Obruc.hev fnult has an amplitude to 4000.ti5~00 meters, and its displacer is
332
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inclin~d in th~ dirpctidn nf th~ b~~in ~t ~n ~ng1~ fr~m SO tn 9U�. In the
dpinidn of Lut (19b4), g gh~iloW v~t~r ~~cEion ~d~~~~nt tu the
t~i~tvpnichnyy Cap~ ~xp~riencQd block ~ub~idpnc~ ~ioag th~ faul~. Th~
dieplacemente of th~ bi~ck~ in Che vicinity of ~h~ Obruch~v faulr wer~
estnbliah~d in the und~rwae~c p~rt~ of eh~ Primdrekaye gnd the t:rasnoy~rov~k~y~
~~i~ma~~nir ~truc~ure~. Th~ re3uv~n~einn (pdg~ibly, hi~eoric~lly, quitp
r~~~ntly) nf th~ Obruch~evskiy fault h~g b~~n prov~d by th~ fr~~ture oE th~
enei~2nt Haykal Cerrac~~ in th~ Slyudyan~kaya Gu1f and in ~h~ Tyy~ itfv~r
d~1t~ (th~ noreh~rn p~rt ef Baylcgl). In ehp moueh di the 1ete~r, in eh~
dpinion df B. Lut, a ee~tion of th~ coagt wirh sharply int~rg~cted
grnund r~lief aa~ thrown und~r th~ 1eve1 of the 1ake. Th~ bagic plan~ of
the Obruchev fault cute off a~~rieg of rocky capes ~uch es Sag~n-M~rygn~
Kovrizhke and Luvar' on the weer bank of Baykal and Kam~n' Bekl~niy in
th~ vicinity of ~eschanoy Bay and shifte eome i~ the direction of the l~k~.
Th~ volume of ehifted rock maeeif~ reache~ 1 km (Lamakin, 1955; Lut, 1964;
p~l'~hin, 1968).
According ro th~ ob~ervations of N. V. Tyumentgev, in th~ vicinity nf the
village of Koty and the GoloueCnaya River, th~ lake of parts of the gmg11
river v~lieys cut off and thrown into the depthe of Baykal hav~ been well
nr~~erved~ V. V. Lamakin (1955) extended these abe~rvgtions to ather
eections of the west shore of Baykal.
The seiemogeological inveatigationa in recent yeare have de~onstrated that
in che recent hietorical paet, the zone of the Obruchev fault wae an arena
of powerful earthquakes. It is coordinated With the Primorskaya and the
Y.ragnoyarovskaya aeismogenic etructurea formed during earthquakes with an
intensity of no leea than force 10 and having an underwater continuation
(Lut, 1964; Khromovakikh, 1965). The Shartlay, Rita, Solontsovaya,
5rednekadrovaya [Central Kadrovaya] and Khibelenskaya seismic strucCures
of grand scale occurring during re~uvenation of the Northern Baykal branch
of the Obruchev fault by underground shocke up to force 12 are located
northeast of them. The echo $ounding of the coastal zone in the vicinities
of these aeiamic structurea demonstrated the exceptional:.; complex structure
of the lake bottom. Under the aurface of the water in a strip up to 8 km
wide giganCic blocks are hidden (up to 900 meters wide) erratic masses
up to 150 meters high aeparated by graben~like depressions to 200 meters
deep (Zhilkin, Pinegin, 1973), Theae are the frontal parts of the seismic
- atructures with their characteristic swell-sinkhole relief. The mo:e
ancient aeiamostructurea of Anga, Tonta~ S~rma, Aral'skaya genetically
connected with force 9~10 earthquakes are coordinated with the Prirrorskaya
branch of the Obruchev fault which runs along the line of the mouth of
the Bugul~deyka River to the Maloye Sea. This branch~ although it enters ~
into the Obruchev fault zone, in the Bugul~deysko~Malomorski,y section plays
- a Recondary role in the rl.ft formation~ J,nasmuch as the amplitude of the
vertic.~l d~aplacement along it does not exceed 20~ meters (Zorin, 1971).
With reapect to the set of geological~geophys~cal and seismogeological
attributes in the vicinity of the Obruchey fault the following sections
can be isolated with different aeiamic potential; 1. M~6.5-1;
333
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Ip~fnrc~ 9. 'The g~~eidn dE rh~ Prim~rskiy f~u1e betw~~n eh~ gduthwegtern
~lo~ure nf the H~ykal b~ein ~nd th~ Rit~ ~~i~m~,~ ~tru~eur~, ~he e~a~inn af
the NerCh~rn d~yk~1 f~uit north o~ the Khib~lpngkay~ ~~i~mie ~~ruetur~
and th~ Kich~r~kiy fault~ ehp Oi~khonekay~ br~neh of ehe Obruchev faulti.
2~ M~7; I~~for~~ 10 ~rp mdre, The Tunkin~kiy favle~ a~~~tidn c~f eh~
Ndrth~rn Bc~ykal faule bptw~~n thp ~Qi~m~~ ~eructur~e ~f itit~ and Khib~l~ngk~y~.
In th~ vieinity nf ehe gnuthwe~tern Gloaurp df ehe g~ykgl d~pr~ggion,
~rtic~l~tion and x-inCerg~~einn df Che ubru~hev f~ult ~nd th~ Ch~r~kiy fault
boedertn~ the depregsion on the gouthea~t take~ pl~ce. '~he clo~ur~ of eh~m
- wes est~bliehed by echo sounding in the vicinity df Kultuk 10 km fr~m the
~here. N~r~ th~ Obruch~vekiy fault ie ~plit ineo g numbpr of gt~p f~ulC~
wieh emplitudp~ nf 700, 900 and 1200 meCers. YC i~ ~hig ch~r~cteristie
"d~c~y" that expl~ins eh~ damping of this pow~rful~ ~xt~nd~d f~ult diglac~-
tion in a very ghort dietance (Lut~ 1964)~
5outh~a~t of 5lyudygnka, in the profile of the dpep water ~lop~ nf the lake
the effect of a new ~tructure b~ging to be felt ehe Cherakiy fault (see
~ig 100). Thp amplitude of the fault acarps with respect to the direction
Erom the coasta~ ahallow atrip in the direction of Ch~ lake water is 90,
180 and 300 meters (Lut~ 1964~. Then to the southeast th~ Cherakiy fau1C
is traced in the form of an underwater ~carp of 900 metere high gradually
incrensing to 300 meters (Ladokhin, 1957). The ehifts glong this fracture
pxpl~7in the inverae asynnnetry of the lnke pool in~the section between
Tankhoy and Mishikhoy. In general for Baykal coordination of the maximum
depths With the western shore is regular. However, along th~ Cherskiy frac-
ture the subsidence of the bottom of the basin takes place so intensely that
it cannat be compensated for by the gediment accumulation (Lut, 1964). In
addition, the uplifted wall of the fault here is incomparably more aharply
dismembered by the underwater canyons which have occurred along the trans-
verse and diagonal fractures (Voropinov, 1961; I:adokhin, 1957; Lut, 1964).
They bound the horat and graben atructures marked by high seismic activity.
On approaching the Selenga River delta, the Cherskiy fault is aplit into
twa independent branches. One of them runs into the internal part of the
dclta, and the other passes along the delta front. The morphological
peculinrities of these fractures have been discussed in quite some detail
in recent papers (Lut, 1964; Solonenko, V., 1964a; Khromovskikh, 1965;
SEiSMOTECTONICS..., 1968). On the periphery of the Selenga River delta
there is articulation of the Cherskiy fault zone with the GolousCinsko-
Kukuyskaya underwater structure (Lut, 1964~, which is the intrabasin heaving -
of the crystal basement. In the bottom rel~ef the Goloustinsko~
Kukuyskoye uplift ~.s in the form of two promontories up to 1000 r~eters
high having northeastern orientaition~ One o� them extends from the
Kukuy Cape on the periphery of the Selenga River delta in the direction -
of the west bank along the traverae of the Goloustnaya River. An analogous
promontory runs from the northeastern patrt of the Selenga River delta and
wedges out into the central basin of Baykal,
334
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~Olt nF~tCIAL US~ ONLY
T'hi~ r.h~raeeeriet~,e und~tw~e~r r~dg~ ~,n ~eru~eur~1 r~~r~~tg i~ ~ nne^w~y
hnrat, an th~ ~~~t (frane~l) ~i,de b~und~d by th~ �~ule, ~nd on rh~ we~t ~id~~
by the b~nd~di~lncneiene (tue~ i961h, 1964~~ In nur opininn, ie ig mnre
~n~iCal t~ cnn~id~r ie eh~ Wee~ern bound~xy o~ eh~ Obru~h~v f~u~l~ zo~ie~
~'h~ northe~~ee~tn ~nntfnuation o~ ehe ~rontai f~uit di th~ Gn~ouetin~kd-
Kukuy~kay~ mdrphn~tructur~ is the S~lenga fault ahich ~nt~r~ ineo the
Cher~kiy ~ractur~ zon~ C3Ei5ftOT~CTONIC3
unique fr~cenr~ i~ ~rov~d by nwnerous outcropg6of~th~rm~lC~pring~~gnd~eh~
ednC@ntr~tion ~f ~~rehquak~ epic~nter~ in the limbg of th~ G~lougtin~ka-
- Kukuyskay~ gtr~ccur~. 'Thp northpast~rn br~nch C~gt~bligh~d ~mplirude 15 m)
nf th~ fr~cture w~~ r~~uv~nat~d during ehe fnrce 9 Cent~~l Bayk~l parthqu~ke
tlf 29 Aupuet 19S9 (Solon~nko, V., '~r~gkov, 1960 .
~oint wee ~ccdmp~nied by roiling o� th~ water in thehform oftaolineerhbelt
_ ~f noreh~agtern orientation. The ~ther pare of the inveerigat~d und~r-
wet~r marpho~truceur~ is formed by th~ tectoni~ gepp eh~ uplifred w~~tern
wg11 of the fault running from th~ Kre~tovekiy Cape in th~ direction nf the
Seleng~ River delea. The gmoothed eurface of the bdttom of th~ lake trnc~d
from thp mouth of the 8ugu1'deyka River ia bro~;en her~ by a al~arp gcarp mdre
t~,en 150 m high (Lut, 1961a, 1963, 1964). Acco~cding to che or,ql rpma~rks of
Yu. A. zorin, these low-amplitude fracturps in th~ crystalline basement
onnthe propoeeddetru~turalmdiagramsf(zerinmp197j therefore they are abeent
whole to the entire GolouaClneko-Kukuyelceya morphostructurerinaemuch gee
possibly a eignificant part of its uplift amplitude ($00~1000 m~tere) ie
not connected with movementa along the fault but is the result of the
eroeion-accumulative activity of the Selenga River i~ the frontal part of
the formed delta againat a background of general do~,mwarping of the Baykal
basin.
The uplift along the Cherskiy fault of the north limb of the Khamar-Daban
arch in the latitudinal segment of the Southern Baykal basin during the
Qu.~ternary period hardly exceeda 250 to 300 meters (the maximum heighc of
the Quaternary lacustrine terracea). The overall acale of vertical move-
ments along this fault could reach maxi~aum for the vicinity of the Southern
Baykal baein with a magnitude that ia on the order of 8000 meters. Un to
5000 metera of this in individual aections could be the "pure" amplitude
of the Cherakiy fault.l In this case; the same law ~s retained as for the
Bayk~l branch of the Obruchev fault; the ma~c~pum diaplacement along the
fault decreaees not in the $ecending moyements but i,n the descending move-
ment~a of the blocka of crystall~ne aubstrate, and therefore these deep:
suturea more promote the formation of the basin than the positive morpho-
atructures bordering ~t,
1Thc amplitude of che bACkground downaarp~ng of the bottom o� the Ba k
basin undoubtedly reaches a signifl.cant value~ but at the present timegi
it i8 1mpoASible to conaider it quantitati.vely.
335
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~dit t~~~tCtAt, U5~ ONLY -
7'ha Udc~knn Eault ~ygtCm ig prednmin~ntly ~ gubl~Cieudin~l ~y~tem nf npo~
teetnnic frdCeure~ dc~uxrl,ng ag ~ r~~u1t ~f eh~ invdlv~m~nt of the we~t
f1~nk nf th~ znc~e ~t th~ Stnnovoy d~~~ ~uture in eh~ pro~p~~ of rift
~~tivetion (AC'CIVC T~CTON~CS~.~~ 1966), ~e run~ morp fh~n 200 1an prim~riiy
dldng ehe nbrth~rn fddthill~ di the Udek~n rid~~~ N~w~v~r, ~ numb~r of
l~rg~ fr~~tur~~ making iC up (N~mgrgkit~kiy, Chin~-Z~kaegkiy) ~re in th~
bddy of thig ~r~h-b1~~k up13f~, conerolling the dev~lopm~ne of th~ mnrphn-
geru~Cur~~ ~f differ~nt ord~r~~
In ~pite of the Compl~x, brgnched pl~n cdnfi~urstidn, th~ Udok~n ~ygtpm nf
di~l~cationg aieh a bre~k in conrinui~y ig ch~racterix~d on th~ whnl~ by
echplon ~tructure predomin~ntly wieh sublatitudingl and northea~terly gerike
df Chp individu~l ~~helon fraceur~g 15 to 60 km long. Compl~xly differ~n-
Ciating the axial part di th~ ri�t zon~, ~e the sam~ tim~ th~y defin~ Ch~
develnpmenC of th~ geru~turp~ diff ering with re~pe~C to th~ir mnrphr,g~n~tiC
p~ruli~ritip~. N~rp tihe type, rate and dir~ction of th~ geiamoteCCnnic
movement~, a~~d aecordingly~ Chp level of Che poC~ntigl g~igmiciCy are
diff~rent for th~ individual fractureg and even geCCic~ns of them. The
high~at geismic patential chnracteri~~~ the fr~cCures contro111ng the
embryonic bgeins Namargkitekaya, Eymn~lchgkaya, Lurbunskaya, and so on.
The main fracturea of the Udokan ~yatem are th~ Namarakitgkiy, Kondg-
~ ~ymnekhskiy, Dovachanskiy, Lurbunskiy, ~megachi-Kem~nskiy nnd China-
Zakatskiy ~see Nos 82-87 in ~ig 106).
Th~ Namarakitskiy fraetures located on the south limb of the Muya-Ch~ra
int~rbagin mountnin commisaure, running in the sublatitudinal direction
(75�) from the Taksima River basin to the Uurelag River. Along the entire
extent (35 lan) it is clearly expressed in the relief, controlling the
south side of the Namarakitskaya embryonic basin.
The west flank of the fracture breaks down into parallel echelons. The
northern echelon running about 12 km bounds the complexly differentiated
bnttom of the western part of the Namarakitskaya basin on the south. On
the souti~ limb of the fracture there is a block of the first stage of the
uplift of the Udokan ridge with an absolute altitude of 1200 to 1300 m.
The apparent amplitude of Ct~e vertical displacement along the fracture is
~pproximately 500 r~etera.
~ 'fhe southern echelon 25 km long separates the first stage of the ridge and
che bottom of the central and eastern parts of the basin from the high
meuntain, so-called Tundakskiy block uplifted to a height of up to 2500 m.
The fracture extends here predomi,nantly along the rear suture of the
pedest4l of the ridge and disappears ~.nto the right bank of the
Purelag River~ The amplit;:~le of the vertical displacemenc reaches 800 to
900 meters~ The displacer ~lane dipa steeply to the north~
'Che west flank of the echelon which runs more than 10 km underwent Holocene
rejuvenation. The deposits of the side moraines of the lake glaciation
336
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~Ott d~~~C~AL US~ dNLY
and divide c~pe~ nf ehe l~fc eribue~rl,es ~f eh~ Ngmgraki~ Riv~r w~re
brdkcn ~nd di~pl~ced. 1'he height of th~ f~ult ~carp r~~ch~~ 10 m~ter~ ~eh~
bn~in w~ll ie down~hrown).
In th~ w~~e, in the headwaterg of th~ N~rund~kan Itiver (th~ T~k~im~ River
hn~in) th~ gouth ~~hplon ie cut by the exCended (mdr~ ehgn 80 km) 'Cgk~im~-
Uzhilindin~k~ya fault xon~ (eQe No 8~ in ~ig 106) bounding the Kokar~v~k~ya
and Tak~im~ b~~ina on the ~outh~aet No 56~ S8 in ~ig 106)~ The z~ne
i~ ori~nCpd in rh~ norCh~g~t~rly d~rQ~tion ~nd on the eagt boundg both th~
_ b1oCk of the first ~t~ge of th~ uplift of the Udokan ridge ~nd, gppgrently,
the northern erh~lon of the Namarakitekiy fracture.
Th~ ~pic~nter of th~ forc~ 10 to 11 Muya ~arthquak~ of 27 Jun~ 1957
(rt$7~9~ center d~pth 22 km) for wh3ch the re~uvenation wa~ exp~ri~nc~d by
two echelong of the Namarakitskiy fr~ctur~ was coordinaC~d ~airh th~ vi~inity -
of the ~rticulation of thege fauit~ (north ~imogt completely and soueh
extending 14 km). The ~eiemogenic movament along the fault bnr~ on the
whnlg the nature of e l~~t etrike elip~ and the rt?tio of the hori,zantal and
_ vertical ~isplacemente was approximately 1:3 (ACTIV~ T~CTONICS...~ 1966)~
Thus, th~ Ngmarakitsl~iy fault ie a clegr ~xample of the fracCure structures
cdusing the development of the embryonic baging for which, as wae demon-
~trated above, the higheet level of seiemicity ie ~h~racteristic. The cnmbina-
tion of paleoeeismodislocations~ modern dislocations cau~ed by the Muya
earthquake and th~ extraordinarily active epieentral field in this fault
zon~ makeg it possible to define its maximum seismic potentis~ ga force 10
or more.
The Konda-~ymnakhakiy fault extending about 100 lan has general sublatitudinal
strike. It is located in the vicinity of the Muya-Chara interbasin
commissure, participating in the formation of the Kuanda and the Eymnakhskaya
embryonic hasin. By its weet flank rnade up of two parallel echelons of
northeasterly atrike, the fault penetrates deeply into the body of the
5outhern Muya arch-block uplift, complexly differentiating it into the
positive and negative morphostructurea of higher orders. On the we~t the
lgtitudinal branch of the Muya-Tokko fault eystem departs from it, in this
way realizing the connection of two regional lineaments. The narrow low-
land commigaure located betWeen them is involved in slow aubsidence, pre-
paring the merging of the Muya and the Kuanda basins.
Farther to the east, the Konda~Eymnakhskiy fault in the form of the clear
contrast fault scarp bounds the Kuanda basin on the south~ The total
~mplitude t~f the vertical diaplacement reaches 10U0 meters (without consider-
ing the plunge of the basement of the basin2. A large thermal spring
(T~F42�C) is aeaociated with the fracture. The one�~sided horst of the
Nnmarukitskiy massi� located on the south wall participated in the movements
during the Huya earthquake of 1957~ Which is ~ndicated by numerous surface
deformationa within fts limits and the nature of the rupture of the tayga
structurea.
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~OIt d~FICIAL U5~ di~LY
`~h~ en~t ~i.~nk of the f~uit i~ brdkett ine~ ~~v~r~l p~r~li~l ~ubl~titudingl
brnnc~hr~ ~xpr~~~rd in th~ r~li~~ by aCe~p gesrp~ ~nd e~nernlling Che mnrpha-
HCructure nf ~hc Lymnakh~kayd ~mbryoni~ b~~~n~ 'Chp Nnidcpn~ v~le~no~ ~nd
n n~mber of miner~l epringa stretch to these faultg~ Accordin~ td the
g~dlogi~nl end ~~dmnrphdl~gi~gl.attribue~~, eh~ amplitud~ of eh~ v~reic~l
di~pl~~em~nts durin~ th~ Quat~rngry eim~ reacheg 900 m~t~r~ h~r~e.
In the central ~nd w~gC~rn p~res nf the f~ult, gecti~ng df itg fr~~m~ne~ry r~-
~uven~tion ~re direce~d(th~ t~ctonic deform~tinng nf th~ g~nd geripg nf
:tiddle Quat~rnary ag~ and Upp~r Quat~rnary en modern prnluvial depnsitg).
Uuring th~ entire period df in~erum~nt ab~ervationg in th~ vicinity of th~
f~ult and e8p~cinlly on its we~eern fl~nk, high concpntratian of ~~rehqu~k~
~pie~ne~rg is eonsCgntly obe~rved~ Consi~~ring th~ ~neirp get ~f ~ttribue~~
chgract~ri~ing th~ s~i~mote~tonir A~CiV~.Cy ~f th~ �guit, it i~ po~~iblp ed
c~nsidpr thaC earthquake~ with ~n intengiey eo fnrce 10 ~r~ poegible in thp
vicinity of it~
The bnvn~hangkiy fault branch~s fr~m th~ Konda-~ymngkhskiy f~ult guppog~dly
in th~ mouth sectinn of the Purelat Riv~r, gnd it follows in ehe nnreh-
easterly (6d-70�) directton ~long the Konda River, acrogs Che Dov~~h~n L~k~e
eo th~ Lurbun Itiver a distance of up to h0 km~ In the gection fram the
gnuthwest flank to th~ Uovnch~n tak~, the frgetur~ zon~ h~g the mo~t complex
gtructure. Here ir ie made up of several ~ubparallel branches in which the
crc~sion-Cectonic Konda River valley is located. In the gouCheasC~rn limb
there is a block morphostructure, the part of which near the fault is
' d~formed by numerous accompanying and f~ath~ring fractur~s forming the
pologenic Dovachan seismic gtructure taken together (Solonenkn, V., 1965;
ACTIVF. TECTONICS..., 1966). One of the sublatitudinal faults feathering
the Uovachan fracture intersects the axial part of the block at a distance
of more than 20 km (the southern fault~graben).
The overwhelming ma~ority of the disturbances of the atructure of ancient
occurrence has the nature of faults, gometimes with left shift. ~ach of the
frnctures is characterized by a mnre or lesa steep, high scarp in Che
reli~� and is confirmed by the geological observations. The seismogenic
movements of the Upper Quaternary and Nolocene time occurred more than once
along it. One euch earthquake with an intensity of no less than force 10
occurred in the eastern part of the southern graben fault several decades
ago, and the last earthquake (M~5.2) on 6 February 1975.
