JPRS ID: 8751 TRANSLATION TECHNIQUES AND APPARATUS FOR REGIONAL SEISMIC RESEARCH IN INACCESSIBLE AREAS AND THEIR USE IN SIBERIA

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~ I FOR ~
SEISMIC RESEARCH IN INACCESSI6LE AREAS

6 NOVEM6ER i979 AN~ THEIR USE IN SIBERIA i OF 3
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~ JPRS L/8751 _
- 6 ~iovember 1979
Translation
TECHNIQt~ES AND APPARATUS
FOR REGIONAL SEISMIC a~SEARCH
IN INACCESSIBLE AREAS -
AND THEIR USE IN SIBERIA
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JPRS L/8751
6 November 1979
TECHNIQUES ANU APPARATUS
FOR REGIONAL SEISMIC RESEARCH IN INACCESSIBLE AREAS -
AND THEIR USE I~V SIBERIA
Novosibirsk METODIKA I APPARATURA DLYA REGIONAL'NYKH SEYSMICHESKIKH _
I5SLEDOVANIY V TRUDNODO5TUPNOY ME5TNOSTI I IKH PRIMENENIYE V SIBIRI -
in Russian 1978 signed to press~21 Apz'78 pp 1-208
[Book edited by V. V. Fedynskiy, "Nauka" Publishers, 1,500 copies]
CONTENTS PAGE
Annotation 1
Introducti~on 2
CHAPTER I. REQUIREMENTS ON REGIONAL SEISMIC RESEARCH
� 1. Subject, Goals and Charac~eristic Features of the -
Regional Seismic Research Method ~
� 2. Existing Deep Seismic Research Method 17 -
� 3. Requirements on the Equipment for Reconnaissance
Prospecting Seismic Research 21
CHAPTER II. THEORY OF SEISMIC SOUNDING
~ � 1. Properties of the Spot (Differential)Sounding Systems 26
� 2. Spot Observation Time Fields 39
� 3. Peculiarities of the Identification of Waves and Use
of Their Dynamic Characteristics 60
� 4. Sounding by Refracted Waves Using Hodograph Elements 64
CHAPTER III. REMOTF-CONTROLLEb TAYGA SEISMIC SYSTEM
~ � 1. Function Diagram of the Equipment 71
, � 2. Seismic Signal Magnetic Recording Channel 74
! � 3. Radio Remote Control System 78
' � 4. Structural Design and Basic Technical Characteristics
of the Tayga Equipment 85
- a - [I - U55R - E FOUO]
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CONTENTS (Cantinued) Page
CHAPTER IV. FI~LD OBSERVATION~ AND INTERPRETATION OF MATERIALS
� 1. Characteristic Features of Field Operations 90
- � 2. lliscrete Correlation Methods 109
� 3. Interpretation Procedures 121
� 4. Construction of the Seismic Sections by a Set of Data 148
CHAPTER V. StOT SOUNDINGS AND OTHER TYPES OF DEEP SEISMIC STUDIES
Testing the Sounding Procedure Using Continuous Profiling
~ Data and Comparison with the Drilling Data 153
� 2. Comparison of the Labor Consumption of Spot Soundings
and Continuous Profiling 162
� 3. Spot Soundings, Dash and Dot Profiling 170 -
CHAPTER VI. RESULTS OF USING THE SOUNDING PROCEDTJRE
� l. Deep Seismic Studies in Western Siberia 182
� 2. Studies of the Basement of the Western Siberian
P"latform 211
� 3. Regional Seismic Studies in the Siberian Platform 226
� 4. Deep Seismic Sounding of the Earth's Crust and
Upper Mantle in the Baykal Rift Zone 240
- � S. Studies in Foreign Ar~as 256
CONCLUSIONS 263
BIBLIOGRAPHY 267
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PUBLICATION DATA
English title : TECHNIQUES AND APPARATUS FOR REGIONAL
SEISMIC RESEARCH IN INACCESSIBLE AREAS
- AND THEIR USE IN SIBERIA
Russian title ; METODIKA I APPARATURA DLYA REGIONAL'NYKH
SEYSMICHESKIKH ISSLEDOVANIY V
TRUDNODOSTUPNOY MESTNOSTI I IKH PRIMENENIYE
- V SIBIRI
Author (s) ,
Editor (s) : V. V. Fsdynskiy
. Publishing House : Nauka
Place of Publication : Plovosibirsk
- Date of Publication : 1978 _
Signed to press ; 21 Apr 78
~
Copies ; 1,500
COPYRIGHT . Izdatel'stvo "Nauka," 1978
: �
~
I - c -
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_ UDC 551.1+550.83(571)
FROCIDURES AND E~UIPMENT rOR REGIONAL SEISrIIC STUDIES OF INACCESSIBLE
AREAS AND TIiEIR APkLICATI0T1 IN SIBERIEI
Novosibirsk I~IETODIKA I APPARATURA DLYA REGIONAL'1VYKH Sr'YSMICHESKIKH
ISSL~DOVANIY V TRUD1`IO~OSTUPNOY MiSTNOSTI (TRUDY INSTITUTE GEOLOGII I
G~OFIZIKA, No 389 [T�lorks of the Geolo~;y and Geophysics Institute, No 389])
in Russian 1973 sig,ned to press 21 Apr 78 pp 1-208
[Book by P1. N, Puzyrev, G. D. ~abayan, A.I. Bochanov, G. V. Yeg,orov,
S. V. Krylov, V. L. Kuznetsov, i�f. M. Mandel'baum, B. P. Mishen'kin,
V. IC. Monastyrev, A. L. Rudnitskiy, V. D. Suvorov, I. S. Chichinin, edited
by Correspondin~;l2ember of the USSR Academy of Sciences V. V. Fedynskiy
and Doctor of. Physical and r7athematical Sciences I. P. ICosminakaya,
Nauka Publishing Ilouse, 1500 copies]
[TextJ The results of research performed by a collective of Siberian ~eo-
physicists in an attempt to create a theory, procedures and equipment for
regional seismic studies in inaccessible parts of Siberia are discussed
in this mono~raph. P1ew data on the structure of the folded basement, deep
zones of the earth's crust and upper mantle have been obtained by using
the developed method of spot (differential) seismic soundings with the
"Tayga" equipmen~ in a number of areas of Siberia (the western Siberian
platform, the Siberian platform, the Altaye-Sayanskaya Oblast, the Baykal
ri�t zone).
This pager will be of interest to specialists in the field of developing
seismic research methods and a broad group o� geologists~and geophysicists
studying the deep structure of Siberia. ~
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INTRODUCTION
The basic prospects for increasing the reserves of the most important types
of mineral raw materials are connected with studying the deep structure of
the little-developed and to a significant degree inaccessible eastern parts
of our country Siberia and the Far East. Therefore the role of regional
- geophysical research aimed at quickly gathering information about the
- larae-scale structural features of the upper part of the consolidated earth's
crust, its deeper zones and the tops of the mantle over the entire territory
is especially important. This information is needed for comparative evalua-
tion of the prospects of the individual areas and the scientifically sub-
stantiated or~anization of ex~loration and prospecting for mineral deposit~.
The necessity for expandin~ the studies o.f the earth's crust and upper mantle
in order to understand the processes of the formation of the mineral deposits
= and their distribution laws has been emphasized in the "Basic Areas of
Development of the National ~conomy of *he USSP. in 1976-1980," adopted at
the 25th Congress of the CPSU. -
Seismic studies are acquiring greater and ~reater si~nificance among the
methods of subsurface geophysics. Tha primary work is being done by the
method of deep seismic sounding (DSS), that is, with the application of
powerful artificial oscillation sources. ~he upper part of the consolidated _
crust (primarily the surface of the platform basement) has been studied
for the most part by the correlation method of refracted wav~s (C.~~IItW).
The seismic techniques insure the highest accuracy and reliability of the
determinations of the deep structure; the data gathered using seismic tech-
niques are basic to the interpretation of the materials from other cheaper
and simpler geophysical methods which, as a rule, are cnaracterized by a
signif icant degree of ambiguity in the solution of inverse problems.
The problems of subsurface seismic research can be provisionally divided
into two groups. The ~irst group includes the problems o~ studying the
large--scale subsurface structural features over broad territoriea, including
geologically inhomogeneous provinces. The second group~�of problems reduces
to a detailed study of the relatively sma11 and most interesting sections.