The long~preserved activi.ty of the Dovachan fault zone~ the traces.of recent
seismogenic rejuvenatioa and the high concentration o� earthquake epicenters
(especially in the southwestern part) permit estimation of its seismic
potential at force 10 or more,
The Lurbunakiy and the Nizhneinga.m~kitsk3y faults are made up of series
of subintitudina~l echelons connected by means of northeasterly shears into
a united zone controlling the Lurbunskiy graben and the Ingamakitskaya
rml~ryonic bnsin from the south and southeast. Its total extent is 50 to
60 km.
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~a~ o~~ic~at, us~ oxi.Y
'Phe fnult ig e1~drly ~xpr~,~~~d in th~ reli~~ by eh~ as~~p ~~5~40�) f~uir
~C~rp~ ~On~900 metere high. Con~idering ehe thickn~~~ n~' Ch~ in~~~
d~pdgice in th~ ba~in~, ehp tot~i ~tmpll~ud~ of th~ v~reieal digpi~c~m~ne
along ir reaeh~~ 1000 met~r~. Her~ thp m~xi,mum di~pl~e~m~nt~ (600~700 tn)
b~iong to the Upp~r Plei~tae~ne to Noiocene C50~,U00 ta 600~000 y~~r~),
whieh i~ ~~tabli~h~d by th~ differen~e in ~1~v~eiona of ehe fooe of ~he
tow~r pl~iatoc~n~ bg~alt fiow 3n the Ing~rn~ki~~kay~ 6a~in ~nd on th~
Se~l~vny mountain~ Th~ 1a~t mov~m~nts in th~ turbun~kiy f~uiti zon~ oc~urred
no mor~ Chan hundr~d~ of ye~rg ~go Cth~ Nizhn~ing~m~kit~kiy ~e~ueture).
Coneidering the degr~e o! inteneity di th~ m+~vem~nts ~lnng th~ ~~ule in thp
Late Cenozoic, the ~~iemog~niC mobility of the zone in the Nnl~e~ne ~nd
th~ reiativeiy high mod~rn eei~mic ~ctivity, it ie correct to conaidpr tha~
e~rthquakee can occur her~ wi,th an intensity eo f~rce 10~
Th~ Ching-Zak~t~kiy faule in ehe form of ~ singl~ laCitud~nel line~r ~nn~
i~ tracpd frnm the upper Ingama~:it River to Che Kalar ftiv~r (~bout ~0 km).
In eh~ weet ie is suppoaedly roupled with the ~ystem of rifrogenic f~ultg
bordering the Lurbunskaya embryonic ba~in~ niagonaily int~rgecting the
U~ok~n arch-bl~ck up~ift, it rontrol~ the neotectonic strucrur~ of the
Up~,~r Ka1ar eubrift basin on th~ ~outh her~~ In the Qast his fault mergeB
with th~ aativated zon~ of the Stanovoy deep euture.
'The p~rtial fracturee making up the China-~akatekiy fracture gy~tem ha~
predominantly sublatitudinal and northegse~rly ori~ntation. In th~ vicinity
of ch~ sh~rp bend in the lower Ingamakit River and on the eagtern flenk,
lar~e f~athering of fractures brench off it to th~ northeast (the northern
br~nch and the Chepinakiy fracture). All of theg~ t~ctonic digt~rbanc~g
are clearly expressed in the relief; the Late Quaterngry movements along
them frequently cauae significant rearrangement of the geomorphological
appearance and the hydrography of the territory.
On the West flank, the fault in the form of a sr~rp 10 to 15 metere high
cuts the cover of the Uiu~;~,.~ plateau basalts. Th~ alag cones of the tao
Vakgtskiy extinet volcanoes~are dir~ctly coordinated with it. On the 2eft
slvpe of the lower Ingamakit River vall~y in th~ Chineyskiy gabbro-
anortho~ite pluton fiQld, the fault is morphologically expregs~d by ~carps
20 to 25 meters high~ replacing each other in echelon form.
In the vicinity of the lower Ingamakit River ahere the northern branch
separacea ~rom the China-Vakatskiy ~ault, the vertical nwvements along the
Eault have led to sharp rearrangement o~ the river network, as a result of
which the headaaters of the China River h~ve enter~d the los~er Ingamakit
bASin. The subsequent erosi,on has obviously occurred using the gaping
tectoni~ ~aulte, and at the pxesent time the loaer Ingamakit River and some
of ita trl.butaries have deep xectilinear canyon-like valleys up to 1.5 km
long and up to 100 meterst
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~a~ n~~~Gint, us~ d~t.Y
~a~t o~ the i~W~r inggm~kit Riv~r, thp bagiC route ~f the Chin~-V~k~t~kiy
f~utt i~ ~hift~d ~am~wh~f th~ ~du~h ~nd ~~cryuirp~ ~ diff~r~nf r~~ructur~~
In thi~ i~eetian eh~ E~ult baund~ th~ Ghin~ ~mbryanic b~gi~ ~nd i~ ~ixpd dn
ie~ ~auEh ~ida by ~~h~in aE e~eeanie ~~ddl~~ ~r~d rr~nChes, mdr~ rar~ly th~
gg~~r ~~~rpp ~p te 4~o S m~e@r~ high. in pian th~y r~pr~~ene ~~y~eem of
~cMei~n eyp~ fr~eeur~~ fr+~m ~.S eo 5 km 1ong.
On ~h~ p~gt fl~nk, in th~ vi~ini~~+ ~f thp upp~r K~1~r ~ubrift b~~in, th~
Chin~-V~k~~ Eault i~ digCOneinuo~~. H~r~, in individu~i ~~e~ion~ of ft thp
- gi~ng df f~u1t and fault-~~hift di~pl~cements gre not~d. '~he ~mplieud~~ df
th~ v~rri~~1 mov~m~ntg r~g~h 10U-150 mpt~r~, and th~ hdriznnt~l mov~mpntg,
th~ fir~t e~n~ of mpt~r~. Th~ g~~tions af m~ximum plunging of th+~ b~g~m~nt
bf ~he b~~i~ ~nd ~~~iv~ ~~dim~n~ ~c~umul~tion ~re ~oordin~f~d ~tieh eh~ f~u1t
~dne (th~ ine+~rfiuve ~f th~ Solot~y ~nd th~ Uert~~, the Amudig L~k~ d~pre~~i~n).
'Ch~ m~teri~l compo~irion of th~ rnCk in ~h~ vicinity nf the Chin~-V~kgtgkiy
f~u1t indicat~g itg en~i~nt pr~-C~mbri~n ne~urr~n~e. The ~1~ar ~xpr~ggion
in eh~ rpltef indicqtp~ th~ re~uv~ngtion of th~ te~tonic mov~mene in the
~u~ternary tim~ ~1on~ ft. 'Ch~ r~juv~enacion of thp tectoni~ zon~ in th~
post~~lacial ~eriod occurred in the flank s~ctians. In the w~st the camplex
df r~~idut~l a~i~mogpnic d~~ormationg With a total extpnt of 43 kn (China-
Vnkae~keya pal~ugeigmegenic structur~) ig suppo~edly COfl11ECt~d H~[tl rh~
pl~i~eoseism region of the force 1p to force 11 ~arthquakes of 2~ebruary 1725
(AC'fIVE T~CTONICS..., 1966). 2n Ch~ ~agtern clogure of the upper Ka1gr
bngin the traces of the Hnlocene (first thoue~ndg of yegrs) movement~ have
b~~n ~~tabligh~d in th~ vicinity of the Chepa fault (the pal~oseiemog~nic
Medved' gtructur~). Thue, the geismic pdtential uf the China-V~k~tgkiy fault ~
zone is egtinsat~d ~ccording to p~leosei~mngpological data at force 10 or
more. 'The epicenCeral field.of the last decade encompag~eg only the western
part of the fault, and the resc of its path ia almoat seismically passive.
Tran~itional Morphostructureg BetWpen the Baykal Rift ~nd Transbaylcgl -
glock-Wave Zones
Along the southeestern edge of ~he Baykal rift z~ne there is a characteristi~
set of morphostrucCural elements developing on inter~rtion of ehe movpments
of the riftog~nic and Tranebayk~l type. The farther from the axia of the
Baykel rift, the l~ss the rift atrpss field ig f~lt, and the bending defora~a-
ti~ns have predominant significance in the d~velopment of positive and nega-
tive morphostructures. The outlines o� the basins on the uplifts are
hturred. Their articulation zones are smoothed; in the ma~ority of cases
the concrast is poor, and the �racture strurtures play a secondary role.
Amanp, the positive morphostructures~ the arched upli~ts predominate. Here
the lnrge arches (for example~ Khamar-D~ban, Ikatskiy, Udokano-Kalar) have
a cnmplex structure. The fxontal parte o� the uplifts turned toward the
rift structures experience sharp rearrangement, pxedomi~antly as a result
o� the degcending (riftogenic) movemencs~ As a rule, they are sharply
differentiated. and on the seismotectonic level they anproach the morpho-
genetic type o� the arch-block upli�ts of the Baykal-Stanovoy zone. At the
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~OR O~~i~IAL U~~ ONLY -
g~m~ eim~, nragraphi~ally the~~ ~ecti,~ng gr~e conne~red wieh large mg~giv~,
wenkly di~�@r~neiaCeci ax~~~~ the Cectonic m~vem~nt~ in which d~r3ng ~h~
herind of MB~ocen~zoi,c activat~,on w~re manif~erpd in rh~ �orm o� a siow,
g~n~r~l ri~e cau~ir?g prpdominance ~f hending deform~tion~.
Th~ n~g~~tv~ mor~ho~tructur~~ a1~o havp eh~ract~ri.eri~ Cr~n~itinngl develnp-
m~r~t~1 f~~eure~, and on the aho1~ th~y b~lnng to eh~ eubri�e b~~in type.
Tt1EHE trough~ wieh gharply dimini~h~d rete of downwarping ~nd thickn~~~ di'
Che C~nozoic depneit~ obvinu~ly exhibited activgtion simulCgneously w3.th -
- th~ large riftog~nic baeina, but th~ proceP~ of their development proceedfi
much mor~ ~low~y.
Let us con~ider ehe most characteriatic exampleg of theee tran~itional
morphoetructures.
pdgifiv~ M~rpho~eructur~g
~'h~ gtand~rd ~tructurea of this morphogenetic aeriea are ehe arched uplifts
di tlie Khamar-Dgban and the Ikat ridges.
The Kh~m~r-Uaban ridge frames the Tunkinakaya and the Southern Baykal rift
- bnsins ~bout 350 km to the south and aoutheast. WiCh reapect to its mnrphn-
~tructural peculiarities, it is nonuniform~ The weatern and northeastern
Khamar-Daban are characterized predomi~antly by the features of arched
upltfts, and the Central Khamar-Daban~ by the arch-block uplifts.
On the whol~, the ridge is aeymmetric; the height of its top surface
in~r~~ses sharply from the direction of the rift zone, reaching 2200 to 2300
meters (maximum height 2758 meters). In the highest part of the uplif t,
sections of the volcanic platesu gnd Tertiary peneplain with gently sloping
wavy relief were retained. Theae fragmentally retained relicts of the
ancient denudation eurface outline the arched uplift somewhat flattened in
itg axial section. Its maximum is coordinated with the central Khamar-Daban.
ilowever, the bending deformation f irst noted by V. V. and N. V. Lamakin
has been best noCe6 in the western Khamar-Daban along the slope of the
- lava platpau.
In general morphological appearance o� the uplift of the Khamar-Daban r;dge,
the stepped nature of the relie~ has been poorly noted. This indicates
insignificant participation of the lateat �aults in the Pormation of the
nrch and in ita internal dif�erentiat~on. The Baykal zone of the central
Khamar-Daban where the Cherski.y fault has a noticeable effect constitutes
an exception~ Here. ~,n the axial part of the upli�t close to the $aykal
1With respect to its morphostructuze and seismotectont,cs, this part of
Khamar-Daban esaentially helong,a to the arch-block structures of the Baykal-
Stanovoy zone. r
~
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bn~in num~rnu~ ~eiemogeni.c fractures nre concenCraeed which are connected
- with Ch~ ~axGhquakea oE the recenC paet o� force 10-11 (Solonenko, V., 1963a; -
_ Khrnmovskikh, 1965; S~ISPtOTECTONICS.~., 1968). Thia zone of high-act3viCy
contains direct proofa of Che growth of ehe Southern Baykal rift basin as
~ r~ault of rupture of the highly upli�Ced parr of the arched morphostruc-
eure by ehe descending (riftogenic) diaplacements of the individual blocks
of ehe earth's cruar. Here an importanr role is played not so much by the _
Cherskiy fau1C zone as by the faults feathering it having ground continua-
e3on in the form of fault scnrpa, obliquely intersecting ehe norChern frontal
pnrC of the cenCral Khamar~Daban.
Thus, in th~ investigdted parC of Che arched uplift of Khamar~-Daban the
clevelopmenC process proceedg in the direction of sharp complication of its
inCernal field. The high seismic poCenCial, in addition to the numerous
seismosCaCiatical data, is confirmed by traces of the greaC seismic
disasters of the recent past the Solz~n, Badkha, Khara-Murin, Snezhnaya
structures, and so on (Khromovskikh, 196.�'~).
Accordingly, Che potential aelamiciCy c~f the frontal part of the Khamar-Daban
urch turned toward the rift zone appea~~:s to be high, and it reaches a
maximum (forcea 9-10 or more) in the central Khamar-Daban. In the remaining
- part of the arched uplift, moderate se~.smic activity is noted, and the
possible maximum earthc~uake atrength is estit~ated at force 8(KmaX~14)~.
The Ikat ridge downs the Barguzin rifC basin from the southeast, and 3ust -
as the Khamar-Daban uplift, it has inherited feaCures of the ancient
plateau (smooth forms of masaive divides, broad development of the planatic;n
surfaceg, and so on). -
The outlines of the transitional boundaxy between the Ikat arched unlift
and the Barguzin rift basin are sinuous and blurred. This nature of the
pedestal zone of articular, the absence of the latest tectonic strikes in ~
it, the so�t and smoothed forms of the relief indicate that the bending
deformations play the basic role here.l
On the whole, during the formation of the morphostructure of the Ikat arch
the inheritance was manifested in predominance of the retarded general ~
uplift which predominantly caused a flexible nature of deformations. Never-
theless, the ~rontal and axial parts of the uplift turned toward the rift
zone experience complex block differentiation (see Fig 107) connected with
the active development o~ the largest, latest fractures Garga, Argoda, _
- Ulan-Burga, Marektakansk~.y, and so on (SEISlfOTECTONICS~t.~ 1968)~ The
lines of these .faults clgarly expressed in the relief are located at an ~
acute angle to the strilce of the Ikat axch and complicate the morpho-
lIn recent times thP linexa epicentral zone was discovered. S. I~ Golenetskiy
considers that it can be c'onnected with the fault sti.ll not emerging at the
surface of the earth (see Chapter VIZI~. -
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~tructure of it~ ~~ntr~1 gnd ri~t p~zt~ by the ~uperpo~~d bldck di~pl~e~-
m~ntg. 'Che nneed ~nule~ g~n~ral nnrthpg~ti~rly ~erike ere expresged in
the rplief by ~rAeion of' tectoniC ~carpa �rom 25~50 to 150~~00 meeer~ high
exrc~nding ~ev~rnl t~ng of 1(ilom~t~re~ Som~ of them control the develnpment
of the embryonic bgeina MarekCakangknya~ Podikee~k~ya~ V~rkhneiknt~knyd~
Ulan-Burga. Thus~ these igreet f~ults~ whi~h hgve n 1oca1 natur~ on th~
_ ~cnl~ flf th~ ~nCire uplift c~uae th~ arch-~block nature of ite centrgl pgre.
'Che s~igmotectonic peculiaritiee nf thte pgrt nf rhe Ik~t arch erp glgo
connerted with the compl~x block differentiation. Thus, in ~piCe of th~
high mndern aeigmic activiCy (Ald about 1.0), this territory is in prncti~e
free of traceg of reCenC dieaetrous earthquake~; there are no macrogei~mic
, dnt~ ~bout Chem since the begicttting of Che 19th cetttury. rC is Cru~ thgC
snm~ nf the fracture~ clearly ~xpreeeed in the r~li~f (Ulgn-Burga~
_ Mar~ktskanskiy, Argodo) eomeCimes carry eigne of aeismogenic mdvementa
occurring in them, but the sources of these mov~menCs obviously run d~~p
into the Attthropog~ne. Of th~m thz Ul~n-Burga faule hag the greatest sig-
nific~nce for e~tim~ting Che potentigl seismiciCy. in iCg viCinity earth-
quakes with an inCensiCy to �orce 9(M~7) ~re poesible. The same potetttinl
cc~n be propoaed also on the whole for the 8arguzn complexly differ~tttiat~d
part of the Ikat arched uplift. Along Lts periphery, along the fault zoneg
contrnlling the developmenC nf the subrift basins (Verkhne-TurkinskayA
(Upper Turkinekaya]~ Vitimknnskaya (VitimkanJ), etructures have been
tsolnted with which the connection of earthquakea oE an intenaity to
_ force $(M=5-1/2 to 6-1/2) is possible. For the remaining territory of the
Ikat arch (about SOr of the area), the occurrence of force 7 earthquakes
is possible (!il4-3/4 to 5-1/2).
'Che sections with clearly expressed arch-block mor~hostructure of the Ikat
uplift are distinguiehed by the constantly high modern seismic activity.
- Here the analysis of the numerous weak shocks and earthquake trenches have
madc it possible to discover Che characteriatic of the center zones separated
- in the section of the earth's crust with respect to the nature of the
mechanisms (Misharina~ Solonenko, N., 1972), which possibly reflecCs the
"layered" nonuniformity of distribution of the atresses in the given section
of the earth's crust.
Thus, the examples of the Khamar-Daban and the Ilcat ridges indicate the
nonuniform seismic potential of the ar~hed morphostructure$ of the
transitional type. The secti.ons of riftogenic rearran~ement of such
inherited, long developinR structures (modern basin formation, the "active"
tectonic~ zone, activated f~ults, and so on} are moat favorable for the
rccurrence of earthquakes with maxiroum intenaity. In Ghe evolution of the
~~lifta themaelves theae sect~,ons can 1.ndicate di,fferent stages of transition
from "pure" (Transbaykal) arches co complexly differentiated arch-block
:atructurea of the rift zone. On the whAle the level of the potential
seiamicity of the ~rch uplif[s o� the transitional type is moderate. The
expected mAximum strength of the earthquakea in the ma~ority of cases will
- not exceed force 8.
,
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~OIt U~~~CtAt, U5C 4NLY
Nrgntivr Mnrpha~tructuxe~
'Che gubri,ft sCrucCureg (S~1eng~Mltantainsk~y~+ Verkhneeutkingkgye,
ViCimknn, Gorbytov~kgy~~ T~ipgkan~kayg~ U~unrov~kaya and upp~r Kgldr)
ncr.upy ~n inrerm~dinee poeiCion betw~pn eh~ b~~ing of ~h~ Bnyknl and thp
'i'ransbgykal eypeg (~p~ ~'ig '100) ~ On .rh~ nthpr h~nd th~y h~ve l~i~torical-
- ~~netir COt1llt~t~Ot1 �W~.tI1 ehe Tf~anebaykal ~nd dn the evolutionary l~ve1 (~t
l~a~t tn eh~ Plei~tocen~) they develop~d in a t~ceonic eitu~tion ~imil~r
~ to them~ On th~ oth~r hand, bpginning with thp pl~igtoc~n~~ th~ d~velopment
~f th~ge tr~neitidnal m~rphngrru~tur~g r~e~ived significanC .influ~nce fr~m
the riftmgpnie rnovementg, whicM ig pxpregg~d in the inten~ificetinn of th~ir
blocl: differentigtinn, th~ involvement of th~ individugl eeceiong of the
bgging in nctive ~ubeid~nce, eeigmogenic re~uvengCion gnd the occurrence
di the 1nCegt faults in eheir borders~
The bn~ement of eh~ gubrift b~eins, by comp~rison with th~ rife ba~ing,
h~hvr. bern upllfCed (~b~oluCe el~vation 300 tn 7bb m~t~re, eomerimeg eo
l(~00 metere), nnd wieli respect to th~ Tranebayknl~ it hag been downthrown
by 2n~-40b mecers. Congidering thp amount of plunging of Che ba~ement and
che m.~ximum ~bgolute elev~Cione of Che Cretaceoue-Paleogen~ planation
9urf.7ce (2fi00 to 2700 meters)~ it is posaible approximaeely to d~Cermine
the totnl amplitude of rhe vertical C~cConic movemenC~ during the Neogene-
Quaternary period of activation, It fluctuat~s fram 1700 to 2100 meters
for the region of diffprent subrift structures. This is approximately 3 to
4 eimeg ].es~ than in the rift structurea themselves~ and it exceeds by two
Cimes the scale of the displacements in the Trnnsbaykal zone. This contrast
of the tectonic movemente as a whole agrees alsn with the velocity gradients
(~grad V~ris0.6~10'a to 1.0�10-8), the values of which ar~ much hi~her than
the Tran~baykal end low~er than the rift. Thus~ even thia approximate
analysiq nf the morphomeCric data makes it possible to describe the subrift
structures ae occupying an intermediate position between the Transbaykal and
rift structures themselves.
The accumulation of 300-700 meter series of Neogenic-Quaternary de~osits in
the subrift basins indicates activation of the tectonic movements in the
- lr~te Cenozoic. In n number of basins ('Tsipa-Bauntovskaya syaeem) the lower,
thin ~art of the aection is characterized by the Eopleistocene, predominantly
IacusCrine facies (t~e depreased molasses of orogenic fotmation). The
:~ccumulntion of,these finely clastic fc~cies occurred under the conditions
of the weak contrnst relief. The intensification of the block movements,
beginning with the Upper Pleistocene~ the increase in the sediment accumula-
tion rate caused sharp facies changea, at the same time, thicker polyEenic
~eries (orogenir. m~lasses) are formed.