In deep seismic research efforts are often made to~combine relatively high
detail with the study of large areas, which leads to high cost, slow
accomplishment of work and insufficient effectiveness of the detailed and
regional studies. At the same time examples of hi~hly successf~il
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deep seismic studies have been known unc~er the condition of concentration
of them on p~oblems of, only a regional or only a detailed nature. Thus,
new important information about the structure of the earth's crust and the
upper part of the mantle over large terr~tories has been obtained in rela- -
tively short time as a result of loc~.,detail. ' worec in the vicinity of the -
transition from the Asian Continent to the Pecific Ocean [111] and at the
transcontinental intersections of the ;vorth American Continent [128]. _
Detaile~ operations are nost effecti~e i.f they are not combined with the
solution of regional problems, examples of which include the studies of
parts of the Baltic Shield [23, 71], in the Jkraine [t07, l0B] and in other
areas.
The reconnaissance (low-detail} operations must precede the studies of a
detailed nature; they must be performed quickly over broad, sometimes ~
inaccessible areas hence, as is known, we come to the efficient strategy
of ~eolo~;ical-g~ophysical research [123].
Seismic studies of the reconnaissance type have long not been actually
perforr.?ed in the eastern parts of our country, for the existing procedures
~ and equipment in nractice have not been suitable for effective use under
the conditions of accessible terrain covered with tai~a, swamps and mountains =
and almost devoid of roads. Therefore by the be~inning of the 1960's a
- contradictory situation had developed: in the Siberian regions with their
colossal potential with regard to still undisco~~ered mineral resources,
such essential work had not been broadly developed primarily as a result
of the abserace of a procedural and equinment base. The application of the
well-known seismic procedures (CMRt1; DSS in the traditional continuous-
profilinQ version) turned out to have low efficienc_y. It was only possible
to investigate the surface of the basement of the platform regions on
individual routes and in localized areas, but this did not provide any
representative information about the regional structure. Over all of
Siberia there was only one 300-kilometer DSS profile in the southern, -
steppe region of the idestern Siberian plain (the Barabinskiy profile, the
work of the NTGU [Novosibirsk Territorial Geological Administration], and
the SNIIGGiMS [Siberian Scientific Research Institute of Geology, Geophysics
and t~fineral P.aw Materials 1953) .
In recent times, the improvement of the seismic method of reconnaissance
has been aimed predoninantly at increasing its detail and accuracy [1, 12,
31]. Tlie same trend is also characteristic of the development of a pro-
. cedure for deep seismic sounding [43, 71, t31, 85, 126). The purpose of this
paper is the use of the precedin~ seismic reconnaissance experience to -
create a procedure for relatively low-detailed subsur~ace seismic studies
over broad, sometimes inaccessible, areas.
The problem of the necessity for developin~ a snecial deep seism~c explora-
tion procedure for Siberi.an conditions, primarily as applied to the study
of the basement, was stated for the first time by V. I:. Monastyrev in
the ti~lestern Siberian.~Geonhysical Trust. In 1956, by his initiative a ~
successful test~ng of the si.mplified systems of observations by the method
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of refracted waves ca.lculated for use of the local elements of the hodo~raphs
of these waves instead of the difficult to realize continuous operation
systems, was started, Latez, this area was further developed p.rocedurally
and equipment~wise as well as in practice in the Tyumea~ Oblast. The mass
application anci development of simpli~ied r.efracted wave observations systems
took place dtirin~; the re~ional work in Central Asia and certain parts of
tlie Eurcpean territory of our country [24].
_ In 1961 N. N. Puzyrev, et al. began the de~~elopment of a procedure making
use of arbitrary systems of spot (dif~erential) seismic soundings with waves
_ of various tyPes (reflected, _heac'. waves, i~efracted waves, and composite
waves) at the Institute of Geology and Geophysics of the Siberian Department
of the USSR AcadeMy of Sciences. By rne middle of the 1960's, the main
components of this procedure had been developed and tested in practice:
the discrete correlation o� seismic waves; special two and three-dimensional
time fields, wtiich are a Eeneralization of the concept of the seismic photo-
. graph to the case of an arbitrary system of sources and receivers of
oscillations; the methods of determining the parameters ~f a medium by time
f ields; schemes for traverse and area seismic observations in inaccessibl~
areas.
Sinultaneously, a number of Novosibirsk, academic and branch er~anizations
(IGiG SO AN SSSR [Institute of Geology and Geophysics of the Siberian
Department of the USSR Acader.ry cf Sciences], IAiE SO AP1 SSSR [Institute of.
Anthropolo~y and Ethnology of the Siberian Department of the USSR Academy _
of Sciences], S:IIIGGir1S P1G SSSR [Siberian Seismic P.esearcli Institute of
Geolo~y, Geophysics and ttineral Raw Materials of the USSR PZinistry of
Geology], the Siberian Special Design Office of the USS~ Ministry of Geology) -
designed and tested li~htweight, radio-controlled Tayga equipment for ~
recording seismic oscillations during regional studies (see Chapter I-IV)
and converted this equipment to series production.
The basis for the developed procedure is a new approach to the identification -
- of waves recorded on short, senarated sections (discrete correlation).
A joint study was made of various types of waves from the most stable,
extended boundaries in the earth's crust. The wave~ are identified with
respect to a number of attributes based on using kinematic, dynamic
characteristics o� the oscillations and the general laws of the structure
_ of the medium and the velocity distribution.
Observations are bein~ performed on the simplest possible, to a significant
degree arbitrary sounding systems (along the traverses or along the area
network) made up of tt~e source and a short (0, 5--1 km) recording device,
the spacing between which is selected in the region of greatest isolation
of the investi;;ated wave or group of waves considerinp local conditions.
The arbitrariness o~ the observation systems and the use of the developed
remote controlled ec~uipment made it possible to obtain the r.equired density
of the points for determinin~ the parameters of the medium (~the reference
point). �
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Alonp with the hodographs~another .Eorr~ of representation of the kinematic
wave cha~'~3CEP.X'iSL'.'IC3 was used spectal two-d:tmensional and three-dimen-
sional time f,ields. The geometric parameter.~ of: the aeismic boundary and
; the velocity distribution oF the medium are found by the time Lields with
sufficient acci~racy f.or thc reconnaissance phase,
In Chapter V, a new proced ure is c~mpared wiCh the traditional types of
regional seismic research.
The broad production intr.oduction of the performed scientiflc-design
develupments has made it possible to proceed with the planned, deep seismic
studies which are continuing at the present time in the Tdestern Siberian
_ platform with its mountain framework, the Siberian platform and the Baykal
rift zone (see Chapter VT).
The performance of this complex scientific-production ~~or~ on the creation
- of a new procedure and new equinment, their introduction and broad produc-
tion use has turned out to be possible as a result of the close cooperation
of a nuMber of scientific and production rrganizations: IGiG SO AN SSSR,
.IAiE SO AN SSSR, IG YaI' SO AN SSSR [Geolo,y Institute of the Yakut Branch
of the Siberian Department of the USSR Academy of Sciences], SNIIGGiMS MG
- SSSR, the ZapSibNIGNI Institute, the subdivisions of the Tyumen' P~ain
Geology Administration, the Novosibirsk, Tomsk and Yakut Territorial P4ain
Administration, the Eastern Geophysics Trust, the Krasnoyarsknefte~;azrazpedka
Trust, the Siberian Special Design Office of the Scientific-Production
Society of the Soyuzgeofizika of the Ministry of Geology of the USSR.
The successful improvement of the equipment and procedural developments,
broad testing and i~traduction of the new methods into industry have been
promoted by the new scientists and specialists. rirst of all the authors
- are grateful to ~lcademician A. t~. Trofimuk for his constant attention to the
developments on a11 levels and also A. I. Bogdanov, V. V. Ansimov,
N. P. Chunarev, Yu. G. Erv'ye, L. G. Tsibulin, N. N. Grachev, N. G. Rozhek,
V. V. Tkachenko, V. A. Kondrashov, G. Sibgatullin, ri. N. Ptitsyna and
many other comrades. -
V. V. Fedynskiy, Yu. Ye. Nesterikhin, E. E, I'utiadi, M. K. Polshkov,
V. S. Surkov, N. V. Arkhipov, L. I. Orlov, I. D. Panin actively supported
the development of the "Tayga" equipment.