T1~e uPper Kalar basin is isol~tted from the overall system of investigated
tr.lnsitional structures (ACTIVE TECTONICS~.~, 1966; Vel'yanovich, et al.~
1969). in contrast to the remaining subrift basins, it was involved from
tf~c P~leogene in intense u~li~ti.ng And during the Late Cenozoic remained in
practice inhert. This is indicated by the thin (to 100 to 150 meters)
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Fo~ ox~ictnt. t~s~ orn.Y "
digcnnti.nuou~ ~eri~a df QugCernary d~pnsitg cdv~ring abnuC 40~ di the
~ b~~in ar~~~ ~rom th~ P1ei,gtoc~ne in th~ developmene of Che upper Kg1gr '
bggin ~nme reactiv~tion ia noCed connecCed w3eh rh~ block differ~nti~tion
n� t}~e Udoknn-Kalar uplift under thp effece of ehe riftogenic mnvement~~
rhi~ we~ nl~o f~lt in an incr~aee in Ch~ Beiatnoe~ctonic activiry~ which
ie confirmed by the "reactivation" of the "F~dorovgkiy" feult on the left
b~nk of che Doroe Riv~r and the p~leo~eismogenic Medv~d' etrucCur~ formed
during the earthquakps of no lesa th~n force 10. mhe seiamoetaCieCicgl
matpriel (during a decade of obaervaCione) wiCh r~appct to the upper Kalar
basih indicgCee ite relativ~ ~~iemic pgeeivenes~r only individual earthquakes
with K~10 were recorded. Hocoever~ it ie not excluded ehat Che sei~miC
~ pa~siveness ie apparenC, occurring gfter the d3sasrroug earthquak~ of
1725 obviously connected with the China-Vakatekiy fault (Solonenko, V.,
1968b). Th~ upper Kalar baein enter~ into the "zone of quiet" in the highly ~
seismic region, and there are grounds for eseuming thaC thie zone ia a
"region of prepar~tion" of etrong earthquakes (Borovik, er al., 1971).
The subr4ft basin~ expanding the Baykal rift zone with respect to its aouth-
easterly periphery ia an additional element in the evolutiongry geries of
_ negae~ve morphosCructurea (Solonenko, V.~ 1968b; S~ISrtOT~CTbNICS..., 1968).
With respect to nge of Cenozoic activation and degree of morphological _
perfeceinn, in the given etage of development they approach Che mature basins -
of the Baykal type, but with respect to intensiCy of the riftogenic movement$,
- they ing behind the ma~ority of the rift basins.
The potential eeiemicity of the 8ubrift basins~ both with respect to seismo-
statistical and with respect Co seiamogeological data on the whole ia sig-
nificantly below the rift structurea (Me4-3/4 to 5--1/2, I~~force 7 to 8).
Etowever, in the vicinities of the Eaults bounding Che individual basina (for
example, the Bauntovakoy-Tiliahminakaya and the China-Vakatskaya), the
paleoseismogeological data indicate the posaibility of the occurrence of
earthquakes with an intensity to force 10 (the Tiliahminskaya and the
' Medved' seismic atructures, see Chapter VII).
Just as in the majority of rift strucCures, the intrabasin commissures have
increased activity in the subrift basins. Por example, in the Bauntovskaya
bnsin on the Busano-Filinskaya commissure, a significant number of weak and
moderate earthquakea are constantly recorded. A strong earthquake occurred
here on 21 July 1968 (M=5.1; I~~force 7), It was preceded by numerous fore-
ehocks. The activity of the cencer was nated after the main shock: thus,
in September-December 1969 an earthquake awarm was recorded here (206 shocks).
- On the whole, the analysis of the structural~geological and seismotectonic
peculiarities of the morphoatructures of the transitional type indicates
that their formation and development occurred under the effect of the
[ectonic stresses acting both from the direction of the Baykal rift and the
Transbaykal black-wave zone. Here the effect of the rift stress field,
beginning with the Pleiatocene, hecame predominant, and in the Holocene,
individual parts of the investigated morphostructures are completely involved
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in th~ riftdg~nic typ~ of. d~velopmene. Accdrdingly, the inarea~ing influ~nce
~f th~ ri~COg~nic proc~s~es a1s~ c~u~pd ~,nc~~aged (by compgrieon w3th th~
Tran~baykal gerucCur~~) aeismic poeential nf the trengiCi,onal type morpho-
aCructures.
Tranebaykal Blo~k-W~ve Zon~
Th~ T'rangbeykel block~wave zone mor~ thgn 60,000 km2 in area occupies the
e~uthpaetern pare of Ch~ ~pipl~tform orogenic belt~ It ig characterized
by ~iCernation of the low and medium mounCain uplifts~with basins of the
Tran~baykal type ~xtend~d in Che norrheasterly direction, which on the whole ~
c~uges nn arch-block (block~wave) srructure of this terriCory~
With reapect to nature of the latest tectonic movemenrs and the morpho-
structural peculiarities all of Transbaykal ia broken down inCo three sub-
zones: Selenga-Vitim (B1), Khentey-Daurskaya (B2) and ~astern Transbaykal
(B~ (see Fig 100.
The Khentey-Daurskaya subzone is represenCed by a high, weakly differentiated
arch uplift. IC was isolated as a first-order structure by N. A. F].orensov,
1948) and Ye. V. Pavlovskiy (1948a). The two other aubzones are large
regions of relative subsidence ~lagging in the uplift behind the Khentey-
Daursskiy and Saykal archea), the internal parta of which are made up of
posiCive and negaCive morphostructures of aecond and higher orders.
A characteri~tic feature of the neotectonic development of the Transbaykal
as a whole is the predominance of the ascending type of movements (Khain,
1973). In addition to the qualitative analysis of the geological c~~uation,
this is confirmed by the quantitative calculation of the rate of the vertical
tectonic movementa. The rate of the ascending movemente is approximately
5 Cimes higher than the deacending. For example, the average rate of rise
of the Malkhanskiy arch-block upli.ft, ~udging by the deformation of the
Miocene-Pliocene planation surface in 10 million to 20 million years reaches
0.1 mm/year. The mean subsidence rate of the Chikoy basin ad~acent to this
arch does not exceed 0.02 mm/year.
Another remarkable feature of the latest and madern development of Transbaykal
is basically the inherited structural plan and type of development of it
Erom the Upper Mesozoic tectonic regimen (Florensov, 1960b; Zorin, 1971;
Ufimtsev, 1971). However~ the inheritance �eatures are not identical every-
where. They appear most clearly with~n the lj.mits of the Selenga~V~tim sub-
zone and the least i.n the D~urskaya and the eastern Transbaykal subzone. ~
Under the cond~,tions of Transbayl;al~ the calculation of the gradi.ents of
= the rate of vertical tecton~c movements and satisfactory convergence of
these data with the seismos~atistics have made it possible to approach the
determincttion of the leyel of the seismic potential both of the entire zone
as a whole and its component elements~ As a result of the calculations~
the followin~ series was obtained with values of the gradients; 1) from
1�10'9 years 1 to 2�10-9 years'1; 2) from 2�10"9 years'1 to 4�10~9 years"1;
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3) frnm 4~10'"9 enr~'1 to 6~10"9 -1
Y ypare (eee ~ig 101). Th3s serieg
npproximtttely Correqponds to Che zones wiCh possible errengrh nf the earth-
qu~ke: L) lees than �orce 7; 2) force 7~8 and 3) force 8~9. Thie
corrpepondence wae initielly esCabl~.ehed by us in the example of the
centrel~ and ~,n part westiern Transbeykal (the vicinity of the Chikoy'
Ingoda nnd Gusinoozerskaya 'besine~, wher~ seiemoetatiseical and paleoseigm~-
$eological daCa are ~vailable. Then it was exCended to th~ remaining
gecCions of the territory of Transhaykal wi~ere the rialeoeeiemogeologic~l
mgterial ig miseing, nnd the aeiemoetetistice are quie~ meager~
We ahg1L discues the specific estimate nf the potenCial seiemici~ty when
deecribing the eeiemotectonic role of positi.ve and negative morphostructurea
in Transbaykal.
Positive Morphostructurea
The predominanC position in Tranabaykal both with respect to area and with
reapect to seismotectonic activity is occupied by the arched and the binck-
arched uplifta. With reapect to mechanism of formation, these structures
are quite aimilar, but for the second type' along with Che bending deforma- -
tions, the brittle deformations also acquire a noticeable role, playing a
gignificantly leaser role than in the BaykalrStanovoy zone. The characCeris-
tic of the development of the poaitive structures is presented in the papers
by V, N. Danilovich (1960~ 1963), N. A~~Florensov (1960b; 1965),
C. F. Ufimtaev (1971). -
Let us present examples of the most characteristic Tranabaykal uplifts.
The Malkhanekoye uplift ia the standard arch~block morphostructure. The
maximum 'height of the Malkhanskiy ridge ia 1400 to 170~ meters; it is 270 km
long with a width to 30-40 km,
The arch-block nature of the latest structure is emphasized by the nature
of the deformation of the ancient planation surface, the relicts of which
have remained at maximum altitudes in the axial part of the uplift and
frequently in the limba. The slope of the planation surface in the limbs
of the Malkhanskiy uplift is 2 to 5�, and at the articulation points of the
limbs of the structure with the intermontane basins, it exceeds 5�,
creating the flexure~forming transitional zones (Ufimtsev~ 1971). In the
transition zone itself between the upli~t and the subsidence structures
are noted which are comparable to the forebergs (Gobi--Altay..., 1963). The
extent of the structures is on the average up to 10 km, up to 3~.m wide,
the absolute elevations rarely exceed 1000 meters, Some asymmetry of the
slopes of these promontori,es is noted. The spoke usually is greater in the
direction of the r~dge.
In vnrious areas ~t is possible to see d~~ferent stages of development of
the forebergs. For example. the generati.ng structures of the given type
are observed~ These are the individual low ridges made up of proluvial
material of the Upper Pleistocene and younger age. The amplitude of the
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r~ldCiv~ uplife r~~ehea 40 en 60 mee~rs~ mh~ more mgture form ~f th~~~
atructures ig Che w~11 exprega~d line~r ridges exC~nding up Cd 15 km wieh
a heighC Co 100 m~ters~ They are m~de up of ehe diglocated ~~rly QunCerngry
depoeits~ F3nally~ it ie nenes~~ry Co con~ider the mountnin chain made
up oE rocks of the Paleozoic baeemenC ehgr are isolaC~d from Che basic
mount~in massifg and are collected by uni,ty of atrike with eh~ "for~b~r$e"
of ehe preceding typ~. They extend up to 1S to 20 km, ~nd ehe relaCive
riees ~re 200 to 300 merers.
TI1E5~ three typee of structurea nre difLerent stagea of eheir dpvelopmene
- and indicate auccessive involvemenC in the uplife of th~ laCergl pgrCs of
the basins, which cauaes expansion of the posiCive struceures aC the expense
of the ad~acenC negative onea. The Transbaykal type of structures are
similar to the Gobi�~in thig respect, and it distinguiahed them theoretically
from the Baykgl (5olonenko, V,, 1968b).
_ The level of potential seiemicity of the arch~block uplifCs of the
tlalkhanskiy type, ~udging by the gradienes of the neoCecConic movements
and the residual deformationa ~see Chapter VTI, Yadrikhinskaya structure)
ia high nmong Che positive morphoatructures of Transbaykal and can reach
force 8-9 at the limit (rt to 5-1/2 to 6-1/2). This is ir.dicated by the
epicenter of the force 8 earChquake of 193~i (M~6).
In the ~eneral case the difference in nature of grocoth of such positive
structures, their intensity, differentiation and stage nature causes
fluctuation of the seismic potenCial of the Selenga-Vitim and the Eastern
Transbaylcal subzones from 1 or leas to force 8~9.
Among the arches of the Transbaykal zone the best studied is the
Khentey-Daurskoye uplift. In the investigated territory it is bounded by
deep faults: Chikoy--Ingoda on the northweat, Onon-Turinskiy, on the
southeast; Vostochno-Khangayskiy on the west, and Kukinskiy (supposedly
according to the geological data) on the east. The width of the arch exceeds
- 150 km, and it ia more than 400 km long. The maximum amplitude of the uplift
fixed by the planation surface reachea 1700 to 1800 meters (the headwaters
of the Chikoy and Chikokon Rivers).
The bending deformationa with large (to 2400 km) radius of curvature
(Ufimtsev, 1971) participate in the formation of the arch. The absence of
large linear arch blocks wi,ll permit the assumption that in the initial
stage of development of this structure no aigni�icant differentiated movements
- occurred. However, traces o~ weak latest tectonic movements F~ith respec to ~
the zones of indiv~dual fractures are quite numerous here. The ascending
- movements of the block are hasically untform along them~ Some of them lag
by 200~300 meters in the upli.ft,
Bei,ng developed in the latest t~,me with inher~,tance from the Upper Mesozoic
structural level~ the arch nevertheless experiences constant growth with the
excepCion of the northwestern part bounded hy the Chikoy~zngoda marginal ~
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puture. Her~, Edr pxgmpl~, thp Altan-Kyr~ngk~y~ Upper M~~dxnic basin
_ eurn~a nut tn bp involved in Che upli,ft~ This b~ein whtch previnusly (in
ehe Upper Juraseic t~ Ldwer Cretac~oue~ wag at the �oot of the arch, making
up ir~ ~ourh~~geern boundary. The boundary of Che arch ~feer the Ne~~en~-
Qu~ternnry pEriod ehift~d about 35 km to th~ soutl~,a~ee, ~nd gt the present
tim~ ie run~ along the Onon~Turinskiy ~gult~ The involvement o� ehe ~djacene
eectiona along the north~~~t~rn rer3c13nal grch, for exampl~, Arshanskay~
~nd Ur~yekaya Upner Mesozolc baeina proceeda annlogously (Ufimteev, 1571).
'Che n~epd pecul3ariCy is aleo characeer3atic for th~ develnpmene of oeh~r
nrches of the Tranebaykal block-wave zone. Seigmically the moeC dangerous
within th~ lim3ts of euch atructures ere the mgrginal p~rtg of the grches
(the limba and pericl3nals).
Negative Morphoetructurea
The Tranebaykal type basine occupy another geiamotectonic position in th~
Tranabaykal lump-wave zone (Flor.enaov, 1960a). Theee are the geomorphnlog-
ically expreased intermontane troughs (graben-synclinalg) linear sectiona
of plunging above the fault or next to the faule between the arch-block
uplifts. The maximum length of them reachea a few hundred kilometers, nnd
the width reaches 30~-40 km (see Figures 100-104). The greatest thickn~ss
of the ttesocenozoic aedimentary series in the basina is 1600 to 1800 meters;
_ of them About 200 meters are for the PYiocene-Quaternary sediments.
As the geological boundaries of the basins let u~ take the flex~re forming
transition zonea along the marginal arcogenic overthruat (or upthruat faults)
_ bounding the region of propagation of the lithofied sedimentary series.
~ With respect tn morphological and ~enetic attributes N. A. Florensov (1960a)
includes only those slopes in the trougha which are converted to the sedi-
mentary accumulation bed with completed layer formation. He includes the
higher ablation region in the mountain border. -
The outlines of the basins diacovered in chis way in general have smooth
features, sometimes disturbed by sharp distortiona connected, as a rule,
with the folded disturbances and the dielocations with a break in continuity.
The basic structural elements of the basina are the trough-like depressions
- aeparated by the projectiona of the cryatal basement reaching the day aur-
fnce or covered with a thin veneer of Mesocenozoic depoaits. In the large
hasina (Chi.ta~Ingoda, Ch~.koy, Khilokakaya~ Gusinoozerakaya) up to 3-5 troughs
are obaerved aeparated by project~.ons of the basement~ These include the
maximum th~cknesaes of the Mesocenozo~c deposits.
In the modern rel~ef the troughs are the lawest sections o� the depressions
occupied by the accumulat~ve nlai,ns. In both cases their surface smoothly
becomea the $djacent arched uplifts, and in other cases, it i,s emphas~zed by
the erosion~tectonic scarpe up to 300-4Q0 meters high or more. In the 8ec-
tion the troughs are asyametri,c. The aeymmetry of the basina finds reflection
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in thp znn~li.ey df diff~rene fg~i,~~ eype~ of loo~~ Qu~rern~ry d~pn~it~,
Aac~rding to th~ dri111ng d~eg, ~nti,r~ly d~f~,ned correspond~nce of it ed
tl~e zonality of th~ Upper Jurasai,c to Lower CreC~ceoue depoe3re ie
eAtablished.
`Che g~ner~l ~h8r~cteristic of the lAteat t~ctonieg of th~ Tr~nsb~yk~l b~sin~
ie the inh~riepd plgn and type o~ their developm~nt from tih~ Upppr lt~~nznic
tectonic cycle (~lorensov, 160a). It i~ ~ieo poeaible to e~lk ~bouC main-
Cenanee in the 1~Ce~C Cime of Che Upper tie~ozoic devplopmenC rgte~ ~his
i~ indicated by the comp~rativ~ an~lygig of the ~~diment accumulaCinn rgr~e
in the s~mp basins as, for ~acample, in th~ Chilcoy bagin ehe maximum thickness
di the Upper rtesozoic apriee in Che individual Croughs doee noC ~xceed
1200 to 1400 merers (Vnukov, 1967). Consider3ng that ~,Cs accumulation hna
occurred during the period from the Upper Juraseic to the Lower Cretaceoue
~nbout 60 Co 70 m1113on year~)~ the average sediment accumulation r~Ce is
npproximately 0.02 mm/year.
The thickneas of the looae Pliocene~Quaternary (10 Co 12 million years)
seriea 1n the same trou~hs does not exceed 150 to 200 meters (Khotina,
1966), that is, the nverage sediment accumulation rate is also about 0.02
mm/year, which by comparieon with the sediment accumulaCion rare in Che
_ rift basins ie almoat 10 times less~ Accordingly, many researct~ers are
inclined to conaider that the basina auba3de only relatively, lagging in
the uplift behind the actively developing positive aCructures. The fact
that in the lateat and modern period they atill experience weak plunge
is indicat2d by the presented aediment accumulatton rates.
Among the other general features characteristic of the Transbaykal basins,
it is necessary to mention Che reducCion of their area ae a result of
involvement of the marginal�parta in the uplifts.
Evaluating the seismotectonic peculiarities of the basin development on the
whole, it is necessary to indicate their insignificant role in the
determination of the level of aeismic potential of Transbaykal. Their basic
formation is due to the smooth submersion with insignificant intrabasin
differentiation. There�ore the tectonic movements connected with the
formation of the basins cannot be a source of strong earthqual:es.
Activated Faulta
In Transbaykal, the latest faults of northeastern strikes which.axe longi-
tudinal with reapect to the amooth morphostructures predominate. With
respect to genetic type they helong to the upthrow faults or the arcogenic
overthruat sometimes complicated by gravitational faults (banilovich~ 1966;
Fl.oreneov, 1960a; Ufimtaev, 19~1~, ~
The lrttest and modern movements along these faults are basically connected
with growth of the poeitive atzuctures~ In some cases they are the
interfaces between the poeit~ve and negative firstc~order structures
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(Mangnl.i~n-Okhde~k qnd bzhid~~Vttim faule~), ~nd in aeh~r~, of g~rond ~nd
hi$h~r arder~ (Khilok~Kgr~ng~, ~ugnuy~k3,y, ~nd ~d on).
The individual'faultg from 20 km or more locat~d parg11~1 Cd ~he ~ontinuati,on
, of pach orh~r or eubstituted in ~ch~l~n form, form ~QpQrne~ sy~eem~ with
diff~rent level of aceivity~ Th~ wideh o� euch ~ones r~ach~~ 20 tn 40 km,
~nd gometime~ more. The total m~ximum ~tnplitude of the vertical di~pl~~~-
m~nt with r~ep~ct to the i.ndividu~l fault~ durin$ th~ plioc~n~-(~u~t~rn~ry
i~ 300 co 400 metpre, and po~sibly mor~ (Khotina, 1966; Ufimrgev, 1~~~).
As an ~xgmpie l~t ug digcu~g thQ eharacteri~e3e of two f~ult zon~~
Mongolian-Okhotek and KhilokPKaren~a e~parating Ch~ firsC and g~cond ord~r
stru~ture~ reepectively.
ThQ Mongoli~n-Okhotek fracture extend~ to Tran~baykal from the terrieory of
Mongolia and in the northeasterly direction, acros~~ehe headwgters of the
Nyukzh~ River, it rune glmoet to Che Sea of Okhot~k. Ita total length i~
up tn 3500 km (in the re$ionalix~d territory~ 1200 km, and the width of it~ ~
zone is from 20 to 40 km.
~
The Eault is the boundary b,etween the eubzones the Seleng~-Vitim (B1)
in the northwest and Che Khentey-baurgkaya (B2) in~the eastern ~ransbaykal
~~g) in the southeagt (see Fig 100).
The fault deforma the ancient Cretaceous-Paleogen~ and younger Miocene-
Pliocene planation surface. The total amplitude of the verticaL displace-
ment of these aurfacea with respect to individual faults in the zone during
the Pliocene-Quaternary time reachea 300,400 meters. The modern activity
oE th~ rtongolian-Okhotak fault is confirmed by the association of the
epicenters of the~atrnng earthquakea of force 11 and 12 with it (*t=$.4 and
8.7) on 9 and 23 July 1905,,and force 8 in 1934, force 7 in 1935, and so
on.
The fault zones in the inveatigated territory include six individual
elements. Their potential seiemicity, ~udging by the pa:eoseismogeological
data, seismoatatiatics and the magnitude of t velocity gradients of the
vertical tectonic movements reaching (4-6)~l0~ears'1, decreases from force
8-9 in the west (the Chikoy element) to force 7 and less in the east (the
Shilka element).
On the whole, a general decxease in the potential seismicity of the
individual element~ of the Mongolian-,Okhotsk fault is noCed from southwest
ta northeast~l
1
Beyond the eastern edge of our map (in the vicin~ty o~ the Tukuringro-
Dzhazda anticl~norium~ it again ~ncreases at least to force 8(!i to 6 and,
possibly, more).