Large collectives of the above-indicated organizations participated in the
` substantiation of the new methods, the design of the equipment, and the
field experiments. r'Iany o~' the snecial;tsts made a noteworthy contribution
i to the development and the procurement of the geological resultst
E. S. Agadzhanov, V. V. A,lekseyeva, G. Anistratov, Xu. F. Barinov,
G. F, Bratova, A. A. Degryarev. V. I~ Belov~ I. I. Babrovnik, D. D. and
I. D. Bondar', Z. A. Bridzinskaya, I. Vayman, V. P. Vasil'yev,
L. Sh. Girshgorn, A. IQ. Gretskiy, D. L. Dryga, L. V. Dubovik, A. I. Dyzhin,
A. V. Yemel'yanov, Yu. G. Zaytsev, V. M, Zamskov, V. Ye. Zakharov,
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A. M. Isaykin, V. A, I:alashnikov, V. N. Kartsenko, 0. N. Klimov,
A. L. lCo~an, A. G, Komlyagin, A. I'. Kolmakov, Yu. G. Konovalov,
A. B. Kreynin, V. V. Krepets, A. L, Krylova, G. V~ Krupskaya, N. M. Levina,
V. G. Leont~yev, G. G. Maslennikova, V, M. Me~erya, Z, R. Mishen'kina,
V. F, Niknshina, V, M. Nosov, M. V~ Pavlov, P. Tf, i'rusova, G. V. Petrik, -
_ V. P. Ileskachev, I. V. Podnarkova, S. V. Potap'yev, R. A. Rakitin,
V. G, Rodikovs A. G, l~yasik, A. S. Sal~nilco~, A. S. Samoylovich,
V. S. Seleznev, M, D. Sergeyev, T. G. Smirnova, M. Z. Sniper, S. K. Sulkovskiy,
R. K. Taipov, L. I.. Trusov, F. ?~t. Trusova, V~ F. Uarov, T. N. ICholodnyakova,
Pi. F. Chernylch, Ye. S. Shlyakhter, A. S. Shtifanov, Yu. A. Shcherbakov,
A. M. Yakimov, t1. T. `ianiye, T. A. Yanushevich.
. The authors of the individual chapters of this paper ara as follows:
Chapter I-- N. N. Puzyrev, S. V. ICrylov, B. N. Tiishen'kin, V. D. Suvorov,
A. I. Bochanov, G, V. Yegorov, I. S. Chichinin; Chapter II
N. N. Puzyrev, S. V. Krylov, B. P. Mishen'kin, V. B. Suvorov, V. K. t~ionastyrev;
Chapter III A. I. Bochanov, G. V. Yegorov, I. S. Chichinin; Chapter IV
N. N. Puzyrev, S. V. ICrylov, V. L. Kuznetsov, B. P. Mishen'kin,
V. K. Monastyrev, A. L. RudMitskiy, V. D. Suvorov; Chapter V--
N. TI. Puzyrev, S. V. t~rylov, B. P. Mishen'kin, V. K. Monastyrev,
A. L. Rudnitskiy, V. D. Suvorov; Chapter VI N. N. Puzyrev, G. D. Babayan,
S. V. Krylov, V. L. I:uznetsov, M. Pi. Piandel~baum, B. P. Mishen'kin,
V. K. Monastyrev, A. L. Rudnitski_y, V. D. Sitvorov.
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CHAPTER I. REQUIP.IIYIENTS ON REGIONAL SEISMIC RESF.ARC~I
�1. Subject, Goals and Characteristic Features of the Regional Seismic
Research Method
The m~st important goal of research is discovery of the reoional strlscture
and density of the depths to establish the relations of the surface
geological features controlling the mineral deposits accessible for
extraction to the structure of the subsurface zones of the earth's crust
and th~e .tops of the mantle.
The regional seismic studies constitute part of a complex of subsurface
geophysics techniques. The seismic method must provide reference data for
interpretation of the gravitational, magnetic and other natural physical
_ field anomalies. By these anomalies the discovered subsurface stru~tural
features can be sv.pplemented and extended to territories which are~ad~acent
to the seismie ope,ration zones. -
At the present time there are r.umerous geological-geophysical facts and ~
ideas about the model of the earth's crust which must serve as the basis
for determining the characteristic features of the subsurface structure
- accessible to express investigation by the seismic method.
It is obvous that in the prospecting work the seismic method must isolate
sufficiently large-scale structural features of the earth's crust and the
tops of the mantle important to the understanding of. the deep nature of the
regional geological structures and the large-scale anomalies of the
natural geophysical fields. The specific problems and ob~ects of investiga-
tion are varied. Indisputably, it is necessary to consj.der that these
include a comparative subsurface study of the platforms (young and o1d),
the folded regions of various ages and the reg3ons of tectonic activity (the
r.ift zones, the re~ions of modern vulcanism). Nowever, wh~must not limit
ourselves to the study a~ these very Iar~e f eatures as a whole contain:Cng _
internal inhomogeneit3.es o~ different order. In order to estimate the
possibility~for the discovery of these inhomogeneities on the prospecting
level, let us consider the geological data on the denuded regions and some
of the results of deep seismic studies.
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Let ~is use the ^?arerials from the tectonic re~ionalization of Siberia
and the ~ar East by structural and formational attributes [22], lir~iting
ourselves to ihe data pertaining to folded complexes, that is, the geologi-
cal bodies o~hich form the consolidated czust. The basic (largest) structures
of the folded cemplexes are the geosynclinal troughl~, the peoanticlinal
uplif ts, the oro~enic type tr.oughs and msny others. These structures are
distingu~.shed with respect to internal structures and rock composition, and
as a rule, they are bounded by large fractures. Statistical data are pre-
sented in I'ig 1 on tile horizontal dimensions of more than 60 such structures. -
The exL-ended structures with a ratio of the axial lengths of 3 to 5 pre-
dominate. The dimensions along the ~ong axis reach 800 km or more; the
' predominant values do not exceed 60U lan. The width of the structures
reaches 300 km with predominance of values near 100 lan.
t1~KA< ~si a b~
400 -
[0~ e � i . ~iro ~
~ ~ � ~ �
� ~
' . � � ~
r
~ ~
P, 96 ~
~0 ~ �
~ Q .
f 0 ?~6f
c
0 ,
EJO 4L'~J GGD 6?D f000 l200 1~00 qxAt.
rigure 1. Characteristics of the horizontal dimensions of
regional geological struetures of the folded
complexes of Siberia and the Far East.
a-- ratio of the width (b) and length (c) of the structures;
b-- hj.stograms of the width and length of the structures
With respect to size, the investigated geological structures are similar to
the outlines of the regional anomalies of the magnetic and gravitational
fields [5]. Therefore the orientation of the prospecting seismic research
for the discovery of the subsurface features on this scale is important not
only f or regional geolo~y, but also for other neophysical r.iethods of study- -
ing the earth's crust.
By the results of the detail~d subsurface seismic studies, the actual dis-
tribution of the elastic pxoperties of the earth's crust and upper parts
of the mantle at the present time is approximated by a nonuniform layered-
block model [43]. The layering is exhitiited in the existence of almost '
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horizontal, slightly ~aavy boundaries separatin~; the medium into a number �
_ of layers with different elastic wave velocities, The ~locking is
expressed in the fact that over. extended (up to several hundreds of
kilometers) sections of tl~e pro�t.les of the deptl~s of occurrence ot the -
_ seismic boundaries, tI1G tt~ickness of the. earth's crust, its fractured
dismemberment vertically, the thickness of the individual layers and the
elastic wave vel~~cities vary little. The articulation of the sections with
respect to the sustained structure usually take plrice along narrow steeply
dipping zones where all or the majority of the mentioned para_meters ctiange
- sharply. These anoMalous zones frequently are exhibited to the tors of
the mantle, and they are considered as abyssal fractures delimitin~ the
crust-mantle blocks. The discussed peculiarities characterize the macro-
inhomogeneity of the deep interior. Sufficiently detailed seismi.c studies
have establish,ed more br.oken blockin~ out of the earth's crust, cliscontinuity ~
oL the gentl.y sl.opin~ sei::mic divisions, comple:c structure of them in the
vertical cross section, t11e existence of. short, sharply inclined t~oundaries
and diffracting features. _
Gently sloping seismic boundaries in many cases do not agree with the
geological concepts of the structure of the crvstalline crust, espec3.ally
its upner ;~art [1!+, 45]. However, the tracing of. thase boundaries, with
procur.ement of the datn on the velocity distrihuti.on of the el.ast~.c waves,
permiCs su~f.iciently reliable isolacion of the larpe blocks of the ear.th's
- crusts and the abyssal fracture zones. The blockin~ out of the crust
accordin~ Lo the seismic data, as a rule, is in good a�,reement witl~ the
. p,eological data on the structure of the upper part of the sectiot~. I?xamples
, oE this a,s*,reement are known in practice in alI exposed ar.eas. The ].aroe
;;eol.o~ical structures frequently aPpear. in the entire thickness of the
- ea?-tli's crust in the form of individualized blocl~:s established by deep
seismic studies.
The local peculiarities of the medium (frequent discontinuity of the
boundaries, smal.l inc].ineci surfaces, diffracting featur.es) obviotisly cannot
be studied during reconnaissance prospecting. The deep boundaries must be
investigated under the assumntion oL their being sustained over large
ter.ritories, but even in a rough approximation ti~is is not v~lid for all
seismic divisions. The most stable ref.erenceboundaries are the surface
of. the mantle (the Mohorovicic discontinuity M) and the upper Uoundary
of the consolidated crust correspondin; to the surface of the crystalline
(folded) basement in the p.latforms. These tcoo boundaries must be studied
in the reconnaissance prospect-ing phase. The intermer]iate intracrustal
seismic discuntinuities can be reliably investip,ated only under favorable
condirions,, for even when using the continuous prof.iling procedure, they
have discontinuities ancl cannot always be identif.ied in the near sections
[43]. Nevertheless, during the reconnaissance operations the possibility
of studying the sharpest boundaries inside the crys~alline crust must be
pr.ovided for.
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It is extremely imPur*ant to emphasize the insufficiency of st~idying only
the morphology of the reference seismic boundaries. This arises, in
parti.cular, f.rom the already--mentioned correspondence of the gently s'loping
seismic stratification of the earth~s crust to the geological data from -
which it follows tllat the confi~uration of the extended boundaries far ~
Erom exhausts alI of the characteristics of the complex structure of the _
investigated medium. In addition, there are a nuMber of examples where the
~ravitational anoma.lies ~ohich are sufficiently lar~e with respect to hori-
zontal dimensions and intensity cannot be explained by the slightly wav}= -
srratiEi.c~tion of the material of the earth's crust alone. Accoruingly,
in the reconnaissance prospectin~; phase, alon; with the morphology of the
bounciaries it is neces~ary to study the larf,e-scale velocity distribution
features (mean, hounciary, stratal) along the traverses and with respect to
area. -
The inEormatian about the variation of the elastic wave velocities is no
less important than the geometric characteristics. It is inadmissible to
iise constant values oF the velocity carried over from other re~ions. The
- information about the velocity clistribution of the elastic oscillations in
the reryions of modern tectonic activity with inhoriogeneities of the elastic
pr.operties of the rock of the earth's crust and the top of the Mantle -
imnortant to subsequent analysis and, along with the electrometric and
geothermal data indicating the possible anomalous state of the subsurface '
material is especially valiiable. The information about the limiting velocity
dist.r.ibution when studying the basement surface of the platforms and the
- boundaries in the upper part of the consolidated crust is also important.
Consequently, the reconnaissance prospecting seismic studies of the earth's
crust must be distinguished from the detailed stiidies not by the nature
(composition) of the infor?na.tion obtained, but only the scale of the
investigated inhomogeneities and the accuracy of. determining the parameters
respectively.
- The importance of the information about the velocity distribution of the
elastic waves will be illustrated in two c}iaracteristic examples of
reconnaissance prospecting seismic operat~ons in the Siberian areas.
The first example pertains to the study of the basement in the southern part
of the Western Siberian platform. In the upper part of the crust two
refracting boundaries are isolated (Fig 2, b): the P boundary correspondinb
approximately to the basement surface of the platform cover, and the lower-
lying I boundary which is discontinuous. The boundary velocity over the
F surface (Fig 2, a) changes sharply in the 5.3-6.2 km/sec range. The
reduced values of the velocity (5.3-5,7 lan/sec) are coordinated with the
sec~ions of exist~nce of the T boundary. GTherever the latter boundary does
not exist, the velocity on the surface increases sharply to 6.1-6.2 km/sec.
The joint investigation of the data on the velocities and the cor~�inuration
of the seismic boizndarie~ leads to the conclusion of the block-fractured
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structure of the basement and the pr.obable ~eolo~ical meaning oE the _
seismic boundaries and layers. The blocks with hi.~;h velocitv at the F
- bounclary ohviously correspond to the folded (Reosynclinal) complex of
_ basement rock, In the blocks with reduced velocity the tops of the Uase- -
ment (the layer between the F and T boundaries) probably are made up of
an intermediate com~lex oE rock with a relatively low de~ree of ineta-
morphism; The geosvnclinal formations run under the I boundary. This
~eological-geophysical analysis oE the seismic data obviously would be
- impossiUle without information about tlle elastic ;oave velocity distribution.
_ u
f,rwic (1 ~
c
a6 - -
r p -
~ ~ 5 1 r^~ ~ _ -
~
� >.,p
~ Ci
~ ~ �u~ xw
_ , S ~2) r
p 1GJ ~~0 3~? dOG 5i,0 ~ 60tJ
0 - - -k~-- ---1--
- 2 y, J~ ~ ~ '
_4 L~=..~4-F~UV.~~'~T~ L.%L'.:.~_~+U~ J~.3_{~~~- Fi~-~-
4/
6 r ~ / .
' ,ti V ~'y ~,3�~5
s yE' / ~-~-~1_ -~-i:� ,ti�-
L~ L.3-.;,d ~ i: lir~~3-G,S h. ',f ~�:,2-Gfi
_ ~O ~ tiS
~ `M ~ 1 ~ 2 ~ 3
riaure 2. Seismic traverse of ttie cities of Ishim to
Larabinsk (Western Siberia) [114]
a-- grapl~ of the boundarv velocity over the Uasement surf.ace -
(F); b-- seismic section; 1-- seismic boundaries; 2-- fracture =
zones; 3 deep wells =
Key:
1. vboundary-~~sec
2. Ishim
3. Barabinsk
As another example let us consider the results of studyin~ the surface of
~ the mantle in the vicinity of Lake Baykal by two procedures: spot seismic
sounding [55] and the seismological method of transmitted composite waves
_ [106, 133]. The second procedure does not give information on the elastic
wave velocities. In the sections obtained by closely arranged traverses,
- the transition from the Siber~,an platform to the highly active Baykal rift
zone, according to the data of both proceclures, is not accompanied by '
_ contrast changes in the r~orphology of the ~t boundary. Actually only the
data on the reduction in the boundary velocity on the Tt surface to
- 7.7-7.8 lan/sec indicates the anomalous properties of the tops of tt~e mantle
in the rifto~enesis zone, This highly valuabl.e inf.ormation was lost during
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the seismolop,ical studies oriented in the given case only to the study of
the conf.igurati~n o� the medium.
Let us discuss some �eneral requirements on the nrocedure for deep seisr~ic
studies oP the reconnaissance prospecting phase,
It was demonsrrate~i above that obtaining full~valued information about the
deep structure containing data not only on the mornholog~� of the reference
- seismic boundaries, but also the velocity distribution in the medium, it _
is possible in the majority of cases only for the joint use of the waves ~
of. various types. The orientation of the seisr.?ic studies to recording waves
of any one type (For example, composite caaves in the first arrival),
although it creatc~ deFiiled conveniences ~ahen per{ormin~ the operations,
usually leads to insufFiciently comolete inforr~ation and even low reliability ~
of the inf.ormation about the r~ediuM period.
~ a Q P,~
0 80 ~
`g'1'o Rh 60 2 x
3 -
40
\ ~ 20
~r+�.~,-,:~ \x ~
270� 90� 0 '
~ ~p g ~0 70 50 30 f0 a�
I'i~;ure 3. Substantiation of the seismic studies of the
block structure of the earth's crust
- a-- strike rose of the lars~e faults of the Altaye-Sayansi;aya
Oblast and I:azakhstan; b-- histo~rar~s of the angles between
the fractures and the rectilinear traverses of different
length (curves 1-3 correspond to traverses 300, 600 and 1?_00 km
long)
Ttie ,joint use of waves of dif.ferent types must be one of the basic principles
of the method of- reconnaissance nrosnecting seisr.?ic research. The presence
oE data on a number of waves even in the case of relatively low-cletail
observations permits reliable identif ication of the ~oaves, more correct
selection of the model of the medium and control of the results of. determinin~
its narameters. All this will promote an increase in tl~e completeness anu
reliability of the infar~?ation obtained without significant complication
of the seismic observations themselves.