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`~h~e Khi1~k�Kgreng~kay~ gyge~m df f~u1t~ in eh~ igtege ~tru~tur~l pi~n
i~ ~h~ b~und~ry b~ew~~n th~ pogi,ci,v~ ~nd negaeiv~ ~~cdnd-nrd~r ~rrucCure~
~ntpring 3nea th~ 5~1~ng~-Vie3,m xon~. 'Che ~x~~nt ~f tih~ ~y~Cpm from eh~
souChWe~t to thp north~~et ie up to 700 lrm wi,th a~one width to z0 km~ Thp -
mean 1~ngth o� th~ individual~f~ule~ makin~ it up is 120 km~
tJi~h respect ed ~snetic t
ype, thes~ are b~~ically ~pChrow fgult.s nr ~reo~~nfr
nv~rthru~te. Thp ~mpiitud~ of th~ v~rC3.~~1 t~Gtoni~ m~v~m~ntg glong th~m
during th~ ~lioc~np~Quat~rnary p~ri~d is mnre eh~n 200 m~eerg (Khoein~,
1966, Ufimte~v, 1971)~ -
The low ~ei~mic $ctivity (A1~+~0.02 ~nd low~r), ~b~~n~~ nf p~l~ogpi~mog~nic
structure~, th~ low m~gnitud~ of the velocity grndients of rh~ v~rCi~s1
t~ctonic movem~nt~ noe pxceedin~ 3�10'9 yeors"j ind3caCes Chae the maximum
1~ve1 of the geiemic porential of the individugl faults in ehi~ zon~ i~
no more rhan forc~ 7-S (appreciebly iow~r th~n for the f~ui~g of the
Mong~li~n-Okhot~k zon~). Th~ other f~ult zon~s baundin~ fhp ~~cond-order
structur~~ dd nat ~x~eed thfg 1eve1~
- A~ompdri~dn of tt~p eeismogeological dnCe wieh resp~ct to the characterix~d
faults zon~~ of different order confirms the exi~ting opinion that ehe
r~~ion~l digturbance zon~s which bound the lgrge structureg having differ~nt
spceds of mov~m~nt ~r~ the moat seigmir. ~n addition, the opinion of the
- unit~d geismic potential of the fau1C zone ent~rs into contradiction with
the aceual material her~.
gnsic Lawa of Seiamotectonic Development
The abdve-described neotectonic and seismotecronic elempntg of the Siberian
Cenozoic pl~tform in the epiplatform orog~nic belt provide important material
for determining the nature of the movementa of the earth's crust for the
genetic varieties of morphostructurea and the conditions of manifestation -
of the earthquakea. The seismotectonic process in many aspects follows the
laws of tectonic development which Were laid down in the Cenozoic for the
Baykal-Stanovoy zone and in the Mesozoic for Transbaykal.
There is a contradictory opinion about the evolution of the rift procees.
In particular, it is considered that compre~gion take$ place from the 5iberian
platform side to the eaet (GrosWald, 1965) or to the aoutheagt (Dumitrashko,
1952; Azhgrrey, 1960; Voronov~ 1964), tension to the southeas[ (Florenaov,
1960a; Zorin, 1971) and to the northweet as a result of ahoving of the
platform back (Van Bertunelen, 19601 or combinat~on of tension aith horizontal
displacement along the faults (I,amakin~ 1968). Without discussing the
advantageR and disadvantagea of each hypothesis, let us note that now the
predominance of the tenaile stresses across the atrike of the neotectonic
struccures of the Baykal rift zone i,s generally recognize~. Accordingly.
the most proba6le and well~�ounded is the system proposed by N~ A. FJlorensov, ~
(1970) aupplemented With respect to aeiamological and geophysical studiea
(Misharina, 1965, 1972; 2orin, 1971).
352
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Th~ ~ngly~i~ and ch~ ~egei,atic~i prae~~eing of Chp r;~C~ ~n the ~g~ df ~~~.z
~urf~e~ pianation �nr ~ur~ei~ a~ ~ whol~ (Timofpypv, i96S~ 196g, 196~)
indie~t~~ rhaC ~ rr~nd 3s obsarv~ad toward the r~~uvpn~tion o� ehp d~nuddtion
pi~inA from we~t to Qa~t, Thue, for ehe orogen3c Centr~l A~ian belt eh~
age of the iniEi~l plain vnriee from rriaeeic in the aeee to Che Crptac~oug-
pal~og~n@ in the past. Thi,~ ~onfirma thQ eequenep of th~ t~~toni~ ~~tiv~~-
ei~n in ~he lat~et timp which 6egan much l~t~r i!~ Pribgykgl'y~ than in
W~~t~rn Aeia (Petruehgvski.y~ 196~i~ ~~he conclueion rhat ehe rift proc~~~
ie cnntinuing Co dev~iop tnward th~ eaet ~gree~ ~ieh th~e~ principl~~ ~nd
~h~ B~ykai r3ft znne i~ at the pr~aeent tim~ ~xpandfng ft~ dietal and lgteral
boundarie~ (Solon~nko, V.~ 1968b, c; ~loreneov, 197~)~
One ~f th~ clear indexeg of groWth of the rift zone i~ the continuing d~velop-
ment of th~ ~mbryonic and the gener.gted bagins (including the eatellit~
baeine) on rh~ elop~e and in th~ axial parte of the bord~r3ng uplift~. On
th~ ~outhwest~rn flank of the II~yk~1-3tanovoy xone the emall baein~ h~ve
dlr~~dy logt the capacity for further devQlopment (~loren~~v, 1960a), and
thp activity of the peripher~l eeiemogenic etructures in Ch~ Upper Pleietocene-
NoloC~ne hae been decre~sed eignificanCly. The development in timp of the
beginning of the neotectonic movements between the aouChwestern erid north-
pastern ends of the rift etructuree is also noted. If for the Baykal and
the '~unkinskaya basine thp maximuia intenaiCy of the Neogene-Qu~ternary
accivation belonge to the Miocene-Pliocene, Chen in the 5tanovny Highland it
belonge to the Plincene-Pl~ietocene (ACTIV~ TECTONIC5..., 1966; S~ISMO-
T~CT~NICS~.., 1968). D. V. Lopatin (1972) arriveg at the eame conclusion
on the baeie of analyzing the geomorphologicgl data With reepect to the
eastern part of the Baykal mou~tain region.
The trend toward re~uvenation of the proceeaea of rewurking of the earth's
cruac on moving from we~t to east finda confirmation also in the manifesta-
tion of the effusive activity. Whereas in the southWestern flank the maximum
manifestation of volcaniam belongs to the Oligocene-Pliocene (Obruchev,
1950; Florensov, 1960a, Floreneov, et al., 1960a) and the eastern flank the
beginning of the eruptione belongs Co the Pliocene~Pleiatocene or Lower
Pleistocene (ACTIVE TECTONICS..., 1966; Logachev, 1968; Lopatin, 1972).
In connection with the problem that hae been touched on regarding the
posaible relation of the Neogene-Quaternary volcaniam to the evoluC3,on of
the rift etructures it ia neceesary agai,n to emphaeize (Florenanv~ 1960a;
Solonenko~ V., 1964b, 1967; ACTIVE TECTONICS.~ � 1966; Florensov, et al.,
1960a), thet the direct relation of the volcanic processea to the zones of
activated faulta has not been eatabliehed any~,rhere in the investigated region.
On the ~ontrary,~ even the Holocene~ Well~preserved volcanic apparatuses and
che b~salt,~c d~,kea (Udokanekiy, Kharaar~Dabani Oka volcanic regions~, to
_ say noth~ng of the more anCi,ent ones, do not have de~ined structural control
on the p~rt of the riftogeni,c faults~ They are associated w~th the struc~
turnl li,nea, ae a rule~ Wh~ch obli.quely the discontinuous elementa of the -
rift structurea or they sre far to the aide of them (Vitim and Oka -
plateaus). This noncoincidence of the stril;e of the volcanic zones
(SV-30-50�) and the riftogenic faulte (aubl~titudinal orientation) is
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_ ~~p~ei~lly cl~~?rly nd~~d in ehe Udoka~n v~1C~nic reginn (Shc~n~nk~, V.,
1g64b; ACTIV~ T~C'CONICS.~~, 1966).
_ On th~ n~oeectoni~ lev~1, th~ neture of the volcan3gm r~fl~ct~ eh~ pror~~g
nf the latest aceivati,an an moding Cn the noreheagtern f1~nk of eh~ Baytc~l
r~ft znn~ (~nlonpnk~, V., 1968b, Haw~?~r~ ehe actual relationa of th~
volaanic and the ri,fCo~pnic, fr~qu~ntly gpgtially combin~ and gyn~hrondugly
oCCUrring prne~~e~~, remain unclear ~nd, mo~e frpqus�.',y of gll~ if rh~y
occur, Chen only in th~ mo~t g~n~~al form. Accord~ngly, in the s~i~mo-
tpctonic ~~p~et Ch~r~ i~ no defined or dir~ce rpi~eion betwe~n th~ volc~nic
r~~inng and ehe ppic~ne~rg of etrong ~~rChqu~kea. N~v~reh~lese, in a
number of cas~e (for pxample~ the Holocene volcanoes of ehe Udokan region)
lncc~l epi~csntral fieids and swgrma of weak earChqugkee are noted which
extend epatially to the individ~al grou~s of volcanos~ IC is pos~ibl~ thae
in ehe~e caees w~ ar~ d~aling not with CQCtonic, but volcanic parthquakp~
CSolonenko, V., 1968c), th~ more go in th~t the "suppr~asion of th~ volc~nic
erurCiane in th~ Ho~ocene is poasibly dnly a C~mporary phenomenon"
(~lorensov, 1960a).
The abov~-enum~rated examples cl~arly indicgte the re~uvenation of the
tectonic proc~~~e~ from west to easC. Accordingly~ Che propoaition of
V. P. Solnnenko (1968b) reggrding the migration of eh~ rift stress field
to the Stanovik region remains valid. However, thie finds confirmation also
in the geophyeical field in which the regular decrease in ~bsolute values
of the gravitational anomaliea above Che basins from southweat to northeast
of the Baykal rift zone ie noted which, together with an increase in the
over~ll 1eve1 of the gravitational field is in accordance with the conclu-
sion regnrding migration o� the rift formation to the easC.
The studiea of the m~chanism of the earthquake centera performed by
A. V. Vvedenskaya (1961) and especially in detail by L. A. Misharina (1965,
1967, 1972) demonstrated that the earth~a crust within the limits of the
ttongolian-Baykal aeismic belt experiences the effect of the horizontal
tensile forces oriented acroas the atrike of the basic neotectonic structures,
and the compressive streases are steeply inclined (more than 45�) or they
nre close to vertical. The orientation usually corresponds to the strike of
the morphostructures,
_ Previously it was cona~dered that on the southwestern ~lank (Tunkino~
Kosogol'skiy sector) the or~entation o� the atress axes is directly opposite.
- The inversion of the 9ayk$1 tectonic f~eld Was explained by the growing effect
oE Central AsiAn stresa f~eld. However, the detai.led studies of recent
years demon~trated that the stressea are summed up here wh3,ch are connected
w~th the riftogen~c and the mountain-.forming processes of the Mon~olian
(lntitudinal) and Sayan (northwestern) d~.rections Which are still complicated
hy the di,rectiona of the tensi,on (decay) in the highly uplifted blocks of
thc eartl~'s crust ~
- 354 '
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AcCOrdin~ly~ Che dif�er~ne e~rrhqu~k~a, even w~.th clnee center~, catt have
n diffpr~nC mech~n~,~m whi~h is confit7ned by the an~lysie oE the mechanism
nf Ch~ w~~k ~arthquake centera, Previously ~'~t appeared Chat in the
Tunkin~kaya b~~i,n nnd r.o Che west, the near-horiznntal eensile ~treases
~cring ncra~g th~ rif t_structures were b~ing replaced by compressive ones.
Thi~ idpa hae noe b~en confi,rmed, and all of the conclusions regarding the
madern d3rection of the eeeConin movemente of the earth~a cruse based on 3e
h~v~ no baAie" (SE25t40TECTbNICS~.., 1965a, p 128). -
On th~ eaet~rn ~1ank of the rif~c zone, gome spec3fiC peculiarieies have
gl~n b~~n diacov~red in the me~chanigm of the earthquake,center~ ~'or the
center df Che 7,verevgkiy eart'nquake of 15 June 1971 (56~28� north latitude,
123~66� east longitud~, P4e5,9~ H~15 km~~ Che subhorizontal orientation of -
the ~xes of the tensile ~nc: compressive stresses has been eatabliahed,
dlthaugh their ~patial poaition wiCh respecC to the structures 3s analogous
to thnt in the Baykal rict zone.
mhe migrgtional process o~' related aceivaeion in connection with ehe rift
formation reached Che viciniCy of Central Olekma, in the individual rifto-
~enic structures (Imgngro-Chebarkasekiy graben and Kudulikanskaya generating
_ basins) are coordinated with the west end of the Stanovoy arch. The plan
differentiation of the intensity of the riftogenic process is confirmed not
only by the magnitud~ and the aize of the~grabens, but also by the thickness
cf the molaeaoid formations filling the basin. Whereas in the Chara and
nth~r loaded roofed basina it is 1000 to 2000 meters or more, in Tokko basin,
nbout 500 metera, and in the emall baeins of the Baykal type (embryonic and
generating), appreciably less tena and a few hundreds of ineters. At the
same time the modern activity of the dislocations wiCh a break in continuity
controlling these atructures is comparable or even higher for the amall basiris
by comparison with the Baykal rift zone. The morphological damping of the
rift atructurea on the east flank of.the Baykal rift zone is combined with
intensification of the general etresaed atate of the earth's crust. In
particular, the basic number of paleoaeismodislocations and strong earth-
quakes in the rift zone of the Stanovoy Highland stretches to the morpho-
atructural complexes in which the amall basins are developing.
In establishing the seiamogeological relations and the seismotectonic
peculiarities~ the principle 4f inheritance has important aignificance.
It was developed by N. S. Shatskiy (1938) as applied to the defined tectonic
structures.
By this term we meant three interconnected aspects inheritance of the
tectonic plan~ tecCon~c forma and tectonic movements.
Thr. f~nyk.~l r~�c zonc hae cli~ri,ng ~,te development to the east cut acroas tha
etrike nf ~,n pr~ct.~ce all of the pre-Cenozo~c structural complexes. These
problems have been investigated in considexable detail previously
(Florenaov, 1960bs Solonenko~ V.~ 1968b; and so on)~ and the conclusions ~
drawn convincingly indicate the auperposed nature of its development.
_ 355
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The rift atructures are newly .Eormed~ and Cheir origin obviously ia
connected primarily wiCh the dynamics o~ the mantle procesaes.
At rhe rresenC time Chexe is a possi.billty far tracing the etructural
- Gvol.ution of the c~rth~a crueC from Che Mesozoic in close cnnnection with .
the tectonic stresx Eield~ The di.slocations with a break in continuity
bounding Che rtesozoic nnd Cenozoic negative structures axe indicators by
means of which ir is possible to determine the direcCion of the compressive
and rensile forces and their change i.n time~ Beg3nning only with Chese
condiCione, we: can state to whaC degree the Yateat sCructures inherit the
development of the preceding ones, for the replacement of the stress field
leads to inversion o� Che sign of the movement of the individual CecConic
elements of the crust. The formation of the Mesozoic basins and troughs
bounded by Che upChrow faults and overthrusts is closely connected with the
predominance of the compress~,ve stresses across the morPh~logically expreased ~
aCructures. _
The ma~ority of discontinuous dislocations of this time connected directly
with the tectonic field have sublat~.tudinal s~rike, orthogonal to the
comPressive stresses~ As~examples confirming this phenomenon we have the
upthrow-overthrust faulta~ spat~,ally and genetically connected with the -
origin of the Kalar, Khaniyslcaya, and Kudula tectonic depressions and the
Chul'man trough. If we consider the series of overthrusts, including the -
Angara associated wiCh the back of the Siberian platform of the same name,
then it is obvious that the compressive stresses do not have a local, but
they had a regional nature. It is true that in the vicinity of the Angara .
outcrop the compresaion structures are significantly smaller with respect
to scale than those within the limiCs of the Aldan shield, and the age of -
the former ia somewhaC more ancient: at least the sed3mentation cycle here
ended in the Middle Jurassic, at the same time as in the Chul'man trough it -
continues even in the Lower Cretaceous. Obviously this is a consequence of
the gradual weakening of the tectonic mobility from west to east in the
Mongolian-Okhotsk be1C (1Vagibina, 1963; Komarov, 1967).
Beginning with the h~sto:~y of the geological development of the southern
part of the Siberian platform in the 14esozoic, we can say that the tectonic
field was characterized by the meridionally oriented subhorizontal compres-
sive stresses and the sublatitudinal tensile forces steeply inclinecl toward
the horizon, and thus, in turn, determined the nature of the dislocations
with a break in continuity and the structures connected with them.
The aaykal rift zone, sometimes following the ancient dislocations with a
breal: in continuity as weakened zones of the earth~s crust, ~.s developing
in general features independently of them and has its own specific features =
of tecton~,c development d~.ffering from the pxeceding stage~ This ~.s
primarily expxessed in the fact that i,t was formed dur~ng the predominant _
stress role across the str~ke of the morphologi.cally expressed grabens
(Florensov, 1960a~ 197,0~. ~,n combi,nat~.on with the hor~.zontal moyements
(Solonenko~ V~, 196Aa~ 1968b~ w3,th respect to the riftogenic faults.
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Campnrin~ the preceding (Upp~r tleeozoic) field di tect~nic gtr.e~~e9 nnd
the mod~rn nn~, we see CMbC rhe oripntnti,on of the stre~s c~xes in Chem i~
dinmetricnlly opro~ire; th~ gen~Cic type of th~ disloe~Cinn~ of the brpak
in r.nntinuity nnd the nature o� Che movements nldng them ere diff~r~nt~
r~nci rnrrespondinqly, we dd ndt have any groundg fdr tnikinR nbout thr
tnl~rrit~d dcv~lopm~nt nf the B~ykal rift xone with r~At~ecC to th~ pr~c~ding
nl~nse of tectogeneeie~
The proceaees of modern activ~Cion of the western part nf Ch~ Stanovoy ridge
hnve fdund thpir expresgion ln the deep eroeion, the rearrgng~ment of rhe
hydrnulic n~twork and ~lsn in tl~e formation of n number of discontinuities
- in the divides and on the elapea of the Zverev ridge expresaed in th~
rrlief. AlonE Che exial line of the lntter~ almost over ite entire extent
there i~ a fault expreseed in the form of a aCeep scnrp~ The forruation nf
ttiis extended (60 km) frectuxe in the apical pgrt of. the arch-block uplift
possibly represente the process of inversion of the Cectonic movements in
connection with the plac~ment of the seress field. A similar procese
ohvinusly has occurred at the location of the Chul'man 1lesozoic trough which
nl c}~e preaenr r_ime perticipetea in the re~ional uplift of the southern part
of 5iberian platfnrm end is a standard inverted morphostructure. The change
_ in str~qs Eielcl, just as the eide of the tectonic movemente was caused by the
effect nf the neotectonic proceases in connection with the development of
tt~e aaykal rift system. It ie entirely posaibl.e that at the present time
in tiie vicinity of the Sranovoy ridge the atresaes of the Baykal type pre-
dominate, nnd the process of complete inversion of the rtesozoic field of
tectonic stresses has occurred correspondingly, and the stress field of the
gr~ykal type is developing farther to the east. -
The deep faults have aince the time of their forma$ion usually represented _
active atructural elementa of the earth's cruat, in connection with which
they usually are considered structurea of inherited development. However,
it is impossible not to take into account the fact that from period to
period, the type, the rate and the nature of the movements along them have
changed, ,juat as their magmocontrolling role has not been constant in tim~
nuring tlie periods of predominant compresaion the penetration of the
magmatic melts in large volumes has low probability, and during the period
~f tension, the situation is more favorable for penetration of the deep,
_ basic and ultrabasic differentiates of the magma (Peyve, 1965; Sherman,
1966; Florensov, et al~. 1960a), The formation of the tectonic structures
is directly connected with the tectonic stress field depicting, in ~urn,
the mantle precessea.
Thus, considerinR the development of the Baykal rift zone~ we must again
emphasize that ~t has developed supprposed with respect to the more ancient
structur~l plan~
Transblykal, on the other hand~ is charact~rized by relatively low level
of sei~smic activity and moderate rate of neotectonic movement, The tectonic
regime here is caused by the predaminant ~evelopment of the modern
structural forms from the more ancient ones, This point of vieW was
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~t~hCr.ci hy N, A~ rloreneov (1960n)~ and it w~a Cnnf irm~d during further
r~ae,hrr.l~~
'~hc predomin~nt type of l~tesr ~nd mddern Cectoni~ moveme�te for Trangbaykal
mugC be congider~d to be Che ~ecending one~ Nere the mopt ~cCive growth
i~a experienced by the nrcheg nnd the aYCh~block positive atruaCurea involv-
ing the laeeral pnres of the negntive seructurea in the uplift.
As ~ regult of the studies of the cent~rs of geron~ nnd w~gl: egrthquak~s
(Mieharina, 1965, 1g67~ 1912; *tishnrin~~, N~ 5olonenko, 1972), in addition
_ to ehe }iorizontal orientation of the ten~ile stresses~ Che orthogonalness
of Chem with respect ro strike of the main neoCectnniC ~truceures was
~lso discovered~ This conclusion is in accordance not only wiCh the general
_ geotectonic ideas of Che rifeogenic atructures, but alau with Che seismo-
teceonic observ~tions in Che epicentral zonea of Che ma~oriry of aerong
e~rthquakep in rhe paet (paleoseismodielocationa) and modern times,
T}~us, the mechnnism of themovement of. the earth's crust during the Muya
e~rthqunke of 1957 established with respect to the seismic dislocations
a~r~eg quite w~ll wiCh the orientation of th~ sCresses in the vicinity of
_ the center (ACTIVE TECTON2CS..., 1966). In the centers of the Nyukzha and
the Olekmtt earthquakes of 195F3, the atress orienCation also correaponds to
- the situation and nature of the discontinuous deformAtions in the epicer~tr$1
r.one~ wtiicti are tension ~o{nts of sublatitudinal orientation with insignifi-
cant component. This nature of the deformations corresponds to the :
- meridionc~l tenaile stresaes noted for the centers of these earthquakes. -
- The determinations of the mechanisms of the centers of the latest strong -
earthquakes Tas-Yuryakhskiy 1967 and Kadar 1970 confirm the presence -
of the tensile stresses oriented orthogonally to the main structural elements
of tl~e Kodar-Udokan and Stanovoy zones.
The studies of the stresses at the centers of the weak earthquakes
" (K~10-11) performed by L. A. Misharina and N. V. Solonenko (see Chapter V)
indicated that even for them, in the majority of cases the rift orienCat~on -
of the streas axes discovered by observations of stronger shocks is
characteristic.
This indicates that the predominant type of surface deformations here must
be the tension ~ointa combined with the faults which can be accompapied
by ~hifts. The surface deformations naCurally are not a direct reflection
of the processes, but at the same time the types of latest structures and
also their spat~.al orientation a~e in accordance with the nature of the
stresses in the center zones.
Thus, the roodern stress �ield di,scovered by the seismic ohservations in
tt~e aaykr~l~Stanovoy seismically act~ve zone agrees with the peculiarities
af the atressed state of the cruat in this region established by the
geological characteristics. The stressed state of the earth's crust
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rem~ins in general typicelly "rift" even in the bordering parC of the _
5tanovoy r~.dge~ wh~,ch indiceCee migration of the riftogenesie procees to
the Stanovik zone~ causing higher poeential seiemicity on it (~CTIV~
T~CTONICS...~ 1966; 5olonenko~ V~, 1968b~ c~,
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CNAPTER XII. SEISMIC REGIONALIZATION
5eiamic regionalization by the earthquake force esCimatea has been criCi-
cized for many yeara. It has been propoaed thaC it be replaced by region-
alization with reapect Co quanti~ative characteristica (seismic accelera-
tiona and their epectra, the duration of the oacillationa and Cheir ampli-
tudes, and so on).
Nowever, these proposals, which are ouCwardly CempCin~, especially for cal-
culating structural earthquake proofness are isolated from the actual na-
tural situation, the poasibilities of the equipment, the level of develop-
ment and "density" of the aeiemological obaervations. They are frequently
based on representations of earthquakes at the earth's surface "by analogy"
or on purely theoretical and not true manifestationa which can be discovered
only by inveatigating strong earthquakes.
Our experience in investigating earthquakes af all force levels (from 5-6
to 12) in the Mongolian-Baykal Seismic Belt and ob~ective data from investi-
gating earthquakes'in oCher seismic zones of the earth indicate t11at .
sharp (to force 2-3 frequently, force 6-7 sometimes) variations of the seis-
mic effect on the ground and atructures are observed at short distances of
up to 3 to 5 metera (Solonenko, V., 1960c, 1962a; Solatenko,V., Treskav,
- 1960; GOBI-ALTAY..., 1963; Solonenko, V., 1974). The investi~atore of the
San Fernnndo earthquake of 9 February 1971, emphasized that the "tremors and
destruction frequently were distributed over the area in a highly unexpected
way, in connection with which the problem of seismic regionalization appears
to be much more complicated than was assumed" (Gillete, Walsh, 1971). These
phenoa~ena have been encountered by Che investigators of the Peruvian earth-
quake of 31 May 1970, who established that often there is no obvious rela-
tion between the intensity of the destruction, the basement material and
the engineering-geological conditions. "We cannot explain all these phenomena,"
they conclude (Plafker, 1971a).
In addition, it i~ necessary to consider the following:
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1. The effect of earthquakes on the ground surface and the atrucCures
varies sharply and theoretically on going from 5 to 6 and eapecially from
force 9 to 10 when the reversible and reaidual deformationa of the surface,
the ground and the earth's cruat with amplieudea to several metera estab-
lished the limiting posaibility of building earthquake-proof structuree
(Solonenko, V., 1960a, 1962a, 1974).
2. The quantiCative parameCere, for example, of a force 9 1oca1 earChquake
cannot have aln?oaC anything in common with auch force 9 tremora as the
"tranait" ones (from the zone of a eCrong ear~hquake of force 10 or
higher).
_ 3. The inetrument characterizatiion of deatructive earChquakes (more rhan
force 8) ia fgced with equipment and many other barriera (Che poaeibility
of obtaining recordinge of epicentral and "trane~C" earthquakes of
equal inCenaity i.n close areas with different engineering-geological con-
diCiona, and ao on).
Thus, in order Co obtain a true quantitative characteriaCic of earthquakes,
_ it is necessary in esaence to have a mass of aeismometric equipment.
If we consider what has been said ob~ectively, it becomes clear that the -
problem of "quantitative" general seiamic regionalization will be solved
only in the distant future if it is solved at all.
During microaeismic characterization of earthquakea, the level of the aeismic
effect is averaged both as a result of Che number of obaervation pointa and
as a result of conaideration of varioua factors. Thus, the "force" estimate
is found to be significantly more meaningful than it appears to the propon-
ents of the "quantitative" seismic regionalization, and iC offers the possi-
bility of designing actually earthquake-proof structurea. For example, in
Irkutsk on 29 (30) August 1959, during an earthquake the intensity of which ~
was approximately the same as over the greater part of Tashkent in 26 April
1966, the buildings k~ith force 8 antiaeismic construction sustained only
light damage in individual cases at the same time as almost all the old-style
buildings, smaller and with thicker walls and foundations made of high-quality
building materials, were deformed and often significantly (Solonenko, V.,
Treskov, 1960).
Thus, there are still nothing to replace the "force" concepC (in the fore-
seeable future). The investigation of many strong earthquakes, wherever it
l~as been done by ob~ective investigators, indicates that the MSK-64 scale
(Merkalli-Kankani-Ziberga-Medvedeva-GEOFIAN-GOST) givea a hi~hly reliable
determination of the intenaity of the tremors and agrees quite well with the
values of M and K(aee Table 2). On this acale the dimensions of the resi-
dual deformations of the ground are esaentially low, that is, by these signs
it gives a high force estimate.
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Tlie relnCion between the force and the magniCude esCabli~hed empiricglly
by thp r~aulCs of inveaCigaCing sCrong earChquakea in Che Mongolian-Baykal
- Seismic Belt (SEISMOTECTONICS... 1968, pgg~ 147) was checked ouC in aub-
sequenC years and has demonatrated good convergence. It agreea well also
with the data of varioua authora for the various seismic zones of the earth.
The divergence is within the limita of accuracy of the observations (+0.5);
therefore it was aleo uaed when compiling the new map~ The corresponding
calculationa with respecC to the relation of M, K and JD facilitating the
use of modern earthquake catalogs are presented in ChapCers VI and VIII
(see Cables 7 and 12).
The preceding seismic regionalizaCion map (5olonenko, V., eC al � 1960b;
Solonenko, ii., 1963a, 1968a), which is the basis for the staCe map (SNiP
II-A. 12-69, Irkut Ob1asC~ Buryat ASSR, Chita Oblast) was compiled on the
seiamostatistical (Southern part of Eastern Siberia) and predominantly
tectonic and paleozeismogeological material. The insCrumenCed data were
very meager, for before 1952 there was only seismic station (Irkutsk), and
then three, but all located in Southern Pribaykal'ye. Since 1961 the ata-
Cion network has been expanded aignificantly, and it provides for recording
earthquakes with K n 7 for the entire rift zone, with the exception of a _
small section of the central part of Baykal from Lake O1'khon to the Svyatoy
Nos Peninsula (representative class K a 8). For the ad3acent parts of the
Siberian Platform and Transbaykal, earthquakes with K= 8 are representativa;
for Southeastern Tranabaykal, earthquakes with K@ 9. In addition, signifi-
cant factual data have been obtained by the network of temporary seiamic .
stations in the Udokan region (1962-1965), in Pribaykal'ye (1963-1965) and
the Barguzin Basin (1972-1973).
At the same time broad seismogeological and special geophysical atudies and
a great vari~~y of analytical seiemological and geomorphological-geophysical -
operations were performed.
It is natural that for such a broad territory as Eastern Siberia where an
area of about 1.5 million km2 has been sub~ected to regionalization, it is
impossible to collect the entire set of seismogeological, seismologic and
geophysical data with the same degree of detail; therefore when estimating
the seismicity of nne territory or another, preference has been given to
the method most "repreaentative" for the given section.
Ina~much as an earthquake is a physical-geolo~ical phenomenon, the regionali-
zation naturally has been carried out f irst of all on a seismotectonic basis.
However, in all phases of seismic regionalization seismologic and geophysical
data were used:
1) Wt~en compiling the aeismotectonic map, the seismological data were taken
~ into account in order to discover the specific seismogeological relations
in structural fields with noneharply expressed boundaries between the morpho-
structures, for classification of the dislocations with a break in continuity
and for solving a number of other problems;
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2) When Compiling the protenCial sei~miciCy map (poeeible epicentral
xone~ of m~ximum earChquakes): along with the eei~nw~ratidtical and
- ~~al~ne~igmngeoingicul d~tn m~p~ of Che sei~mic acCivity~ maximal eur[h-
yuakee uttd long-renge forecaeCing of ~eiemic acCivity were uaed. The
probable regions of ehore-term "seiemia calin" (see ChapCer X) were also
Caken lneo eccount. When ieolating the zonea of increa~ed ceneer acCivity,
the grapha of the recurrence rate of ehe egrthquakee were considered;
3) When calculating ehe averaged isoeeiema~ in addition to asiemoeCatis-
tics and the data on aeiemic dislocaCione~ calculationa of the damping of
rhe oscillaCions were aleo.used;
4) In the concluding phase of the regionalization~ a11 of the isolated
regiona were checked and corrected with re~pect to all of the seiemologi-
cal and geophyeical mapg.
The basic difficultiea of regionalization were encountered when estimaCing
the seiamic denger of a Cerritory where there are no paleoaeismodisloca-
- Cions. Wherever there are epicenCera of atrong hiatorical and modern earth-
quakes, in Cheae seismogenic morphoatructural zonea, there are no paleo-
seiamodislocations. Wherever there are no paleosQiamodislocations or there
are fewer of them and they are unreliable, there are no seismologic data
aufficient for aeiamic regionalization (Transbaykal). The difficultiea
also ariae from the facC that tha geological data in the absence of paleo-
seismodislocations do not up to the preeent time have a reliable quanti-
tative e:;treasion. Neverthelese~ for territories with aeiamological and =
paleoseismogeolagical material insufficient for regionalization it is neces-
sary to use the radiants of the vertical tectonic movements. From what has
been stated it ia clear that our seiamic regionalization map cannot be put
in any definite caCegory ("seismostatistical," "seismotectonic," "tectono-
physical," "quantitaCive," "paleoseismogeological," and ao on), and it is
in the complete senae a map of complex seismic regionalization. -
By the level of seismic activity in the regionalized territory three regions
. are clearly isolated (Figure 108): 1) the Siberian Platform--in practice -
an almost aseismic region with "transit" earthquakes from the Baykal seismic
belts; 2) Tranabaykal with moderate seismic activity and with "transit"
_ earthquakea from the Baykal rift zone and Northern Mongolia; 3) the Baykal -
rift zone with maximum seiamic activity.
Whereas for the last zone the paleoseiamogeological data can serve as re-
liable indexes of the higher level of seismic potential, for the platform
they are completely invalid, and for Tranabaykal they have suxiliary value
(the paleoseismodislocations are few and unreliable). The seismostatistical
data for Transbaykal are also unreliable, for before the middle of the 20th ~
century there are only spotty data on the earthquakes, and the seismic sta-
tions (two in all of this enormaus territory) have been in operation for
3 to S years. It is natural that for moderate seismic activity there are
inaufficient data for compiling the activity and K maps. Accordingly,
an effort has been made to determi~e the seiamic �~x potential of such
regions by the quantitative method of M. V. Gzovskiy.
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_ ~
f hr, ~"r ~ N I ~ Lw`~ I
~ ~ , , ~ ( i)1.J
~ .~,~.r.
, ~
1 ; , i (SO ~ ~ ~
. ~
i c~~ Q:]~ ~ ~ ~
~ ~ v
~.ti r 1
~ ~1 ~ � n,+
A L" ~
~
'w_ h_M~~ ~
r
~ ~ ~N4
~ , ~ ~ i
, ~ ~ ~ ~ ~ �
! " 1: ` ~ _
' 1 ~ M
~
~ 1 .L~'~, ~ ~ ~
~ � ~
! ~ ~~~~Ni ~ i
` ~:1 ~2~) ~2:~ ~ , ~ ~ �
~~~~i'Q~i''~`~ i:. L ~ , , ~
~ ~ ~ _ ~
~y~'~ ~ f:Al
.
~ ~ .
~ -L ..u~ v 1'~ -
~ ~ f13) . (SA)
. : ~ ~ ~...a 'i}'~ . � ' � I
_ . . ~hrrtt ( w ~
~ ~ ~ ~ , M
A r ~ '
( i 1 ~t~
� ~8j,i~ N ~ _ i
- ~ ~ ~ �
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9 ~ i � ;
� / ~N
c3r~ c4s~ I
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Figure 108. ~See following page~
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I'igure 108. Tiap of eh~ eeiemic regionalization of ~~~Cern 5ib~ria.
Compiled by V~ Solonenko~ R~ A. Kuru~hin, M. G~ Dem'ygndvf~h,
S~ V~ La~tochkin~ V~ V~ N~,kolayev~ S~ D. Khil~tco~ V. S~ Khromovskikh,
V~ M. Ko~hetkov,, V~ M. Zhilkin~ A~ D~ Abglakov~ ~dited by V~ P~ 5olonenko.
(5ee preceding ~age fo~ Figure 108~
T1~~ zon~s of possibl~ occurrence of the egrthquake center~ or their
- magnitude (11~ and the 3ndication of the example inteneity ~ZO);
1-- t4>7 (force 10 or more); 2-~~ M-- 6-1/2 to 7(force 9), 3-- M=5-1/2 -
to 6-1/2 (force 8~9), 4-.� M�4-3/4 to 5~1/2 (force 7~8), S~- M 6.5, the seiemog~nic fracCur~r~~ ag a rule~ reach the
~urface of the earth (see Chapeer I) and ~ignificgntly in~xea~e the macro-
s~igmic effect. The eeigmngenic ~oinCs and sharp oecillaCiong of eh~ wallg
of ehe faulrs with g residual ampllCude Co 0.$ m~tere and eomeeime~ mor~
(trup amplitude approximaCely twice th~t; gee Solonettko, V., 1968c; GOBI-
ALTAY...~ 1563, pp 326-328) unconditionally deatroy any sCrucCure~ even
with force 9 antisei~mic reinforcemene.
The i~ol~eiott c~f euch gectiong ia entirely ingical: no one ob~eces to in-
cr~gging the force eeCimate by one as a result of unfavnrable engineering-
hydrog~oingical condiCions, and what can be more unfavorabl~ than a moving
seismngenic fault zone? During gener~l regionalizgtion, the former cannot
be reflected on the map (becauae of ecaling conditions), at Che same time
ns the seiamogenic faulta are a mandatory element of the cenCer seismiciCy,
seismotectonic, and seiamic regionalization maps, and so on.
When investigating atrong earthquakes in the Mongolian-Baykal aeiamic belt
and according to the published data the following laws were esCablished already
15 years ago (Solonenko~ V~~ 1962b; SEISMOTECTONICS..., 1968, pp 146-149)
confirmed by aubsequent events both in the Soviet Union and in other aeismic
zones of the earth.
1. For linear seismogenerating structures the force 10-11 earthquake zone
extends in a narrow strip along the seismogenic dislocationa. The width
of the zone is about 4 km on the active size (or sides) of the structure and
2-9 km, on the passive side. In the presence of feathering and accom~any-
ing fractures, it can increase to 10-12 km or more. For the block seismo-
genic structures the intensity of the tremor on the surface of the displaced
structure is distribuCed nonuniformly--the difference for adjacent sectiona
reachea several force points, but the variations with respect to area are _
not sub~ect to advance calculation.
In the pleistoscism zones of force 10-11 earthquakes (Tsaganakoye, Muya,
Iiayan-Tsaganskoye, Mogodskoye, and so on) the established amplitude of the
verticnl and horizontal displacements reaches 7-8 meters, the ampliCude of
Che surface waves in loose ground is up to 4-5 meters with a length on the
order of 15-20 meters. In the loose ground the width of the gaping trench-
~ointe is ~asual up to 4-6 meters, frequently to 10 meters, and in individual
cases to 19 meters (ACTIVE TECTONICS..., 1966, pp 151-152). In the rocky
ground ~oints are formed with gaping to 4-5 meters and obviously sometimes
more.
Tl~e apparent opening of the faults on the aurface of the earth along the
strike is observed over an extent of up to 30 km (the Muya earthquake),
and with predominance of the shift component, to 45 km (the Mogodskoye
earthquake on 5 January 1967, M= 7 3/4). During the Muya earthquake the
movementa in the fault zone were obse:ved to 90 km from the epicenter to
the east (in the direction of the shift of the ridge) and to 50-55 km in
- the opposite direction.
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The creaCinn of economicelly ~nd tachnically ~xpediene antieeismic atruc-
tures for force 10 zones i~ impoesible; Cherefore they must be categorically
cloeed for conetruction, with the exception of unavoid~ble communications
which mueC croes such zones by the ehortest path.
- 2. ~he force 9 regiong with re~p~ct to eeiemic danger are nonuniform. In
the saiemogenic fau1C zone actually the forca of the earthquakea exceedg
tha reei~Cance c~f the eCructurea wiCh any earthquake-proofing conetruce3on.
These movements are ob~erved along the aCrike of the fault up to 50 km~ -
and sometimee more. Therefore in the force 9 regions along the seismogenic
faulte aC a diatance of up to 2 km from them the erecCion of capital'struc-
tures (with the exception of unavoidable communicationa) is inadmisaible.
On the seiemic regionalization map, such secCione are ehown as poseible
center zonea with M ~ 61~ to 7.
3~ ~or the force 8 earthquakes in Che epicentral segment of the se,iemo-
genic atructure there are eharp~ but as a rule, revereible oscillations of
the walls of the faulta and the macroseismic effecta reach force 9(on the
average to lk km~along the fault and 1-2 km acrosa it). There�ore it is
neceseary to avoid capital con~truction in auch ~onea.
4. In the areae with thick (300-400 metera or more) seriea of nonmetamor-
phic sedimentary rock, the earthquake intensity decreases sharply and ir-
regularly. Therefore in the internal parta of the baein in the abaence of
highly active seismogenic structures in their basement, the initial norma-
tive force of the earthquake can be low by one force point.
In order to outline the areas of the "transit" tremore in the direction of
the seismogenic structures, it doea not appear possible to use the standard-
ized procedure. For example, by the calculated data for the circular iso-
seisma and by the average aizea of the f,soaeiamal areas with respect to -
n~acroseiamic effecta (see Table 19) on the Siberian Platform the area of
the force 6 region by comparieon with the 1962 map (Solonenko, V., 1963a)
should be expanded 200-250 km to the northwest, which contradicta the avail-
able macroseismic data. Therefora primarily aeiamoatatistical data were -
used, and in case of a deficiency or in the absence of this data, the average
data (see Table 19) considaring the seiamic wlnerability mape and also th`
specifics of the apread of the tremore over the summary isoaeismal map.
When determining the boundaries of apecific aeismic regions, definite dif- _
ficulties are encountered. The regiona with possible force 10 earthquakes
or higher and the sections of the force 9 regions with increased seismic
danger require especially careful analysie of the seismogeological, seismo-
logic and geophyeical data. They~ as has alread~r been stated~ must be first
of all forbidden for capiCal conetruction (with the exception of coimnunica-
tions) and, aecondly, they must be the starting points for deterniining the
boundariee of the "transit" tremor regions, including the platform sections
where no local etrong earthquakes occur. The problem ia somewhat facilitated
by the fact that these regione are within the boundaries of the Baykal rift
system (with the exception of the near-rift zones of the Oka and Kitoy faults
in Eastern Sayan).
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During general regionalization, the concept of constantcy of the maximum
earthquake engrgy over the entire extent of the aeismotecronic fracCures i
is used. For the Baykal rift~ we have long refrained from using this rule
(Solonenko, V.~ 1963a). In the overwhelming ma~ority, the faults have more
an.cient occurrence, and the riftogenic processes causing high seismicity
are Cenozoic. If a fault goes beyond Che boundaries of the rift zone, the ~
seismic activity decreases aharply (for the Obruchev fault system, from
force 10-12 Co force 5-6). Under these conditions, the question naturally
arises of the limits of Che force 10 region in the flank zones wiCh poCen-
tial seismic activity of force 10 or higher (see Figure 108). If we con-
sider, as usual, thaC at any point o� the section with potential seiamic -
activity of force 10 there can be an epicenter c~f the corre:sponding force
eatimate, then the boundary of the force 10 region musC be considered along
Che strike of the structure aC least 25 lan or more, and the force 10 region,
45 km (see Tab1e 19). This lengthening of the high-force regions from our ~
point of view is valid only in the case where the seismologic data indicate
tiigh acCivity of the fault zone beyond the proposed boundary of the rift
system. In the opposite case the provisional epicenCer of the future earth-
quake is taken in the center of the section of the seismically active zone
which can insure a force 10 earthquake, that is, 25 km rrom the end of the
structure. In this case the distal boundaries of the regions of potential
seismicity and sei~mic regions (see Figure 108) of different intensity coin-
cide. .
isolation of high-force,regions, the probable recurrence rate of the
_ ~:Crongest earthquakes is taken into .lccount also. The earthquakes of force
11-12 were not considered, for their probability is very small. The traces
- of such earthquakes have been established only in three areas of Che rift
zone (Southern Pribaykal'ye, the western shore of Central Baykal and the
Udokan Ridge), with intervals between their epicenters of 350 and 750 km
where such earthquakes have never occurred at least during the last thousands
of years. The possible force 10 earthquakes in isolaCed seismogenic struc-
_ tures, the potential seismicity of which according to geological and paleo-
seismogeological data will reach force 10 were also not taken into acc~unt,
but the recurrence rate of such earthquakes is low (no more frequently than ~
_ once in a thousand years according to the paleoseismogeological data and less
ttian once in ten thousand years by the seismic vulnerability map), and by
the seismological data, the activity and K~X are low. These regions belong
to force 9. ~
Description of Seismic Regions
The basis for isolation of the regions, especially of high seismicity (force
9, 10 and higher) is the paleoseismogeological, seismotectonic and seismo-
statistical data. They determine the initial ("background") seismicity for
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thp average ground conditionel~ Along wiCh thie~ ~eismologicgl atid geo- -
phyeical maCeriaLa are u~ed (the Cime-~pace dietribuCion of Che earChquakee,
the seismic nctivity of Che region of ~pecific eeismogenic structure and the
probable maximum earthquake cenCer with reepecC to K ~ the long-range fore-
casting of the seiemic acCivity~ the "preparation" zonee~ and so on).
The increase or reduction in the force estimate ae a reeult of the engineer-
ing-geological~ geocryological~ geomorphological and other purely aurface
- fnctor~ which are taken inro account only during detailed seiemic regionali-
zarion and microregionalization are not reflected on the seiemic regionali-
zation mep.
The boundaries of the eeiemic regione of higher forces on the whole do not
correapond to the boundaries of Che center zones of higheaC activity taking
into account the entire set of geological-geophysical data. However~ there
are no exact boundaries of such zones in nature~ in connection with which
t3~e boundaries of the seiemic regione can be drawn only within the limits
of Chp defined fiducial intervala of valuea of different intensity and ac-
tivity of the obaerved procesaes.