. The problem of how to perform the reconnaissance pros~ectin~ study of the
deep continuation of the regional near-surface ;eolo~;ical structures
with respect to the e~:tended rectilinear nrofiles or by the area-wide
observation network is important. It is known that the fractures and,
consequently, the ~eological structures bounded by them, are orouped with
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~~ith respect to the strike directions into ~our orthogonal and dia~;onal.
- systems. This phenomenon is :Cllustrated by the strike rose o~ the large
fractuxes of the Altaye~Sayanskaya Oblast and ICnzalchstan (~i~; 3, a)
compiled by the tectonic map o~ Furasia (editor A, L, i'anshin, 1966). _
Accordingly~ the extended rectilinear traverses, even ~~ith optimal orienea-
- tton o~ them, in many cases cannot run acroas the strike o.f. the ma:~ority
of intersectin~; AtructureA. Thus, ~inder the condit~.ona of, rhe Al~r~ye-
Sayanskaya Oblast and ICazakhstan, it is possible to intersect the re~ional
structures almost at a ri~ht angle to the strike only by limitin~ the
extent of the seismic pro�iles to the first hundreds of kilometers (Fig 3, b).
The traverses about 1000 km long intersect the boundaries of the structures
at predominant an~les from 40 to 90�. All of tlie values of. the angles in
this range are almost equinrobable.
Consequently, the nrofile observations are not always advantageous: a~sj.o-
nificant part of the investigated structures will intersect almost along the
strike; which decreases the information obtained per unit length of the
profile ancl can cause difficulties when interpreting the ~aave field as a
result of different types of side effects. It is exPedient to combine the
profile studies witti the area studies.
The solution of the nroblem of the density of the networlc of seismic observa-
tions durin~ the reconnaissance prospecting caork depends to a~reat extent
on the peculiarities of the specific seismic procedure the method of.
identif.ication and type of waves used, the methods and accuracy of determining
the parameters of the medium, and so on. These peculiarities will be investi-
gated in Chapter IV, and here we shall consider that each single determina-
tion of the parameters of the medium (velocities, c~epths) is absolutely
~ accurate, and the distortions of the shape of the relief of the sPismic
boundaries h(x) an~ the graphs of the velocities along the profile..v(x)
are caused by the discrete nature of the location at the points of determina-
tion of the parameters of the medium (the reference points). Under these
conditions, it is possible to obtain an estimate of the maximum distance
axp between the reference points, which must not be exceeded in order to
avoid undesirable distortions of the results.
a From information theory (the Kotel'nilcov theorem or the reference theorem
[127, 129J) it is known that the funceion y(x) (in our case the funetion
of the variation in depths or velocities alon~ the mixed profile) with
respect to its discrete values followinQ through the t1x~ interval, cannot
be exactly recreated, for its spectral components are lost at .frequencies
- above wp=n/~x~. The least value o~ the relative mean square errur in the
~ r~creation of the function y(x) is~
i
-~a ~
J ~ S(co) ~~dw ~ ~ S(w) ~2dco'
mi?i
_ ~,~a ~r.~>
p ~ ,
2n J' ~x, dx
_ .
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where y is the r.?ean squaxe eXxox ~.n recXeation o� the ~unction y(x);
p.is the mean s~uare value o� this'~unction~ S(w) is ~.ts spectrum.
In order to use the presented relation, it ia necessary to be �iven the
- f.orm as a function y(x), that is, h(x) and v(x). ~ror~ the seismic opera-
tions experience (characterj:stic examples with reepect to the Siherian
areas are presented in Chapter V) it follows that the relie.f of the deen
seismic boundaries obviously is primarily caused bv the fracture-block
- structure of the earth's crust. The function h(x) usually has a step form;
_ smooth variations of the de~ths are noted. Stati_stical data are presented
in Fig for i~lestern Siberia about the horizontal dimensions of the step
and amplitudes of the discontinuities and their boundaries for the
t4ohorovicic surface and th~ hig,h~r-lying I boundary. The actual velacity
distribution along the seismic boundarie~ vboundary~x) also can be
approximated by step functions. This type of ~;raph vboundary~x) is apparently
connected :�~ith the block structure of the crust, and in the case of the
baser~ent surface (I'i~ 5) also with the erosion of the complex folded rock
penetrat~c~ by intrusions. The norizontal distribution of the mean (ef.fective)
and mean interval velocities, which are the integral parameters of the medium, ~
must be appraxi.mated not b;T step function, but by smooth functions containing
anomalies with approx.imately the sa~e horizontal dimensions as the corresnond-
ing blocks of the earth's crust.
- a
g~
~ ~ to ,
FO
40 12U Q00 280~,~tac 0 2~ 9 10ah,KM
~
P~
~10 . .
QD
~00 400 000 q,x,K 0 �1 8 ~ 1P e h, K,u
Fis;ure 4. HistoUrams of the hor~zontal ef~ect b and the ~
aMnlitudes 6h of the steps in the relief o� the
seisnic boundaries T(a) and P'I (b) by the results
of the deeu seismic soundings in GTestern Siberia ~ '
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P~916 -
40
20
~
0 40 ~~0 9P0 f00 e,KM 0 q4 ~,8 1,2eury~~
Fi~ure 5. Histograms o� the horizantal dimensions b and ampli-
tudes ~vboundary the step anomalies in thA
distribution oP the boundary velocity over the
basement surface of the ~]estern Siberian platform
' (by the spot seismic sounding data)
For approximation of single anomalies o.f the depths and the velocities, let
us talce the following simple functions:
a~or' Z ~x~�- i ,
yi ~x) = for b b (I.2)
0, 2>x>z
and .
_ ~ in too~,. (I.3~
?Jz~x) = ae b~
The first function (square pulse, Fig 6) simulates the denth variation of
the parameters reflectinc the block structure of the medium. The second
function, called a bell function, permits tnvestigation of the continuous
distribution of the parameters. Its width (b) is provisionally taken at ~
the O.Ola level (Fi~ 6, b)
- As a result of the substitution of the functions yl and y2 in the expression
for min ~y/p and the mathematical transformationsl we obtain the desired
- expression. For a square pulse
b 1
i-cosri- - 2
minY_ 1+2 2 6 ~x~-nSiCn~) . (I.4)
P a
~ ~xa '
i
1For the bell function these transPormations are presented in Chapter IV,
~1.
.
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Lor the bell .funct~on
L
min n _ ~ (I.5)
.
P V-- [1 -~U (2 y21n llw ~ Oxo
u u
Here Si (u) 91~ clt, ~(u) = n` e-~=d~ is the integral sign and the
0 0
- Laplace function.
During reconnaissance prospecting in the majority of cases it is possible to _
consider it admissible to have relative distortions of the structural forms
and velocity anomalies up to 25%. By the graphs o.f m~nY( b~l
~ ~r )
in Fio 7 we find that this condition wi11 be satisfied if the distance Ox~
betcaeen the reference points does not exceed one quarter (for the step
anoma.lies) and one third (for the smooth forms) of the width b of the
investi~ated objects. Assuming, in accordance with the results of the
precedin; analysis, for the deep parts of the earth's crust that b=100 km,
we obtain ~x~,25-30 km. blhen studying the upper part of the earth's crust
where a ~reat deal of detail in the results is necessary, clustering of the
points of determination of the Parameters of the ~edium can be used. In
this case taking the width of the discovered anomalies at b=30 ltm (see Fig 5), _
we obtain OxoF7.5-10 km.
~
. p � f
z t Qp
~ 2 2
40 ,
~ 20 .
-~r ~ ~ 2 3 4 5 8 7 8 ~
ex
I'igure 6. Rectangular (1) and bell k'igure 7, Minimum relative errors
(2) nulses in the recreation of the square (1)
and bell (2) pulses b}* discrete
- measurements
Thus, it is possible to formulate the sub~ect and the Qroblems o� the deep
seismic studies of the reconnaissance prospectir.; ~hase in the following
way: the discovery of the large (about 100 km or more across~ blocks o�
the earth's crust and the ~racture zones senaratin~; them in order to dis-
_ cover the deep nature of the re~ional geological structures and the cor~respond-
ing anomalies of the natural geophysical fields; the mandatory study of the
foot, the roof of the c~nsolidated crust and the basic peculiarities of. the
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velocity distribution o.f the elastic waves ~n the medium. Tl-~e e�Fective
procedure for reconnaissance Qzospectin~ seismic research miist be based on
the ~o~.nt use ~f waves o� various types durin~ area and traverse observa-
tions with determination of the parameters o� tlle medium no more rurely
than every 25-30 lun, and ~ahen studyin~ the un;~er nart of the crust, every
7.5 to 10 km.