'The boundaries of the high-seiemic (force 9 and 10) regions have been drawn
the moat definitely. Their isolation ie clearly controlled by the nenCec-
tonic structures with higheat seiemic potential, the paleoseismogenic atruc-
tures and a?odern seiamic dislocationa and also the entire set of seiemologic
ciata. The regiona of moderate and low aeismicity (force 8, 7 and 6) which
are isolated predominantly by the seiemostatistical, aeismologic and averaged
macroseismic data (see Table 10) and also by the type of latest atructurea,
degree of iatensity and conCrast of the neotectonic movementa are lesa re-
liably outlined.
~ 1. The regions with earthquake intensity of force 10 or more extend spa-
tially to the Baykal rift zone. Cenetically they are closely connected with
the marginal parts of the large rift structures, being located along the
zones of activated ("seiamogenerating") faults. Among them the clearest
examples are Tunkinekaya, Obruchev, Kodar. Udokan, the Stanovoy fault system,
the Cherakiy fault and other aeismically ar,tive lineaments. These include
the short dislocations with a break in continuity activated in the anthropo-
gene, developed in the regions of highly se~smic regional interbasin commis-
aures where, as a rule, they control the development of the small rift struc-
tures of the type of type of the generating and embryonic basins.
In the ma~ority cases the isolation of the epicentral regione of maximum
seismicity is substantiated by the paleoseismotectonic structures, the forma-
tion of which occurred during earthquakes with M on the '-der of 7 or more.
1 B the avera e
y g ground we mean the natural sand-loam ser~es with deep
occurrence of ground water of more than 8 meters (from the level to surface).
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_ In ndditinn Co the strucCural-CecConic and the eeiemogeological criterig~
- Che leolgCion of euch zonee ie aubsCantiaCed by an increased concentraCion
of the epicenters of moderate and weak earthquakea, which is reflected on
the seiemic activiCy map (the values of A10 for them uaually do not drop be-
low 0.2),
- ~l~e highly seiRmic epicentral regions extent in narrow (from 1-2 to 8-10 km)
= strips along Che riftogenic faulCs. Here Che fau1C zones wiCh simple struc-
ture~ with Che aleareat contraet of the neotectonic movemenCe (�or example~
Tunkinskaya, Obruchev, Barguzin~ Kodar~ and so on) give rise ta etill clearer
and etraighter boundaries of the force i0 seismic regions. In the case of
complex structure of auch zones (echelon structure~ broad development of ac-
companying and feaChering dislocations~ variaCions of the active faulta,
sharp block diffrenCiaCion in the marginal and axial parCs of Che uplifts
bordering the rif.te~ the syatem of generating basine~ and so on) the force
10 seiemic regions are expanding and have complex configuraCion. This is _
eapecially characterietic for the rift sections of ehe arch-block uplifta
(Khamar-Daban~ Udokan) and the large inCerbaein mountain commiasures (Upper
Angara-Muya~ Muya-Chara). For regio~nalization of the highly seismic zones -
it is asaumed thaC the aingl~ seiamotecConic lineament ia seismically dan-
gerous to an equal degree a].ong its entire extenC. However, as hae.already
been noted at the beginning of the chapCer, the large~ exCended zones of
"seismogenerating" faults are divided into secCions with differenC level of
seismicity. Firet of all, this pextains to the faulCs which go beyond the
iimitg of the tectonic stress field of the Baykal rift zone both on its flanks
and on the periphery. Accordingly, aignificant sections of Che Tunkinskaya~
Eastern Saya, Obruchev, Barguzino-Muya~ and Stanovoy systems of activated
faults are included in the force 9 seismic regions, and against this back-
ground they are conaidered as zones of increased seiamic danger. For auch
sections, the absence of explicit signa of seismo~enic re~uvenation and
a lowered level of modern seismic activity are usually characteristic (see
Chapter XI).
In addition to the neoCectonic and seismogeological factors, the isolation
of the force 10 regione is confirn?ed by the seismostatistical data--the
epicenters of etrong (force 9-10) earthquakes and alao inereased concentra-
tion of the epicenters of ~oderate and weak shocks within their boundaries
(see Figure 73-75), which is reflected on the aeismic activity maps (see
Figures 16-78) and maximum earthquakea (see Figure 89). The values of A
for such regions usually do not drop below 0.2. However, in the Baykal-1~
Stanovoy seismically active zone there are a number of force 10 regions which -
on the seiamic activity maps and the maps of maximum possible earthquakes
correspond to low values of A 0.05~ and K < 14). Examples: the
Muya Basin~ the Northern BaykaQ part of the Obiuchev faults, the Upper Angara,
Parama and China-Vakatskiy (eastern part) fault zones in the Stanovoy High-
land. The inclusion of such sections in the force 10 regions~ in spite of
the noncorreapondence to the seismological data, is substantiated primarily
by their seismotectonic position (all of them control the development of rift -
structures and erabryonic basins) and coordination of the paleoseismogenic
structures occuring during earthquakes with an intensity of no less than
force 10 with them.
= 372
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' F'or the Obruchev f~ult zone theee are ehe following eeructurea: 5ouehexn
Rita~ Shartley, Srednekedrovaya [Central KedrovaygJ~ Khibelenelcgya, Solon-
teovaya; for Che easCern parC of Che Upper Angara faulC--Che Ogney struc-
ture and the generating Churo grgben; for rhe vicinity of ehe Muye Baein--
Takein and Parama etructures, and for the eaeeern eection of the China-
Vakatgkiy fault--Che Medved' atructure (eee Chapter VII). Many of the
enumerated sectione with respece to macroeeiemic information and instrument
data are confirmed by Che epicentere o� atrong (on the order of force 8)
earthquakes. Thus~ for example, on 6 Auguse 1931~ an earChquake occurred
in the viciniCy of Che northweat shore of Lske Baykal with a propoaed in-
_ tenaity of more Chan force 8; in Che vicinity of the northeaetern border
of the Upper Angara Baein inetrumente recorded two earthquakea wiCh an in- -
tensity of up to force ~(11 March 1936 and 17 September 1957); in the same
region on 18 AuguaC 1902 an earthquake was fe1C~ Che force of which at the
observation point reached force 8(aee Chapter VII).
It is also proposed that aC least part of euch zones (for example, easC of
- the end of the China-Vakatakiy and the Upper Angara faulCs) corresponds to
the regions of "preparation" of atrong earthquakes (aee Chapter X).
When i8olating the force 10 regions on the map~ the poasibility of the oc-
currence of earthquakes also with greater intensity is suapected, which is
indicated, for example, by certain paleoseiamogenic phenomena within t;he
boundaries of the Baykal rift (the Shartlay, Southern Rita structures) and
the Stanovoy Highland (China-Vakatakiy structure). However~ the recurrence
- rate of such seismic dieasCers on tlie ~rhole for the territory of the Baykal-
Stanovoy seismic zone ia low (according to the paleoaeismogeological data,
no more frequently than once in 500-600 years). In practice they are ex-
cluded from the regionalization and muat be conaidered only when constructing
especially importanC long-range projects.
The regions with earthquake intensity of force 10 or more occupy an area of
33,800 km2, which ia almoet twice the area of the force 10 regions isolated
on the seismic regionalization map of Eaetern Siberia of 1962 (Solonenko, V.,
1963a). The area was increased as a reault of inclusion of the water part
of Lake Baykal in the regionalization (about 8,000 1~2) and partially as a
result of isolation of new force 10 regiona in the rift .one nf the Stanovoy
Highland (about 7,000 km2) diacovered during complex sf~iemogeological studies
in the last decade (ACTIVE TECTONICS..., 1966; SEISMOTE~;,TONICS..., 1968, _
1975a,b). The unavoieability of this increase was proposed also earlier
(Solonenko, V., 1963a). The regions with maximwn intensity of the possible
- earthquakes have also been isolated here along the 'riftogenic fault zones
controlling the northeastern part of the Upper Angara Basin, the northern
- and western sides of the Muya Basin and the system of small (embryonic)
basins of the Baykal type within the boundaries of t~e Upper Angara-Muya,
the Barguzino-Muya and the Muya-Chara interbasin mountain commissures.
The force 10 regions along the Tunkinskiy and the Barguzin fault zones and
northQast of the Svyatoy Noa Peninsula have been increased somewhat. In the
, latter case the highly aeismic reRion encompasses the Bol'sherechenskaya
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nnd Chc Snenovekaya s~CelliCe basin~ nnd the zones of ehe lateaC �aulta
bounding them (S~ISMOT~CTONICS..., 1968; Abalgkov~ 1973) locnCed on Che
conCinuaCion of the seismically acCive Cetttral Bgykal interbasin commissure.
Two new gmall force 10 regions have been isolaCed on Che northeaeCern flank
af the Bnykal rift zone, on the left bank of the mi.ddle courae of the Olekma -
~tiver (Olekma-Charn interfluve). They outlined the seiemogenic atructurea
of the epicentral regiona of three aCrong earthquakes--Olelnng and Nyukzha
_ 1958 and Tas-Yuryakhskoye 196~ (ACTIVE TECTONICS...~ 1966, SEISMOTECTONICS...,
1975a).
The force 10 seismic regions muat be Forbidden for capiCal coc~aCruction.
IC is necessary ta coneider the facC thaC in Che ma~oriCy of cases these
regiona~ as a rule, are characterized by extremely unfavorable or unsuit-
able engineering-geological and geomorphological conditiona for construc-
Cion. Only apecial atate intereats or apecial economic requirementa can ~us-
tify Che erection of certain engineering structurea in theae areas. It is -
Crue Chat in individual c$sea, especially where aignificant expansione of the
force-10 regions are indicgCed on the described map (Southern Baykal, the '
Muya-Chara zone), on deCailed inveatigation and microregionalization, it ia
poasible to isolare areas wiCh reduced aeiamic danger. The acale does noC
pem~it indication of auch small sections on the map, buC it ia necessary to
coneider that the poeaibility exiata.
2. The regiona with earthquake intensity of force 9 occupy the largest areas
in the Baykal-Stanovoy aeiemic zone, primarily along the system of Ba~',lcal
rifts and on its flanka. EssenCially all of the morphoetructural elements
of the Baykal rift zone (primarily the rift baein) are characterized by
force 10 potential seismicity. In the regiona of the uplifts directly bound-
ing the rift basins, these areas include the complexly differentiaCed central
parts of the side and the arch-block morphoatruct+ires removed from the zones
- of maximum (force 10) seigm~city.
The ourlines of the force 9 seismic regions are connected bo~th with local
center zones and with the extent and configuration of the forc~ 10 regions
from which the force 9 surface effects extent (the "transit" tremors). Ac- -
cording to Table 10, during an earthquake with an intensity at the center of _
ri > 7 this effect can extend to a distance of up to 30 lan across the strike
and 140 km along the seismically active structures. Thus, in the force 9
seismic regions bordering the broad belt of the activated fault zone with
established maximum (force 10 and higher) seismic danger, obviously the "tran-
sit" oscillations play a aignificant role. Moreover, centers of force 9
earthquakes are possible here according to seismotectonic conditions.
In the regions of mature rift basins, the force 9 zones include longitudinal
rift forming faults or the set of echelons of such faults (without apparent
traces of seismogenic re~uvenation) contro'ling the maximum plunged sections
of tt~e basement. In the formation of the articulaCion zones of these basins
w~ith the mountain bordera a eignificant role is played by the bending de-
formations, and the mean velocities, in spite of the maximum scale of the
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neotecConic movemenCs probably is somewhaC lesa Chan in the amall rifto-
- genic morphoatrucCurea. In the maCure bagine~ in gdd~.Cion, the zones of
force 9 seismic danger include Che intrabaein commissures and lateral pro-
3ectiona Ch~t are manifee~ed on Che aurface characterizing the t~harp dif-
ferentiation and increased contraet of the movemente of the individual
block~ of the basement of higher orders.
The large regional interbasin commieaurea are in practice completely asso-
ciatad with the zonea with poesible occurrence of force 9 earthquakea.
Such zones here include ehe ama11 rife basina, tha bottoma of which, as a
rule, are differentiated with de�ormation of local intrabASin and inter-
_ basin commiasures, and the aides are frequently complicated by young longi-
tudinal and transverae faults. Uaually the embryonic baeins of this type
are separated by connniasurea into a aeriea of depresaions as a xesult of
which, inside them the blocks with different signa and rates of latest move-
ments are in contact. WiChin Che limita of these negative morphoatruaCurea
it is posaible to expect Che occurrence of reaidual seiamotectonic deforma-
tions connected with the local force 9 shocks and onea excited by maximal
earthquakea, the hypocentera of which are within the zones of Che main rift
_ forming faulta. The examples of the Muya (1957) and the Mondy (1950) earth- -
quakes indicate thia quite obviously.
'The regions of probably force 9 earthquakea M~ 6 1/2-7, within the limits
of regional commissures also include the sharply differentiated parts of -
_ the block morphostructures usually located between the zones of increased
seismic danger. Here we also have the parts of the faults having maximum
degree of aeismic danger with respect to geological and seiamic data (M
but going beyond the limiCs of the morphoatructures which cauae this danger.
(For example, the Muyakan fault, the northeastern parta of Che vicinities
of the Upper Muya, the Uchargaeskiy, tihe western parts of the Southern Muya,
the Konda-Eymnakhskiy a:?d many other faults in the regional commissure areas). .
Thus, in the force 9 regions the seiamic danger depends csn the manifestation
of both local earthquake centera with M= 6 1/2-7 and the surface effects
of the "transit" tremor from the direction of the seismogenic structures of
high potential (M 7). Here the force 9 regions are constricted in the
- case of the simply outlined force 10 zonea (for example, Tunkinskaya, EasCern
Sayan, BarRguzin, Obruchev, Upper Angara) and they expand significantly ln ~
the case of complex configuration of them (Southern Baykal, Muya-Chara re-
gio.is) .
It is necessary to note that in the investigated territory of Eastern Siberia,
significant sections of force 9 regions with respect to area are not always
confirmed by strong earthquakes and high level of modern seismic activity.
However, with respect to the neotectonic situation, the degrees of differen-
= tiation, contrast and amplitude of the latest movements, intensive rearrange-
ment and developmE~nt of the neotectonic structures they are analogs of the
areas with the established force 9 seismic potential. For exa~.~ple, the
375 ~
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flnnk parts of the Baykal rift xone (Eaetiern Sayan and the SCanovoy uplift)
- and certain morphostructures of Che transitional Cype from the direction of
the Tranebaykal b]nck-wave zone (Khamar-Daban, Ikat~ Udokan-Kalar, the fault-
block uplifte)are under euch aeiemogeological conditions. Nearer to the _
marginal part of the 5lberian PlatfoY..~ Che force 9 regions are consCricted,
- which is connecCed wieh a sharp reducCion in Che seismic potential of Che
uplifCs bordering the ri�t zone to force $ and even 7(Primorakiy, Upper
Angara, NorChern Muya, Delyun-Uranakiy ridgea) and the appearance of pre-
dominantly (transit) Cremors with an inCensity to force 9 from the cenCer
zones of rhe force 10 earthquakea.
In seismotectonic reapecta the force 9 regions~ in contrast to Che regions
of maximum selsmicity, encompasa not only the rifr zone itself, but they
- also go beyond its limiCa. This is caused by the peculiarities of the seismo-
= geological relations and nonuniformity of the seiemic manifestations within
the limits of the transition morphosCructures. Thie nonuniformity is felt
primarily in the fact that Che force 9 regions are outlined in the cases of:
a) combination of local force 9 centers and "transit" force 9 tremors from
the maximum seismicity zones; b) auperposition of force 9"transit" tre:mor
- on the stru~tures within the limita of which the earthquakes wiCh M to
6 1/2 are poesible; c) local earthquake centers with intensity of force 9
(M > 6 1/2). ~
In connection with *_he facC Chat the paleoseismogeological data are explicitly
inadequate (on the basis ~f the fast denudation destruction of the traces of
the residual deformations in the force 9 pleistoseis!n zones), the analysis of
the seismological and geophysical materials has great significance when isola-
in~ the force9regions. Above all~ these regions are located within the limits
of the regions characterized by increased values of the seismic activity ~
(A p > 0.1). The same values characterize the epicentral regiuns of his-
torically known force 9 earthquakes (see Chapter VII). The same thing can
also be said about the K map on which the force 9 seismic regions as a
whole correspond to the areas where the occurrence of maximum earthquakes -
with K> 15 is assumed. The map of the long range furecast of the seismic
activity in general features also confirms the boundaries of the force 9
regions.
However, a direct comparison of the high force regions isolated with xespect
- to the seismogeological and morphostructural criteria with the maps of the
seiamic activity and maximum earthquakes indicaCes that in a number of cases
(Ol~k.~na-Chara ineerfluve, the northern border of the rift zone of the Stanovoy
~ liighland, the southern part of the Northern Baykal Highland, Eastern Sayan,
Khamar-Daban) there are noncorrespondences: force 9 seismic regions, for
example, are characterized by low values of A and K . The explanation
for this (in addition to the existence of thel~"zones~of calm" see Chapter
X) can be found in that the adopted functional relation K = K (A1
; does not take into account all aspects of the interrelationXOf t~ieXStrong
and weak earthquakes. Thus, for the viciniCy of the Ikat ridge with its
high valuea of A10 the abaence of si.:rong shocks (seismostatistics since the -
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beginning of rhe 19th century) and paleoaeismodielocationa ia chgrac-
teristic, and within the limite of Southern Baykal and the Tunkinakaya
zone for comparatively 1ow valuea of the seiamic act3~ity, epicenters ~
of atrong earthquakea and paleoseiemodislocaCiona are known.
The seismogeological and sei~smological etudiea per�ormed in the lasC decade -
on the territory of Eaetern Siberia permitted significant more preciae defi-
nition and more reliable aubseantiation of the boundariea of the �orce 9
aeismic regions. Here their areaa wer~ aignificanCly reduced on Che north- .
- eastern flank of the Baykal rift zone and from the direction of the marginal
part of the Siberian Platform. The total area of the force 9 regions in
the investigated terriCory by comparison with the seiemic regionalization
map of 1962 was reduced by 62,500 km2.
The small increase in area of the force 9 regions took place in WeaCern ~
Transbaykal within the limita of Che morphoeCructures of the transitional
type (I:~at and Tsipa-BaunCovekiy aecGiona)~ primarily as a result of the
force 10 zones (SEISMOTECTONICS..., 1968). For example, the vicinity of
the Ikat ridge has, according to the inatrumenC data, a very high level of
seiamic activity (A10 ~ 0.5-1), and the calculations of Che aeiamic vulnera-
bility permit us to expect earthquakea in it with an intensity of more than
' force 9 with a recurrence rate of 2,000 to 5,000 yeara. However, the absence
of clearly expreased paleoaeiamogenic structures does not provide grounds for -
isolation of a force 10 region here. In addit;tonP this area is located on
the periphery of the highly seismic rift zone and partially goes beyond its
limits. The nonuniformity'of the atructure of the earth's crust establishec~
in the Ikat region, and the "layer by layer" stress distribution in cross
section and different earthquakes with respect Ca center mechanism estab-
lished in the Ikat region (see Chapter IV) ~bviously create favorable pre-
requisites for constant relief of the sCressea by numerous~ but weak (K =
= 12) earthquakes. However, con connection with the seismotectonfc pe-~X
culiarities of the transition morphoatructures with i~road development of the
faults active in the Cenozoic (Ulan-Burka, Garga, IkaC, and so on) and the
formation of the embryonic basins in the axial part of the uplift, the iso-
lation of the force 9 region here appears to be substantiated. _
On the continuation of the Ikat zone to the norrheast there are transitional
morphostructures of the Bauntovskiy Region also considered in force 9. This
includes the Tsipa-Bauntovskiy system of subrift depressions, Kadalinskaya,
Bambubukoyskaya, the Tilishminskaya ~embryonic bas~Lns and the uplifts directly
bordering them. The seismic potential of these morphostructural elements is
- hi~h and can reach force 9-10 which is indicated primarily by the paleoseismo-
genic Khapton and Tilishminekaya structures detected here with an age on the
- order of the firat thousand years (see Chapter VII). The seismic activity
of the Bauntovakiy territory is high (0.1 < A < 0.35), and earthquakes
are possible with K~X to 16. However, the re~urrence rate of the force 10
_ earChquakes is sparse here (according to the seismologic datat, every 20,000
to 50,000 years). Thus, with reapect to the set of seismogeological data
the system of Tsipa-Bauntovskiy and Tilishminskiy transitional structures
is dietinguished by reduced (by comparison with the rift zone) seismic po-
tential and bel~ngs as a whole to the regions with force 9 seismic danger.
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Nere the Tiliahminakiy fault zone controlling Che development of the embryon- ,
ic baein gttd beartng Cracea of �orce 10 earChquakes remaine a region of in- _
creased selamiciCy.
The force 9 regiona both with respect to atruceur~l-teceonic and engineering-
aeiamogeocryological characteriaCics, and with respecC eo aeiamic danger~
are nonuniform. Wirh detailed investigaCiona ehis permits isolation (eape-
cially in the large rift basins with a Chicknesa of the loose depoaita of
more Chan 300 to 400 meters) of the areas~ the iniCial normative seiamiciCy
of wt~ich can be low by 1 force pnint. Neverthelesa, iC ie necessary again
to emphasize that under Che conditiona of Eastern Siberia in the force 9
- seismic regiona, especially on the island permafrost, the choice of sections -
for large-acale construction requirea preliminary detailed engineering-
- geological, aeismogeocryological and seismic atudies, ~nd the zon~s of
increased aeiamic danger (aeiamically active faults) in general must be ex-
cluded for capital conatruction (naturally, wiCh the exception of coum?uni-
caCiona). .
3. The areas with earthquake intenaity of force 8 occupy the smallest areas
in the mountain belt of Eastern Siberia, encompassing the marginal parts of
the Sayan-Baykal-~tanovoy arch. In Transbaykal they includa the vicinity
of the Chikoy Basin which previously was clasaified as force 7 increased
aeiamic danger (Solonenko, V., 1963a)2.
The isolation of the force 8 seiamic regions is caused both by the spread
of Che "transit" tremora from the highly seiamic regions and by local centers
with intensity to force The greater part of them are locaCed at signifi-
cant distance from the highly active rift zone.
- The boundaries of the force 8 regions are substantiated first of all by re-
duced seismic potential of the neoCectonic atructures on the limbs of the
- Sayan'-Baykal-Stanovoy arch and, aecondly, the width of the zones encompassed
by the "transit" tremors from the direction of the highly seismic (force 9
and 10) regions (see Table 20) [sic-=perhaps they mean Table 19--TranslatorJ.
In addition, the amall force S re~ions with respect to area are isolated
within the li~nits of the rift zone itself. This is primarily the internal,
deeply (more than 300-400 meters) plunged parta of the large rift basins
with weak differentiation of the basement removed from the seismic active
borders (for example, the No;cthern Baykal Basin). The scale of the map _
does not permit depiction of such sections in o':her rift structures with
thick series of loose depoaita. However, it is necessary to consider that
in the Tunkinskaya, the Barguzin, the Upper Angara, the Muya and the Chara
Basins it appears possible to is~late small force 8 area:~. Thi;~ pertatns
also tu the central, weakly differentiated parts of certain rift uplifts
(for example, Barguzin, Southern Muya, Udolc~n, Kalar and Kodar Ridges).
' 2 I:1 the SNiP-IIA, 12-69, by recommenda~�ion of the editorial commission o�
the Earth Phyaics Institute of the USSR Academy of Sciences it was inciuded
in Che force 6 regiona although this contradicted the factual data (Solonenko,
V., 1966a, page i67).
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On ehe whole, tM$ forc~ 8 regione, with reapect to their structural-geo-
logical peculiaritiea and nature of eeiamic manifeatationa, are still more
nonuniform Chan force 9. Among them the following are isolated:
1. Tt~e moderately act:ive areae (A ~ 0.02-0.1~ K < 14)~ whera both
local force 8 earthquttkes and the l~"transit" Cremoe from the center zonea
of highly seiamic (fo~ce 9 and 10) regiona occur. In the rif~ belt, as has
already been noted~ Cttese are the central parts of the large basins and the
axial sections of the arch-block and block uplifCe removed from the seie-
mically acCive faulta. These include also the f],a~nk morphoatructurea of
the Baykal rift zone within the boundariea of Che arch-block uplift of
Fastern Sayan and Stanovik. -
' 2. The weakly active (A1 ~ 0.01-0.05; K ~ 12-13) regions of predominant-
- ly "transit" tremors witFi~low recurrence ra~e of local shocks wiCh intenaity
to force 8. These are the marginal, weakly differentiated parte of primarily
the arch uplifCs and depression lowlanda in the *_ranaiCional region to the
Transbaykal block-wave zona.
3. The in practice "centerleas" areas with extremely low values of the
_ modern seiamic activity (A10 < 0.01)~ where only the "transit" tremors are
exhibited. Theae are predominantly the n~arginal (ahield) uplifts and to a
leaser degree, the foothills troughe of th~~ activated part of the Siberian
Platform.
4. The moderately active region of the Ch3koy Basin in Southwestern Trans-
baykal (see below).
The macroseismic atudy of atrong earthquakes (force 9, 10 and higher) in the
- territory of the Mongolian-Baykal aeismic belt and the seismogeological
analysis of the residual deformations indicate (see Table 20 [sic]) that
the force F aurface effects extend from the epicenter of the force 9 earth-
quake (with a depth of center of 15-20 km) to a diatance of up to 130 km,
and force 10, to 160 lan. Accordingly, an extraordinarily nonuniform intensity
distribution on the earth's crust.ia noted (especially in the preaence of
complex engineering-geological, geomorphological and geocryological condi- -
tions). Therefore the "mechanical" outlining of the force 8 regions by the
magnitude of the establiahed maximum radii of the corresponding isoseisms
can lead to aignificant un~ustif ied expansion of the area of the regions.
The "tranait" tremors of the force 9 and 10 center zones of highly seismic
regions are in the final analysis defining when drawing the boundaries of
the force 8 regions. Here, in all of the known cases the force 8 macroseis-
mic effects (average) of the strongest earthquakes of the Baykal-Stanovoy
seismic zone have not spread more than 160 km from their epicenters, and
this boundary was taken as initial for the initial external boundary of the
force 8 r~gion. Then it wae corrected depending on the seismotECtonic situa-
tion, the nature of the epicentral fields, the isolines of seismic activity,
K~X, and so on. Here a check was made wi~h respect to macroseismic effects
(a so average) from the force 9 center zones. However, for definite quanti-
= tative estimates of these regione (especially in the marginal zones of the -
Sayan-Baykal-Stanovoy arch) there are still insufficient instrument and
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seiemogeological data, and it ia neceasary to uae the materials with re-
spect to oCher eeiemicnlly active regione (Mongolia, CenCral Aaia, Cali-
fornia, and so on).
On withdrawing from the axial Baykal-Stanovoy seiemic zone, two force 8
regions are isolated in which the centera of the local earthquakea wieh -
an intenaity to force 8(K < 15) are posaible. In the inveatigaCed
- territory of Eastern Siber~aX boCh of theae regiona are repreaented only
by their marginal parrs.
One of them--the northwestern flank of the extended Tukuringra-Dzhagdinakaya
seismically active zone--encompasses part of Che Chernyaheva and Tukuringra _
ridges extending to the Upper Zeyak Basin. This reg{on on the exiating
seiemic regionalization map (SNiP-IIA 12-69) belongs to force 5-6. How-
ever, the aeiamogeological and the inatrument aCudies performed here in
1970-1971 and in 1974-1975 in connection with planning the BAM [Bayka~-
Amur Railroadj route and building the Zeyalc Hydroelectric Power Plant
[SEISMOTECTONICS..., 1975b) have made iC poasible to reexamine Che eatimaCe
- of the seiamic conditions of thia territory.
The force 8 potential seiamicity here ia determined by the modern tectonic _
- activity of the Tukuringra arch-block uplift and the systems of latest faults
bounding it (Gilyuyakiy, Tukuringra, Southern Tukuringra, and so on),
partially entering into the Mongolian-Okhotsk deep fault zone. These struc-
tures are connectE~d with quite numerous epicentera of earthquakes with
K= 9-14. In recent years force 6-7 shocks were recorded here, and on
_ 2 November 1973, the Zeysk earthquake occurred with M= 5.6; K n 14~
I~ = force 8(Semenov, Avdeyev, 1975). It confirmed the correctness of the
isolation of the force 8 region along the Tukuringra zone. According to
the preliminary seiemogeological materials, in 1967 V. N. Solonenko already
_ forecasted high seismic activity of this territory.
In connection with what has been discussed, the force 5-6 estimate of poten-
tial seismicity of the Zeyak Region finding reflection in the SNiP II-A.
12-69 appears to be extremely unaubstantiated, which, beginning in 1967, was -
made known by the design organizationa (Lengidroproyekt, Gidroproyekt).
In Southwestern Transbaykal, the Chikoy Basin is considered to be force 8.
According to the aeismic data in it moderate seismic activity is noted
- (A10 = 0.01-0.02; K~ < 13), th~t is, the expected maximum earthquake in- -
tensity here can reac~i force 7.
However, the Chikoy Basin is part of the broad Khentey-Daurskaya seismically
active zone which reaches into Northern Mongolia. The western segment of
this ~�-~ended zone in the territory of Mongolia exhibited itself in 1905
with the strongest earthquakes (M = 8.4 and 8.7; JD = force 11 and 12).
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. ,
For the viciniey of the Chikoy Basin~ gccording Co ~elamoeCatistics~ a
force 8(M ~ 6) earthquake wae knnwn in 1934 (Solonenko, V., 1968a~ page
367); in addition~ during the eeiemogeological aCudies (Laetochkin, 1972)
- the residual deformationa of Che force 9 earthquakes were establ3ehed here
(the Yadrikhinekaya and the Kuyuktuyekaya etructures). The posaibility of
the occurrence of the centere of force 8 earthquakae in this area ie also
. indicated by the higheet magnitude of the velocity gradienta of the verCical
neot8ctonic~movements for the territory o� Tranebayk~l-- ~grad V~~ x(0.4~-0.6)�
�10' year` ~
All of thia forces us to clasaify the Chikoy Basin as force 8. Its bound-
ariea are drawn conaidering Che nature of the damping of the macroseismic
effecta in the example of the earthquake of 1934 (Popov, 1939) and uaing
data on the averaged isoseiame (aee Table 29 (sicJ).
The regions with earthquake intenaity of force 7 encompass large areas with
comparatively weak differentiation, contraet and inteneity of the latest
tectonic movementa. On the one hand theae regione include the weakly active
(A p < 0,01; K < 12) marginal uplifta of the Aldan Shield, the Northern
Baykal and the�~xPatomakiy Highlanda and the poCentially aseismic marginal
troughs and uplifts of the Irkut amphitheater, and on the other hand~ the
~ greater part of the Transbaykal block-wave zone (A - 0.01-0.05; K ~ 12-
13) and the aection of the Nyukzha-Gilyuyekiy depression between theagtanovoy
Uplift and the Tukuringra Ridge.
In the direction of the Siberian Platform, the centera of local earthquakes '
(with K w~.thin the limits to 10) are extremely rare with the exception of the
activated part of the Aldan Shield were in the vicinity of the Chul'man
depression and the uplifts framing it on the north, increased seismic activity -
is noted (A10 to 0.05), and it is poseible to expect an earthquake with
Km8 = 13). The aeiamic dangers of these territories is determined basically
by ~he "transit" tremors from the center zones of the force 8-10 regions.
In the Irkut amphitheaCer, the local force 7-6 centers are in practice ex-
cluded. At the same time the macroaeismic data with respect to strong earth-
quakes from the highly seismic zones give riae to the isolation of the force
- 7 region over a significant territory of this atable and rigid block of the
eaith's crust, including primarily the Priatanovoy and Predbaykal'skiy troughs.
On the whole the boundary of the force 7 region on the Siberian Platform side,
by comparison with Che preceding map, was left unchanged with the exception
of the small aections in the aouthern part of the Aldan Shield and in the
Baykal-Patomakiy Highland where it is augmented as a result of the force 8
region.
The new force 7 seismic region is isolated in the southern p~rt of Yakutia _
_ within the limits of the marginal structures of the Siberian Platform, the
seismicity and the latest tectonics uf which have not been investigated,
and therefore they were coneidered aseismic (with respe~ct to their platform
situation). However, on 8 October 1974, a force 7 earthquake occurred here
(M ~ 5.2; K= 13), the epicenter of which was located in the Berezovakiy
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trough (see ChapCer VII). According Co Che exieCing macroseiemic materials, -
here a quite eignif icant force 7 area with respect Co aize was isolated,
Che basic parr of which mueC be to the norCh, in Che Y~kut aeiemic zone,
where the system of extended faulte running from ttortiheaeti to the Berezov-
skiy trough was ieolated. The boundaries of tihe region before performing
tihe sp~~cial seiamogeological atudiea must be conaidered quiCe approximaCe.
The broadest force 7 region encompaesea part of Weatern Tranabaykal, Central
Transbaykal and a small area of Easeern Transbaykal. For atrong earthquakes
in the Baykal-Stanovoy zone, the tremor intensiCy reaches force 7 for epi-
central distances to 320 km, and in individual cases to 500 and even 675 km.
Thu~, for example, for the earthquake of 1 February 1725 [sic] the center
of which is moat probably located in the Ukokan seiemically active zone~
in Chita (the epicentral distance is abouC 600 km)~ even Che force 8 macro-
- aeismic effecta were noted. Here, during the Muya earChquake (about 500 km)
on 27 June 1957~ numeroua cases of deformations of the atructurea correspond-
ing at least to force 7 macroaeiamic effecCa were noted, and for Che Tas-
Yuryakhakiy (675 km) on 18 January 1957, individual cases of auch deformations.
The seismogeological data, the increased velocity gradients and also the rela-
tively high degree of differentiation and contrasC of the vertical neoCec-
tonic movements indicates the posaibility of the occurrence in the investi-
gated areas of Transbaykal of 1oca1 force 7 earthquake centers. These in-
- clude the Uletovskoye earthquake of 1912, the group of Western Transbaykal
shocka of 1835) 1856 and i,915, the earthquakes of 1963, in Priargun'ye and
1965 (M = 5 1/2, in the v:lcinity of the Daurskiy Arch. In a number of places, -
' seismogravitational structures are noted (for example, Tanginskaya in Che
border of the Ingoda Basin). With respect to Che seismological data, over
a significant area of Transbaykal earthquakes are possible with K = 13.
Here the relatively high ~~alues of the velocity gradients of the �vertical
neotectonic movements (2�~'.0-O~grad V~m < 4�1'0'9 years'1) serve as confirma-
tion of the force 7"background" seismicity, which, according to M. V.
Gzovskiy, can correspond t~ force 7~~and more rarely force 8 earthquakes. -
Some expansion of the area of the force 7 regions in Transbaykal is caused,
on the one hand, by the appearance of new seismostatistical materials indi-
cating the local force 7 ea~.rthquakea (22 June 1963, M= 5.3, K= 13;
21 November 1965, ~ 5 1/4,, K@ 14; 3 September 1970, M= 4.5,�K m 13),
and on the other hand, more careful analysis of the seismotectonic situa- -
tion, including the velocity gradients of the lateat movements. ;
Ttie total area of the force 7 regiona in Eastern Siberia have increased by
comparison with the 1962 map and SNiP-IIA. 12-69, from 516,000 to 558,000
km2 both as a result of a reduction in area of the force 8 regions (the
Aldan Shield, the Baykal-Patomskoye Highland) and as a result of e~cpansion
of the force 6 regions (EPStern Transbaykal).
The regions with earthquake intensity of force 6 are isolated on the Siberian
Platform and in the southeastern part of Che Transbaykal block-wave zone
(Eastern Transbaykal subzone). -
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On the pl~Cform the area and confi~uration of Che force 6 aeiamic region
are caused by the naCure of propagation of Che "traneit" seiamic oecilla-
tions from force 7 og Che Baykal-Sta~n~ovoy zone of the arch-block and rifCo-
genic movements~ In SoutheasCern Tranebaykal~ on the contrary, the 1oca1
center zones (K < 13) have defining significance, and the "CransiC" tremora
play the subord~nate role. As a reault of the remoteneae of th~ aeiemic
stationa from these areae~ the preciaion of determining the epicenters of
the eartihquakes ie inaufficient to establiah the relation of the earthquake
centers to the epecific geological atructures and the morphoatructurea.
_ On the Siberian Platform aide, the boundary of the force 6 zone is quite
reliably aubatantiated by the seiamostatistical material~ and therefore in ~
general is left without change by comparison with the previously exiating
m~p (Solonenko~ V., 1963a, 1968a). At the eame time, within the limits of
the Eastern Transbaykal aubzone the area of the farce 6 region is increased -
as a result of the force 5 region isolated here. Thia ie cauaed primarily
. by the new seiemostatiatical data and increased values of the v locity
gradienta of Che verCical lateat movements to (1-2)~10'9 years-~.
The most active in the terriCory of Eastern Transbaykal appesrs to be the
Nerchinako-Zavodskoy region where weak ahocks have been quite frequently
recorded (K < 12), and in individual years (for example, 1700, 1800, and
so on), stronger earthquakes were noted according to he macroseismic data.
The latter, poasibly, are connected with the "transit" tremors from the
- Sranovoy and the Mongolian-Okhotak deep fracture zone. It has not been ex-
~ cluded that part of the weak local earthquakes here are not of tectonic
origin, but landslip orig~~ (collapses of old mines, karstic caves, and
so on).
Peculiarities of the Seismic Manifestations Under Permafrost Conditions
The problem of special engineering-seismological conditions of the perma- -
_ frost region has been recently stated (Solonenko, V., 1960b, 1962a), but
purposeful special studies were started only in 1966 on the east bank of -
the Baykal rift zone wher~~ high seiamic activity and complex permafrost,
the thicknesa of which varies in short distances from 0 to 1100-1300 meters
are combined (Nekrasov, et al, 1967; NQkrasov, 1970). These and subsequent
studies performed under the direction of 0. V. Pavlov in the Barguzin rift
valley and in Transbaykal, and laboratory experiments confirmed thz proposi-
~ tion of eharp contrast of the variation of the seismic vulnerability as a
function of the permafrost c~nditions (Solonenko, V., et al., 1970, 1972;
- Pavlov, et al., 1972; Zarubin, Pavlov, 1973; Dzhurik, Leshchikov, 1973;
the necessity for isolating a special engineering-seism~geocryological
= region in the seiamic region has come. In the Northern Hemisphere3 it
occupies an area on the ordez of 10 million lan2, that is, about 3.5 million
km2 in the territory of the USSR, and the rest in North America (Canada,
Alaska), Northeastern Greenland and on the islands in the Arctic Ocean.
3 The Antarctic ie in practice aseiamic. v
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The effect of the seiamic proceases on permafroat is especially cle~rly -
and directly obvious in the aeismogenic etructurea which during atrong
earChquakea experience multimeter vertical and horizontal displacements.
Here old fracture zones are uncovered~ and new ones occur which insure
Che conditiona for the formation of anomalous endogenic (ascending) and
_ exogenic (deacending) Chermal fluxes.
The most high~y seiamic permafrost region in Eurasia is the Baykal rift
zone. The cryolithozone is extraordinary here. In the rifC valleys there
is permafrost of the "Baykal type" (Solonenko, V., 1960b): even near the
southerY? boundary of ehe cryolithozone the permafroat is encountered to a
depth of hundreds of ineters. In tihe section the permafrost has two layereu
atructure. The upper horizon ia modern, predominantly insular permafrost ~
to Cena of ineCera thick and rarely more than 100 meCers (in the northern
basins according to the geological data, to 200-250 meters). The lower _
horizon of the permafrost ia relict, syngenetic. It was formed obviously
on the boundary of Che Holocene where the climatic conditions promoted the
formation of permafrost, and the high mobility of ~he earth's crust noted
- by seismic acti~�ation, its aubmersion and burial. These horizons rarely
_ merge; as a rule, they are aeparated by a horizon of thawed ground from
tens to hundreds of ineters thick.
The Baykal type ~erma�rost can b~ encountered noC only in the rift zone but
also in other geological structures experiencing aignificant plunging at
the end of the Pleiatocene to Che beginning of the Holocene.
The dependence of the cryolithozone on the type and nature of movement of
the tectonic structures has been confirmed by the geothermal observations =
, (Demidyuk, 1968). The least value of the thermal fluxes (on the order eri
300 kcal/m2-year) and greatest thickness of thE: permafrost were established
in the negative structures. A significantly higher thermal flux to 4,000 _
to 26,000 kcal/m2-year in the positive atructures and maximal, to 160,000
kcal/m2-year and more was established with respect to the tectonic dis-
turbance zones. There�ore in the seismically active regions, even in the
- frozen layer of low temperature (to -10� and lower) thick (to 1100 meters
and more) permafrost, narrow, but extensive taliks [thawed ground] are
encountered coordlnated with the zonee ~f tectonic disturbances and, above
all, ttie seismogan:ic lineaments. They _:re often well deciphered with re-
spect to vegetat-ion, more "luxurious" and heat-loving by ~omparison with
the vegetation of the sections alongside. However, there can be exceptions
to this general rule. The inactive faults, during the course of the seismo- ,
genic movements of the earth's crust, often passively open up, and cold
- air can pour into them, which will promote the development o' permafros~
and the formation of lode ice to significant depths (on the east flank of
the Baykal rift zone on the Udokan Ridge we were able to observe veins of -
ice to tens of centimeters thick at a depth of about 700 meters).
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The p~rm~froet esaentielly coroplicetes the geismic regionalization~ The
proper ~~lection of the combingtion of pernafroet and aeigmic ch~racterie-
tir.g he.e important algnificance here. Kowever~ it ie imposeible to con-
eider a11 of the v~riety of permafrogt condiel.ona; Cherefore unavoidgbly
it is necessery to ~ise a rough classification geocryological echeme. Ag
, the fir~ti pxperiment~ the following vereione was proposed (Solonenko~ V., ~
1973): I--individual iglande; II--insular; III--with talik ielands: a)
block, b) cellular or mosaic; IV--continuous; V--Baykal type.
The aeismic propertiea of permafrost depend not only on the granulometric '
composition~ the icinese and temperarure, but also the thicknesa of the
permafrogt, Che con~iCions of ite oc~urrence, ar~d so on. These relations ~
are varied; many of tr?~m have eCill not been atudied. In the first ap-
proximation the perma,froet is di~~ided up with reapect to aeismic ~roper-
ties into hard frozen, platy and paeudothawed and loos~ly frozen. The
solidly frozen includes the ground, with .reapect to the velocities of the
longitudinal se,9mi.: wavea (3.5-4 km/s~c and higher) and the oscillation
emplitudeb~ simila~ to rocic. Its temperature is below -2 to -3�. Ti~e
loosely frozen and pseudothawed ground has temperaturea above -1�~ and
tre seismic propertiea of this ground are appr�oximately the same as for
the truly thawed ground. The platy frozen ground takes an intermediate
. position with reapect :o its seismogeocryological characteristics.
Witi~ the accumulation of factual material, it appears possible to classify
_ the aeismic permafrost-lithologic complexea. Their boundaries far from
a:ways coincide with the boundaries of the engineering-geological micro-
districts. For example~ in one seismic lithological-permafrost cAmplex
there can be platy frozen coarsely clastic depc.eits and solidly frozen
fine grained soil (the velocities of the longitudinal wavesy frequency-
ampl'.tude characteristica of them can be in practice identical). On mr~king
the rransition to the pseudothawed or thawed etate the force of the former
is higher by one and the latter, by two or three; the bearing capacity and
other geotechni~al properti~es will be different.
F.ach of the isolated types of permafrost tias its osm specific engineering- `
seismageocryological peculiarities.
Type I. The thickneas of the permafrost in indiviciur~l islands usually is -
less than 15 to 20 metera. The thin (firat tens of ineters) lenses of perma- -
frost either have no significant effect on the amplitude level of the oscil-
lations or during passage of the seismic waves they cause aharply expressed
resonance phenomena. In the pre8ence of water saturated soil above them
. capable of mud eruptions, the permafrost lenses can receive additional low
frequency oscillations. The breaking up of the beds ar.d lenses of perma-
frost, the settiing of the individual blocks and fast degredation of it are
not excluded. Therefore the construction of the capital structures on the
- permafrost islands without preliminary thawing of it in the seismic regions
is undeairable. -
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Typ~ II. Insular permafrost usually is high temperature. The aoil is
pl~ty frozen dr pseudnChawed. By comparison with the rock and solidly
froxen ground the intensity of the earthquakee rige~ by one to three
force pointg~ Th~ fine-grained highly icy ground wiCh layered and reticu-
lar gtructure ie especiglly dangeroue.
. With a permafroeC thickn~as on the order of 20 to 40 metere in Che presence
of interlayers of thawed or pgeudothawed ground in it, resonance phenomena
and an increase geismic danger by tWO to three force points are probable.