Let us more specifically define these general re~uirements as applied to
the study of the basement of the platform regions where recently new Roals
have been set for the re~ional seismic studies connected with estimation ~
of the prospects of the oil-bearing nature of wealcly metamorphic sedimentary
rock belonging to the upper level of the basement. TThen solvin~ these prob-
lems obviously it is impossible to limit ourselves to 5tudying the surface
of the basement. The deepness of the studies r~ust not be less than the -
denths to the foot of the upner structural phase of the Uasement, the tinick- -
ness of which can be 5 to 10 km. As a result of the three-dimensional
nature of the investigated layered-block structure of the basement the
work must be of predominantly an area nature with tracing in the plan view
of the fractures separating the lar~e (several tens of lcilometers across)
blocks of various tynes. Along with the data on the confi~uration of the
boundaries, the information about the spatial distribution of the velocity
in the medium bearin~ information about the acttial composition of the rock
has primary significance.
, �2. Existing Deep Seismic Research Method
The corresponding nrocedural problems have been discussed in detail in
references [43, 14~3, and so on]. Let us briefly consider the state o~E the
art with respect to the problem, primarily in connection with the problem
of reconnaissance research.
Predominantly nrofile observations are being used which are divided into
continuous, piececoise continuous (the dashed lines) and spot (the dotted
lines) observations. This senaration does not apply to the observation
systems alone. The working models of the medium, the procedures for wave
_ identificationy the interpretation procedures, the completeness and detail
of the results obtained are also distin~uished.
Continuous profilinp (Fig 8, a) has become the most widespread in the USSR;
no less than 90% of all o~ the DSS pro~iles on the dry land were investi-
~ated by this procedure. The observation systems are calculated for simul-
taneous recording basically on the z--component of the reflected (usually
critical and transcritical), refracted ~ne~d waves, re�racted waves) and
other types of waves for a suf�iciently detailed stuciy of a section of the
entire consolidated crust, and in individual cases, the upper part of the -
mantle itsel~. As a ru1e, a longitud~nal profile a.s used witfi a spacing
' between the groups of seismographs of 100 to 200 meters and several ident3cal
multichannel seismic stations. The lengths of the hodograph~ reached
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a
0 ~0 100 f50 200 250 300 ~ -
~
\ /
0 150 300K~t
~ C
�
I � � o -
� � � �
� � � �
�
I � � � �
� � �
t � � � ~ �
0 50 x,u ' -
Figure 8. Diagrams of seismic observations
Profiling: a-- continuous; b-- piece~vise continuous;
c spot
250-350 lan (500-600 km when studyin~ the boundaries inside the mantle).
The `spacin~ between the explosion points when studying the deep boundaries
will on the average be 50 to 70 km, and sometimes to 100 km. In order to
investigate the upper part of the section, a denser network of oscillation
sour'ces is given. ~'he systems of overlapping and counter hodographs will
permit continuous correlation of the waves over extended sections of the
profile, the application of quite strict interpretation methods for
determination of the configuration of the boundaries and the velocity dis- ~
tribution in the medium. The continuous profiling (longitudinal and non-
longitudinal) with detailed breakdown of the section of the earth's crust
with respect to elastic properties is especially effective for detection
and tracin~ of the faults and other irre~ularities. Detailed continuous
observati~ns are also needed to discover the nature of the recorded deep .
waves. The�deep seismic bounding operations by the method of continuous
profiling frequently are combined with seismic exploration of the sedimentary
series cahich essentially increases the reliability and value of the data
obtained. The operations by the rePlected wave method with recording by
the common depths noint~method for investiQation o~ intracrustal boundaries
have great theoretical si~nificance.
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As a result of the deep seismi.c research with respect to dense cont~.nuous
observations sytems in the USSR, broad in~ormation has benn obtained on
the pecul3ar~.ties of the recorded wave fields, the layered--hlock structure
o~ the earth's crust under various geologir_al conditions, the velocity ~
, distributi.on laws, the fine structure oE the crust, the se-[5m~c ~notnaJ i.c~s -
li~ ri~t~ tll~yHHtII frn~�r~n�~~ zc~n~r+ i~ncl c~L�li~r ~if~cullr~ri.ki.c~r~. 'I'I~~~fi~~ r~~r~uilri~ fn
c~clcl itlon t:o l-he i r p,eneral e+c LentiClc q-ipni.f~tcance, const.ttute a basi.:+ Lor
i'urther improvement of the deep seismic sonnding method, including in
connection with the problems of operations in the reconnaissance prospecting
phase. It must be noted that the operations with respect to the continuous
profiling with the blast points separated from each other (`by more than -
250 to 300 lan with approximately the same lengths of the hodograptis; must
be considered in the cate~ory of reconnaissance prospectin~ procedures by the
nature of the information obtained on the deen structure and the reliability
of determining the parameters of the medium.
. Piecewise-continuous profiling (Fig 8, b) differs from continuous prof ilin~
by the presence of omissions in the seismograph installations with respect
to profile and si~nificantly less dense arran~ement of the sources. In the
USSP, this type of observation was used in the initial phase of development
of the deep seismic sounding method. Now it is used to a sma11 extent in
the inaccessible parts of Siberia for the so-called parametric sounding for -
preliminary study of the basic characteristics of the wave picture.
Piecewise profilin~ is the basic type uf observation on the dry land when
studying abroad. The short (no more than a fe~v kilometers) seismograph
installations are placed with significant (10 km or more) breaks along
rectilinear nrofiles, beginning r~:ith the source of the observations Co
distances of about 300 lan. Sometimes the extent of the hodographs obtajned -
reaches 600 km. Often several dozen recording stations are used simultaneously.
As a rule, the blast points are located no closer than 100 to 200 km to
each other. Systems of single or counter hodographs are used, the extent of
which is selected countin~ on obtaining recordings of the r.efracted wave _
from the M boundary in th~ first arrival.
The area systems of rectilinear profiles r.adiatin~ from one common oscilla-
tion source have found application in the United States and Western Europe.
As a result oF incompleteness of the investigated observation systems usually
it is possible reliably to trace only the refracted waves re~orded in ~he
first arrivals over extended intervals of the profile, The use of the
following waves, especially if they do,not ~orm sufficiently extensive
hodographs,~is complicated. i~Jhen interpreting the data ~requently studies -
are made of single hodo~raphs without relatin~ them, which forces simpl~fica- -
tion of the model of the medium, reducin~ it to a layered model with plane
horizontal boundaries and constant velocities, As a result, in spite of
the relatively high density of the seismic observations, the distances
between the reference points of determination of the paraneters of the
, medium turned out to be appreciably Iarger than the limitir~g values which `
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were substantiated above be~inning with the conditions of reliable discovery -
" of. the investigated ob~ects. The horizontal nonuniformities, the block
_ nature of the crust, and the deep fzactuxe zones, as a ru1e, do not find
- reflection in the resultant conetructions. iJsually hi~rhly reliable data ~
are abtained on tt~e tl~lckness of the crust and the boundary velocities at
its foot. The intracrustal boundaries are determined with less reliability
and they are not obtained zvery-~ahere,
It was possible to achieve a reliable separation of individual deen waves
in the subsequent arrivals during piece profiling by recording them in
specially selected intervals from the source. As an example, we can use
, the work of the Hun~arian geophysicists for studying the M boundary by
reflected waves recorded near the initial point [140]. In the Federal
Republic of Germany, piecewise profiling systems are used which have been
designed for tracin~ the waves reflect2d from the same part of the boundary
for various blast-reception distances [142].
Spot profiling (see Fig 8, c) is used predo~inantly for marine investigations
in the mobile blast version [32, 111]: stationary seismic stations on
ships, buoys, bottom seismographs recording waves from the blasts moving
along the profile line are used. The spot observations on dry land conducted
abroad differ froM the Piece profiling by the apnlication of one or several
seismoc;raphs (frequently multicomponent seismograph) located at one point or
in a very small space instead of the quite extensive recording devices.
Seismological receivin~ equipmeat is ~ften used in this case. At the
present time such systems have become quite widespread for the recording of
waves at great distances from the source (~1000 km or more). -
The continuous profiling nrocedure permittin~ us to obtain more exact and
reliable data on the deep structure obviously cannot be used in the
reconnaissance prospecting phase of the operations as a result of its .
complexity, its great consumption and impossibility of performing continuous
observations in inaccessiblP areas in large volume. The low-detail operations
are nerformed on the continents (actually only abroad) using piecewise and
spot profiling. The simplicity and the relativelv small amount of labor
involved in the observation systems characteristic of these procedures have
been obtained within the framework of the traditional approach based on
usirg the hodographs. The rarefaction of the observation network complicates
identification of the waves, causing significant schematization of the
models of the medium. As a result, the above-f.ormulated problems of '
reconnaissance prosnectin~ deen seisu~ic studies during piecewise-continuous
and spot observations are not always solv~~d with sufficient co~rpleteness
and reliability. In addition, in these methods it is necessary to perform
operations with respect to su~Piciently ex;tended rectilinear~prof iles,
wh3,ch is far from always possible under conditions of inaccessible terrain
and also in densely populated areas.