In the presence of talik and p~eudothawed sinks~ cumulative prc~cesaes are
probable which can involve mulCiple increase in amplitudes of +.he oac~lla- `
tions and spouting of the ground in the central parte tne ealike.
Construct~on in this type of permafrost i~ also ut'~deF~irable~ but it can
tiurn out Co be unavoideble, for it irequently de~rp3ops in the moet conven-
ient areas for deve?opment in river valleys and intermontane basins.
Type III. Permafrost with talik ialands can turn out to be the moeC complex
(especially Che cellular aubtype) for engineering-seiemogeocryological ex-
ploration and regionalization ae a reault of the whimsical combination of
solidly frozen~ platy frozen~ paeudothawed and thawed ground with aharply
different seismic properties~ and the morphology of t,: cryolithozone itself
promotes broad and varied manifeatation of reaonance and cumulative processes4.
~or the blocks subtype permafrosC the talik lineaments next to the faults
are the most aeiemically dangerous as a result of the total increase in
force points as a result of thawed ground and movements along the disloca-
tions with a break in continuity. _
The variations in the force poiats by comparison with the initial ones in
the areas with type IZI permafrost can fluctuate from minue oae or taro to
plus one to three points.
Type IV. The solid permafrost predominantly With solidly frozen ground in -
the foundation of the structurea. When constructing while retaining the
permafrost, the normative force pointg can be lowered by one. Uaually the
structures are erected on pilinge with ventilated basements. However, the
nature of the operation of the pilings in two (Winter) or three layer medivm~
seismically sharply nonuniform~ remains unclear. The oscillations of the
foundation are realized as a result of the upper part of the ground, and
with depth the amplitude of the oscillations decreases rapidly. All of this
can lead to powerful shearing atresses of the pilings. Ho~+ever, the latter
can play the role of a clexible foundation which under defined structural -
characteristice has a F~~sitive effect on the earthquake proofness.
4 This
proposition hae found confirmation in the instrument engineering-
seismological atudies petformed under the direction of 0. V. Pavlov. It
was eatablished that in the talika of limited size the increase in intensity
of the tremors reachea force 2.
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Und~r ~Cructures with hot Cechnological processea~ as a rule~ Cglik ainks
occur Which have a~hgrply negative effect on their eeiemic conditions.
Type V. In Che areae with Baykal type permafroaC~ a number of apecific
engineeri~g-seismogeocryological problems ariee. The multilayered struc-
ture of the loose series fi}lling Che basine of the Baykal type can change -
the is~~eismal field sharply. Yt is poseible that thie ie one of the causea
of eignificant divergence sf the intensity of the tremors not only in the -
closely Iocated ground, but evea individual p~rts of the same atructure
which we have often encountered when inveatigating the consequences of
etrong earChquakes (Solonenko, V.~ 1960c).
Before the apecial stu~diea of the aeismic propertiea of the areas with perma-
frost of Che Baykal type iC is neceaeary to orient ouraelves on the proper-
ties of the upper (modern) horizon of the permefrost considering that the -
lower thick (taundreds of ineters) aeries of loose and frozen sedimenta ex-
tinguiah the force of the aeismic shocks aC leasC by one point (Solonenko,
V.~ 1962a; ACTIVE TECTONICS..., 1966).
In the case of seismic re~lonalization of the permafrost region it is neces-
sary to compile either a complex permafrost-seismic map or auperpose a
geocryological map of the same scale on the basic map. The detailed seismic
regionalization ia most efficiently carried out on the basie of the morpho-
structural complex engineering-geological and geocryological regionaliza-
tion.
In the case of seiemic microregionzlization, in accordance with the basic -
construction principlee (While maintaiuing or destroying the permafrost)
, it is proposed that two maps be compiled: for natural conditions and for
thawed ground (Solonenko, V., et al., 1970, 1972).
, For xegionalization of the territoriea of the specific Rtructural complexes,
a specialized map can be compil~d considering the new postconstruction perma-
frost conditions or temporary mapa with respect to the periods of mastery
of the areas, considering that the temperature, the iciness, the ratio of
the solid and liquid phases of the Water~ porosity aad denaity of the soil
during the courae of developmeat and during the year vary continuously re- ~
versibly and irrevereibly. The seismic properties of the rock vary corres-
pondingly: acouetic rigidity, amplitudes and periods of the oscillations
- of the ground, resonance and cumulative properties and also the nature of
_ the interaction of the ground-structure system. An earthquake has an active
effect on the courae, especially the rate of the geocryological processes
_ and phenomena: solifluction is accelerated, the movemeat of places is
facilitated as a reault of the masa alipping of the active layer, the -
established thermal regimen of the upper horizons of the permafrost is dis-
turbed, which causes degredation of it With all of the consequences follow-
ing therefrom~ and it promotes the formation of ayalanches. At the same time
the permafrost to a significant degree determines the nature of the seismo-
gravitational phenomena, conaolidatiag the rock masses on the slopes and at
~ the same time reducing the number of landslipa, laadslides, earth and rock
avalanches~ especially during earthquakea o~curring during complete freezing
of the active layer.
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The Oymygkonskoye earthquake of 18 :tay 1971 (force 9~ M~ 7) wae indica-
tive in thia respect. Its epicenter was near the pole nf cold of the
Northern Hemiephere. In Che pleisCoceism zone over an area of 3 x 6 km
along the fau1C zone maseive separations of the Chawing parC (abouC 0.3
- mecere) of the nctive layer occurred. Tne soil-vegetative mgs~ in the
velleys of the r;vers formed mud flowa up to 5 to 6 meCern thick. On the
general alopes (to 15�) and in the horizontal aections mass spouting of
fine gravely type soil occurred (Kurushin~ et al., 1972), but it was not
accompanied by significant aubsidence aa is observed in Che permafrost
areas. On the whole, as a result of the permafzost~ the seiamogravita-
tional phenomena during this earthquake encompaesed a smaller area and
had amaller dimensions Chan for idenCical earChquakes in the nonperma-
froat areas.
The distribution of tne tremors ov~r the aurface of Che earth was also re-
markable: in the area with solid permafrost Che inCensiCy of the Cremor
wae regularly attenuated. At a distance of 250 to 350 km, it dropped to ~
force 4 and then conCinued to aCtenuate. but at the epicentral disCance
of 450-500 km on reaching the inoular permafrost region near the Sea of
Okhotsk, the intensity of the tremor rose by 1 to 2 pointe. The force 4
tremor ~ras felt on the coast of the Sea of Okhotsk at a distance of about
700 km. The relation of the tremor intensity to the type of permafrosC in
the given case is obvioua and indisputable (Solonenko, V., 1972a).
Tt~e extended iced zones frequently are connecCed with fissure-stratal water
of the seiamogenic lineamenta. In the seismogenic ~ointed zones in places
very thick ice fields are formed--to 10 t~ 15 meters or r~ore in the Syul'-
banskaya~ China-Vakatekaya seismogenic structures of the rift system of the `
Stanovoy Highland (ACTIVE TECTONICS..., 1966). During the earthquake some- -
times a powerful "volley" eruption of water takes place which under winter
conditions leada to disastrous formations of giant ice fields. Thus, during
- the Gobi-Altay earthquak~ of 4 December 1957 (force 12, M= 8.6) an ice -
field more tfian 10 km long was formed (Solonenko, V., et al., 1960a).
-
' Ir. the sections with highly icy soil the earthquakes cause or activate
thermo{:arstic processes. This is insured either as a result of the forma-
_ tion of fissures through which the ground ~rater and surface water pours
into the permafrost or as a result of throwing off of the active layer and
uncovering the permafroat. Strong seismic shocks are not necessary for
this; weak earthquake awat7ns can cause the same effect. For example, in
1967 in the vicinity of Leprindo Lake in the Stanovoy H~.ghland in the epi-
central area an earthquake swarm (85 ahocics) of moderate intensity (K to
10-11) suddenly formed a thermokarstic mud valley 650 meters long, 10 to 15
metera wide with a depth to 6 metere and a thermokarstic sink more than
2,500 m2 in area and 20 meters deep (in moraine).
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Engineering seismogeology has been faced wiCh complex problems in general~
and especially under the conditions of permafroat (Slonoenko, V., 1971~
19~3). The existing meChode of ~eismic regionalization have been developed
ueing the materials from the seiemic regions of osr southern republics and
foreign countries with poeitive geochermal regimen of rhe aoil. The engi-
neering-geological and instrumen~ aeismological obaervaCiona give the soil
- parameters, characterietic of them during the investigation. During further
engineeric~g-seiemogeological interpretation, the etability of theae parame-
ters ia underetood. Under permafrost conditiona the geotechnical and seiamic
_ properti~s of the soil in the vicinity of Che ef~;ective engineering aCruc-
tures change conatantly. Therefore the existing development wiCh respect
to the aeiemic regionalization procedure, eepecially microregionalization
are unacceptable to a eignificane degree in a permafrost region.
All of che growing .~�atea of developmenC of seismic regions in permafrost
areas are bringing about a new acientific area--engineering seismogeocry-
ology.
We have alread had the o .
y pportunity to state (Solonenko, V., et al., 1~71)
that in the seismic areas of permafrost regions, during construction the
antiseismic measures must be combined with antipermafrost measures. There-
fore in order to aelect optimal construction sites the seismological and
engineering-~eocryological exploration ie ineufficien~. A careful economic
analyais is also needed. For example, conatruction in a force 8 region
with inaular permafrost (types I~ II and partially V) can be more expensive
than in a force 9 region but with favorable engineering-~eiamogeocryological
conditiona.
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CONCLUSION
The analysis of the seismological. seiemogeological, geophyaica]. and paleo-
seismological data wiCh respect to the Eastern~ Siberian seismic region has
demonetrated that on the modern level of scien~,ce, the seismic regionaliza-
tion can be carried ouC only with complex uae of the enumerated materials.
Depending on the local conditiona, the "weigYi~t" of certain data can be .
varied significantly.
In spite of the obvioua achievementa in aeiamc~logy, aeiamogeology and geo-
physics, the aeiemostatiatical (macroaeiemic ~,ad inetrument) and paleo-
aeiamogeological data rem$in as before the on].y reliable data for eati-
mating the true level of aeismicity.
At the preaent time far �rom all of the territ~ory of Eastern Siberia has
been encom~asaed by the comple~ studfes. The basic efforts have been aimed
at studying the most seismically active parts-~-the Baykal rift zone--which
has been investigated in quite eome detail ove~.r its entire extent (about
2,000 km).
As a reeult of the complex studies it was disc,overed that the Baylcal seismic
_ belt is with respect to external signs alone ~~art of a united Asian aeist�ic .
zone entering into Eaetern Siberia from Mongol,ia. At the southeasteru pro-
~ection of the Aldan Shield the seismic belt i,s branched: one branch is the
Dzhugdzhurskaya, which runs to the Sea of Okhc~tak, and the other, the
Verkhoyanskaya, turna sharply to the northwest; and runs to the rift system
of the Aretic Ocean. This purely external fac,tor (seismicity) has provided
the basis for certain authors to see the relat:ion of the Baykal rift zone
to the world rift 8yatem. However, the indivi,.dual parts of the seismic `
zone are connected With various types of neote~.ctonic structures, different
geophysical fielda and tectonic stresa fields. They ~ave different depths
and earthquake centex mechaniame, that is, thEuy are different with respect
to the main tectonic-phyaical signR.
As is known, the effect of the tensile atressEi.s acroes the structures is
one of the most characteristic (if not the dnl,y) aigns of typical rifts.
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In this respect the B~ykal rift zone is reliably ieolated from the world
rifC syetem by broad fields of near horizontal compresaion. Moreover, it
is exCremely complexly conetructed, both with reapecC to morphoatructural
aCtributee and the deep structure, and it has a mobile tectonic regimen~
Over Che greater part ~f ita extenC, Che various morphoetriicCures of th~~
Baykal syatem are undergoing energetic modern growth in the lateral and dis-
tal directione and rearra~gpment.
The growth of the baeina along the atrike is moet clearly expreea~d to Ch~
east of the Upper Angara Baein. Here the interrifC mountain commiasures
are broken by the newly formed basina which finda refleckion in the in- -
creased (by 3 to 5 timea by comparison with Che mean) ~eismic activity of
_ the interbasin mountain commissurea and also the easCern disCal zone of the
rift system. In the latter~ the riftogenic processes still have almost not
received morphosCructural expreesion. With reapect to the velocity gradienta
of the vertical tectonic nwv~menta, Che geophyeical and seiemological cal-
~ culations, K here is no more Chan 12 to 14 with rare recurrence rate.
ActuaYly, th~eXis one of the moet eeismically dangerous sectia~~s of the rift
zone with probable er.rong and frequent earthquakes with K to 16-17.
On the other hand, on ~he southwest (Eastern Sayan) flank of the rift system
fading of the riftogenic procesaea is taking place.
Whereae in the Baykal rift zone the seismic activity ie determined pri,marily
by the development of rift ba~ina, in the Transbaykal block-wave zone, the
arched uplifts have increased aeiamic potential. They are weakly recompen-
sated (see Chapter IV), and the energy of the compensation uplifts is small,
insurinA manifeatation of rsre atrong (to force 8, M to 6) earthquakea.
However, theee earthquakea are occurring, and it is imposaible not to con- �
sider them during s~ismic regiona~ization.
Between the Baykal rift and the Transbaykal block-wave zones a system of .
- aubrift structures has been isolated, the aeismotectonic development of which
is taking place on interaction of the movements of the riftogenic and Trans-
baykal typea. Thie hae also predetermined the potential aeismicity of the
subrift etructurea: the total amplitude of the vertical movements is: the
Neogene-Quaternary time in them is twice ae high as the Tranebaykal Basins,
but three to four times lower by comparison with the nearest rift vall~ys.
The poaeibilitiea of the occurrence of earthquakea of maximum t~tensity _
_ (more than force 9) here obviously are lower, which was taken into account
when isolating the seiamic regiun.
_ The Siberi~n Platform, appearing to be previously aeismically passive turned -
out to be not so lifeless. In any case, in its marginal part earthquakes
are possible and sometimea occur ~for example, 8 October 1974, K= 13�,
I~ a force 7) which are not inferior with respect to energy to the Tashkent
earthquake of 1966. Thia significantly expanda the area of the required -
seismogeological-geophysical atudies in Eastern Siberia (in any case When -
building structures of increased danger: the high-head hydroelectric power
plant dams, and so on).
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The quick improvemenC of Che aeiamic regionalization map of ~astern Siberia
� hae become poseible as a reault of Che appltcaCion of Che paleoseismogeo-
lo~ical method (combined with oCher methods of inveaCigarion). When u~ing
ttie populgr procedures (without paleoseismoge~lagical procedures) a long -
term accumulaCion of aeiamoaCaCistical material is required. The ob~ective
analyais of tt~e various data has demonserated rhaC wherever ehe upper 1eve1
of the seismicity of specific aeismogeni~ structurea (the rift zone) has
been deCermined by Che paleaseiamodislocationa with certainCy, Che seismo-
logical and geophyaical materials confirm the high values of K~X, A1U and
Che recurrence rates of the earthquakes.
Where there are no signs af paleoseismodislocations (the ed~es of Che Siberian
- Platform), Chere Coo, according Co instrument data the seismic activity is
equal Co or cloae to zero, although sometimes earthquakea occur here which
in the presence of populated places would be destructive. In the areas where
the paleoseismodislocationa are not expresaed or are absent (Transbaykal),
the seiamological data are unreliable. However, in auch areas with Cime _
the reliability of the seismological data will be increased, at the same
time As the proapecCa for improving the reliability of Che paleoseismogeo-
logical material are problematic. This again confirma the necessity for com-
41 plex studiea and not confining the atudies to any one method.
The paleoseismogeological data still remain rhe only dats when discovering
the evolution of seiamic procesaes which has great significance for esti-
mating the degree of reliability of the long-term seismic forecast accord-
ing to seismological-geophysical data.
In the uninveatigated or poorly investigated regions paleoseismogeology is
the only meana of fast determination of the epicentral zones of sCrong earCh-
quakes, their maximum intensity, the discovery of seismi~ally active atruc-
tures, and so on. In the broad investigated regions the paleoseismogeologi-
cal studies can essentially supplement the seismological data. While in prac-
tice the required time of instrument observations for ob~ective estimation
of the activity, K and the seismic vulnerability is actually unknown, we
can only say with certainty Chat the 10 year period of observations is too
small for theae purposes. For example, the only arch-block Udakon structure
coupled with a single system of deep faults noted over the entire extent of
the paleoseismodislocations of force 9-12 has A from 0.01 to l, K from
- 12 to 17, seismic vulnerability of more than for~e 9 of 1,000 and, more rarely
50,000 (see Chapter VIII and IX). It is natu~al that such calculations can
not be the basis for auch a serious document as the State Seismic Regionali-
zation Map.
The concluaion atill remains valid that we arrived at when studying the seis-
micity of the rift zone of the Stanovoy Highland (ACTIVE TECTONICS..., 1966)
~ that for quantitative eatimation of th~ recurrence rate of. the earthquakes
the rec;irrence rate graphs can be used if they are compiled for large se~smo-
genic structures or systems of them responsible for the preparation of strong
_ earthc;~akes (an area of no lesa than severxl tens of thousands of square
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- kilometers)~ Under our conditions tihp recurrence rata graphe increase the
number of earthquakes of force 11-12 and in this part must be corrected by
th~ paleoaeiemodislocations, but they give more reliable recurrence of Che
force 10 ahocks, the traces of which are quickly destroyed by denudation
and are in part skipped over during paleoaeismogeological studies.
During the course of thia work, coinciding itt time with the "boom" in Che
area of earthquake forecasCing (not only location and intensity but also -
- exact time), we have constantly followed the course.of these invesCigaCions~
~rimarily in Japan, Che USA and Che USSR~ anc~ we have tried to give an ob-
~ective evaluation of their reeulCs inaofar ae poesit~le. We have arrived
at the following concluaional:
1. No reliable relatione have been eatabliahed between the deep structure
and the level of modern aeiamic activity of the local areas.
2. Modern movemenCa of the earth's crust are not such a reliable index of
posaible seiamic activiCy; their ratea in the platform as~:iemic regions
sometimea are 2.5-6 times higher Chan in the highly active seiamic zones. -
3. The establiehed anamoloua movemente of the earth's cruat which frequently
, are considered as predictora of earthquakea Cake place several hours to 40
years before atrong earthquakes (the Alaskan earthquake of 27 March 1964),
and probable ones, to hundreds of yeara.
4. The hydrogeological (including hydrochemical) changes during the course
- of preparation for an earthquake or the earthquake itself are observed at
a distance of up to ht~ndreds, sometimes thousande of kilometers from the
epicenter and cannot be the basis for predicting the location, intensity
and time of the earthquake.
~
5. The predictiQri of strong earthquakes by seismic cycles (Fedotov, 1968)
begins with constancy of the aeiamic regimen. ~he facts indicate that con-
stancy of the seiamic regimen for local regions cannot be discsssed, and
it is only in thie case thgt it is in practice expedient to predict earth-
quakea.
An unfounded amount of attention has been given to the prediction of the time -
of earthquakes. The index of this is the fact that in mountainous regions -
up to 80 to 90 percent and more of the victims and material losses are not
connected with the earthquakes ~hemselves but with the accompanying seismo-
gravitational phenomena (landslips, landslides~ earth streams and avalanches,
mud flows). If in auch cases the time of the earthquakes were prediced, the
citiea and settlements would still be lost, 3nd the people would be killed.
1 From the report by V. P. Solonenko at the International Sympoaium on
Earthquake Forecaster Research (1974). ~ -
393 ~
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Therefore the engineering-eeiemogeological forecast in mountaine, especially
loese regions ie in pracCice more imporCnnt Chan the short-term �orecaeting
of the time of Che earthquake. Under perma�rosC conditiona (more than 50
peraent of Che area of ehe seismic regiona of Che USSR), the significance
of rhe engineering-seiamogeocryoloEical forecast is aCi~.l hi~her.
Mode.rn knowledge of the processea leading Co earthquakea do not leave room
Co doubt Chat the exacC prediction of the Cime of an earthquake ia still
unaCtainable. At the present time seismogeologists, seismolopista and geo- -
physicists can hy their collective efforCa with quiCe high reliabiliCy fore-
caet the location, poasible intettsity and approximate recurrence raCe of
earthquakes. "It ia vitally important not to predict the exact Cime when
a city will be destroyed but to construct it in a place and in such a way
that it will not be desCroyed" (Solonenko, V., 1974).
394 -
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BI$LIOGRAPHY
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395 -
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9. Argent'yev, V. P. "Problema of the Tectonica of the Sayan-Baykal -
Folded Selt~" in the book: MATERIALY K GEOLOGICHESKOY KONF~itENTSII~
POSVYASHCH~NNOY 50-LETZYU SOVETSKOCO GO5UDARSTVA I 10-LETIYU BURYAT5I:OG0
GBOLOGICH~SKOGO UPRAVLENIYA (Materials on the Geologir,al Conference
_ in Honor of Che 50th Anniversary of the 5oviet Union and the lOth
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DAL'NEGO VOSTOKA) (Tectonics of Transbaykal (Materials for the Tenth
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16. BAYKAL'SKIY RIFT. (Baykal Rift), Moscow, Nauka, 1968, 175 pages.
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20. Belousov, V. V. ZEMNAYA KORA I VERKHNYAYA MANTIYA MATERTKOV
(Earth~a Cruat and Upper Mantle of the Continenta), Moacow, Nauka,
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Siberia), Part II, Novosibirak, 1972, pp 59-65.
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(Soviet Geologya~ No 10, ~972, pp 134-139. _
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"Horizontal Dieplacementa along the Faults and Some Methods of
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1963, pp 5-33. -
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~
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~
UZB. GEOL. ZHURN. (Uz6ek Geological Journal), No 3, 1970, pp 3-7. I
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_ ' IN-TA AN SSSR (Works of the Seiamology InsCitute of Che USSR Acad~my
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36. Vvedenakaya, A. V. ISSLEDOVANIYE NAPRYAZHENIY I RAZRYVOV V OCHAGAKH
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38. Vnukov, A. V. "Geological Structure and Conditions of Formation of
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1967, 27 pages. -
_ 39. Voytovich, V. S. PRIRODA DZHUNGARSKOGO GLUBINNOGO RAZ~;OMA (Nature
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~OEt O~FtCIAL U5~ ONLY
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;
Fa~ ~~t~tetnt~ us~ ~rtt~v `
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10845
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