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In the method of seismic sounding nroposed below wliich is inrencled for the
performance of the operations of, the reconnaissance nrosrect3ng pl~ase, an -
effort was m~de to surmount the indicated dif.f.iculties based on broad
~nformat~on abotit the wave field and ~he ~truclur.e oC the meditim ohtn~.ned -
as a result of. detailed operrttions hv tne continuous prof i].:Lng mcthod.
; ~3. Requirements on the rq_uipment f.or Reccnnlissance I'ro~;pectin~; Seismic
, Research
- 4Jhen performing reconnaissance prospecting studies by the deep seismic
sounding method, the seismic waves.are excited by blasting with ~o~Jerful
charges of from 2 to 4 tons, for the seismic waves are recorded >iethod ['138] are pre~sented
in Table 1. ~
From the table it follows that with a 12~uo1t intake the autonomous operating
_ reserve of the "Zemlya" and "Cherepakha" recorders of 10 days is insured
by 12-volt power packs ~~ith a capacity of 300 amp~tiours (under the condition
_ that 80i' of the initial storage capac~.ty will be used). This type o�
power pack can be arranged by us3.ng six NIaI-100 batteries with a total
weight of ~00 kg. AS a result~ taking into account the remaining�.ectuipment
� of the observation station (the seismographs, seismic cradle, and so on)
which is widely used in the geological service, can transport the eguipment
for only two observation stations at a time, Already with resgect to
this paramQter alone, the indicated equiQment cannot satisfy the require- _
ments placed on the deep seismic sounding operations in inaccessible ~..=eas,

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r~~i~ ~~t~r~r.c;rni, ~ist~, c~cvi,v
for the time required to equip 10 observation stations runs into several
days dtiring which the recorders w~.ll operate at idle.
_ The recoder of the "P4ars--66" equipment which best satisfies the basic
requirements, has two def.iciencies; it only has three seismic recording _
channels and 3 short a~itonomous operating reserve (about 1 hour) requiring
the pr~sence oE a dutyo uPerator at the observation station to switch an
the r~corder dj.rectly before the blast and switch it off after making the
recor.ding. It must be noted that it includes a radio receiver which
receives the time marlc signals over a long wave or short wave radio channel.
The time marks have the follow3ng structure at the receiver output: second
marks are representecl by single pulses of 0.1 second duration and an ~mpli-
- tude of 8 vol.ts; mint~te ~arlcs are made by double pulses of the same type
and the hour marlcs, hy triple pulses. For the Ionger time marlcs the
recorder has a ~uartz-stabilized oscillator, the signal from which is
recorded by one of the service channels. The second service channel is
used to record the time marks received by radio.
In the USS:; an effort has been made to use raciio telemetric equipment to
build e~uipment for the deep seismic scunding method [34, 35]. This equip-
ment was created at the Larth Physics Institute of the USSR Academy of
Sciences. One set of it includes seven portable field units, each of
which transmit information from three seismic channels, and the central
recerding station with a 21-channel recorder. ?:owever, this equipment has
not found broad aPplication in the deep seismic sounding method as a result
of limited ran~e (20 km) usin~ the ultrashort wave radio channel. The other
radio wave bands do not insure the required carryin~ canacity of the radio
telemetric channel; therefore the applicatiorL of radio telemetry and the
equipment for deen seismic sounding is not prospective.
An American patent is known [143], proposing a procedure and a device for
recording the seismic sinnals by radio~controlled distributed single-channel
magnetic recorders. The system includes a radio transmitter which transmits
commands to the blast point and to the recorders. The radio receiver at the
blast point s~arts the reel-to-reel magnetic recorder, which records the
time signals transmitter on one channel, and on the other, the si~nal from
the seismic receiver installed at the blast point.
The radio receivers with which each recorder is equipped, switch the recorders
on. Then si~nals from the seismic receiver are recorded on one~channel,
and the time si~nals on the other. The successive blasts are recorded
: one after the other alon~ the length of the magnetic tape. The field
recordin~s on the base device are copied alternately on another ma~netic
carrier on a drum insuring match~ng with respect to the blast times or other ~
marks, correction of the speed of the field tanes and suppression of the
noise caused by nonuni~'ormity o~ movement of the magnetic tape~. ~
All of this is prir.iarily designed for the construction of a seismic explora-
tion station without seismic cradle, that is, each seismic channel must
be autonomous, it must have a radio receiver, decoder. and tape drive _
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tnechnnism. l~rom the l~o:int o~ view o:f: ~Pie requlrc~ments on tl~~ dee~ seism:Lc
sounding ec~uipmentt this solution is ~.ne~f.icient, �or the cosl- o.E L-l~e
equi.pment and Lhe total mass calculated f,o~~ onc seismic recordin~; ch~nne.l
are increased.
It must also 6e noted tl~at the autonomity o� each seismic ct~annel l~ads l-o
_ the hi~;hXy labor-consuming subsequent operat:ton of. reprodtiction.
_ In addition, the proposed re~tote control Aystem cai11 have i.n~ufFicienC -
noiseproofness inasmuch as it is proposed tt~at one attr:tbute the presence
of a signal of- defined 1:rec~i~ency at the output of the r~.dio recciver be
used to switch on the recorder. The f:urther experience in the clevelopment,
operation and maintenance of rad-Lo remote controlled ec~uipment 11as shown
that such simple measures are inadequate to insure the reqrxl.recl noiseproof-
ness.
Thus, the analysis of Soviet and forei~n equipmeiit for similar purposes
indicates that the enumerated requirements will be most completely met l~y
- radio remotely controlled autonomous seismic recording equipntent with
magnetic recording (see the description in Chapter TTI),
I
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I~'U~t u~~'I~'IC.[n~~ 1~51: uNt,v
CHAPT~R II. TIiEORY OF SEISMIC SOUNDING
As has already been noted, seismic sound3ngs to study inaccessible parts
of Siberia have been develoned in two versions. In the first of them,
which initially arose as a simplification of observations by the refracted
wave method (P~V), a study is made of the refracted waves 3n linear and
spot soundings. This version [79, 80] has found application in studying
the basement of the I�Jestern Siberian platform in the Tyumen' Oblast. Another
version called the method of arbitrary spot (differential) sounding systems
[98] is based on reflected and refracted waves using special time fields
for internretation. It is used both when studying the basement of the _
plaC�orm regions and the entire earth's crust and tons of the mantle.
�l. Properties o.f the Spot (Differential) Sounding Systems -
In reconnaissance prospecting seismic research relativelp simple observa-
tion systems are used. A st~dy is made below of the general properties
of the spot seismic observation systems. The problems of their practical
realization are discus'sed in Chapter IV.
Sounding
The simplest seismic observation system is sounding made up of the source
(0) and the receiver (S) of elastic oscillations (Fig 9, a). The source
and the receiver are separated from each other by some (optimal for record-
ing the investigated waves) spacing ~ called the sounding base. The informa-
tion about the kinematics of the wave field obtained by one soundin~ is
exhausted by the wave propagation time (t).1
The sounding for monotypic wa,ves does not have polarity~~ thexeiore the source
and the receiver can change places~ The pronagation time o~ the monotypic
waves does not change ~rom th~s conversion.
lIn practice it is exvedient to have a linear or area type installation of
, seismographs at the reception point. This makes it possible to determine
the regularity of the waves and their apprent velocities, which is imPortant
for wave correlation. The sounding with a distributed receiver is called
differential soundin~. _
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' Ti~e soundin; position in the obsexvat~.on p~ane i.s determined by the
- coordinates o~ the central point of the base m and the angle 6~ormed by
the soundin; base with some ~ixed direction. For observations along the
profile with which the x--axis is usually matched, it is sufficient to
indi~lCe ~he x-axis of the point m.
1; C
a
o m= ti t ti
~
-
\ I~ hm
o~ m a S \h t~ U t~
L zm 1- ~ 4,. ~4
~ V
. 0 ~ S
s z~ x
e
~ ~ x"
~ ~ ~ -
Zf6L r -ro_ _ a- - o- -v. -o
2~ 3 x
L --o--~t-~--o-o I
~ I B Hanpaenenue ~ y~
1 I m eoccmanW+
x x+ez ~ � �
Figure 9. 5pot observation diagrams
Key:
1. ascending direction
Any seismic observation system (conCinuous or discrete) can be made up of -
the soundings, ~ust as the simplest elementary systems. Let us first
~ consider the properties of a single sounding, limiting ourselves to the
most widespread cases of recording reflected and refracted (t~ead); waves.
It is impossible to study the seismic observation systems separately from -
a model of the medium approximating the actual geological section. As the
model l.et us take a two-layer medium with plane boundary at a depth zm
under the sounding center, wiich an angle of inclination ~(Fig 9, ~~j.
The elastic wave propagation velocity in the upper layer (v) and along the _
boundary (vboundary) are consCant. The condition of cons~ancy of the
parameters v, vboundary and � is introduced only for the loca5. ~zction occu-
pied by one sounding. Therefore in the ma3ority of cases this approximation
is suitable for studying media with curvilinear interfaces and variable
wave pr.opagation rates.
G. A. Gamburtsev [20] introduced the concepts o~ complete and incomplete _
seismic observation systems. The system is considered complete, by the '
data of which a unique determination of all of the unknown parameters of
the model of the medium is possible. If the�observation system is inade-
quate for the unique solution of the problem, it is incomplete.
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Only one VAZtIE~ of the a~r~Lval time o� the invest~.gr~ted w~ive is mea5ured by
a 4in~;le sounding. Consec~uently, the soun~ling can be considered ~ compleCe
system only in cases where the number o~ unknown parameters j.n tt~e -
approximating model is no greater than one, I'or the adoptecl two-layer model
the sounding is an incomplete system, f.or the number of unknown parar~eters
reaches three i.n the case of observations of reflected taaves (zm, ~ and v)
and four when recording refracted waves (2m, v, vboundary)� Let us
j.nvesti;ate the problem of ambiguity1 of the determination of the depth of
occurrence of the seismic boundary by the data of one sounding when tti~
values of the velocities and the slope angle are ~iven c~l.th some error.
As bhe measure of the ambiguity we sha11 consider the ma,a,nitude o{ the
error at depth occurring as a result of inexact assignment of the remainin~
parameters of the medium.
Let m~, m~ and ~,boundary be the errors of the parameters c~, v and vboundary�
Then the error in depth as a result oP inexact assi~nment o{ each of these
parameters will be equal to the following respectj.vely:
dz
~mz)~ = a~ mW~ ,
~m:~o = d~ mo~ ~AI.1) ~
da -
- ;Zey � 1. boundary (mZ ~Z ~ dvr m�r' -
where z is the depth alon~; the vertical at an arbitrary noint of the sound-
i~tg base, that is, z=z(x), O,x~Q.
In order to find the derivatives it is necP~sary to have the function z(x)
of the parameters of the medium. Tn the known hodo;raph equations For the
two-layer model l.et us espress the depth h with respect to the normal to
the boundary under the oscillation source in terms of z(x), considerinp, the
angle ~ positive in the direction of dranPin~; of.the boundary;
la = z(x) cos ~p - x sin q~, (II.2)
For the cases of reflected (tzefl~ and refracted ~trefr~ We obtain,
respectively:
toTp = v ~~4 la (x) cos ~ ( 2 - x) sin ~]2 lz cosa (II.3)
~1~
t~ 1 2 cos t z x Cos t x Siil c i
- n [ ~ ) W -I- ( Z - ) P] -I- v cos cp, (II.4)
, r
I:ey:.. 1. refl; 2, refr
1The velocity ~v, ~boundary~ and the angle o~ inclination of the boundary
are differential parameters; there.fore the ~problem of determining them~is
naturally solved not by the data frdm�a single sounding, but by a system
, of soundings when measurement of the time gradients is possible.
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~ where i=are sin v/vboundary'
rrom equationa (II.3) and (ZI.4) we ~ind the necessary functions:
82
a (x) _ (x i ) tB ~ -4- ~ , / U ~�Tp - l' , (II.S)
i 2 con� q~
vt
z(x) = x- Z tg rp 2 cos ~ cos 2 t~ (II.6)
Aft~r differentiation of equations (TT.S} and (.II.6) and simple transforma-
tions we obtain the following expression for the relative errors in -
determining the depth at an arbitrary point of the sounding base. -
~ In the case of reflected waves:
(zz)~ - (z~ 2zl lseca 1' j~ tg c~ 1 m~,
m m m/ ~+C r4z" ) J -
~ ~mz)n ia ~o m ~iI'7~
zm -(1+4zm) u .
In the case of refracted waves:
~ Z)m _ L\tm - 2tm) se~2cP (1 -F' Zim tg dl t6 cP~ m~, ' .
\ i
~i = U-� secz i, . (II.$~
~ t~or _~2zm - tg i I tg i,
1
From the formulas obtained for (inz}' it follows that the effect of the error
in the slope angle depends on the n~sition of the point x at which the
depth is caZculated. The form of this function is determined to a ~reat
extent by the initial information about the slo~e of the boundary. ~,io
cases are possible. In the first of them the si�n of ~(the direction of
~ drop of the boundary) is known in advance. In the second case which is
more widespread in practice, the direction of the drop is unknown. The
slope of the boundary usually is a sign-variable function; its most probable .
value can be assumed to be zero. This assumption leads to an error in giving
the slope angle equal with respect to magnitude to the first slope (m~=~).
Let us consider the first case. Let us orient the x-axis in the drop
direction; then the an~le ~ wiil always be positive. From the first .
equations of the system (II.7) and (II.8) it follows that on the prof ile
a point xopt exists, at which (mz)~=0, that is, the depth z(xoPt).is found
uniquely. For reflected waves
( L
xonT = 2 I 1- Zi (1-{- 4z2 1 sin 2cp , (II.9)
~ ~ , -
Key: 1. opt -
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- for refracted waves
i
xunr - ~ 1- ~1 (1 `l t,g d l si~r~ 2tp~. (TI.10),
~1~ ~ m ~
Key: 1. ont
The point xoFt;is always shifted from the center of the sounding base in
the ascending direction of the boundary~. Tfie magnitude of the shift
increases with an increase in slope and with sufficiently large angles the
point xopti can go beyond the limits of. the sounding base (see Fig 10).
In the second case where the direction of ascent (the sign is unknown,
the error (mZ)~ cannot be indicated uniquely. Therefore it is expedient
to consider the maximum value of the modulus of this error in each point
of the sounding base to be maxl(mZ) I'or the reflected and refracted -
waves considering the fact that m~=~, we shall have the following
resnectively:
max m
~~m z)~ r l im - 2zm I secz cP -'r'(1 -f- ~Z ~ tg (IT.11).
L \ m
max m x l
z~~~= (im 2imISeC2cP-~-(1-}-zzmtgiltg~~~J~~~. (II.423
\ /
At the center of the sounding base (x=R,/2), the investigated functions
have a minimum value which inc�reases with an increase in the slope angle
of the boundary (I'ig 10, b). Consequently, in the oiven case the central
point of the base is characterized by the least ambiguity in determining
the depth. This characteristic has important significance in sounding
theory.
As a result of investig,ation of both cases it is possible to formulate the
following sounding property. The ambiguity of the determination o~ the
devth caused by inexact assignment of the 51ope angle of the boundary is
different at different po~t~ts of the sounding base. In the general case
where the ascending direction of the boundary is unknown, the center of
the base is characterized by minimum ambiguity. Tf the ascending direction
is given, then there is a point un the profile at which the dePth wi11 be
- found uniquely.
~ The second property o.f the soundin~ following from ec~uations (II.7) and
j (II.8) consists 3n the fact that the ambigui,ty in determining the depth
~ at any point of the source~receiver interval increases with an increase
' in the sounding base. The errors (mZ) and (mZ)~ in the case of reflected
waves are pro~ortiona.l to tfie square o~ the ~6ase, For the refracted waves
_ the values o:~ (mZ)~ and ~mZ)`~ are proportional to the base.
bound~ry
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Consequently, ~it is necessary to strive to ~ise soundinPs with the least
Possible distances between the source t~nd the receiver of the oscillations.
(mz)w~ a ' ' b ,
Z ?5 . mC2~; `Yo '
30 ~'--2
20
~e~�
_ 15 ~ ~=e5� 2~ \ /
~ ~ /
10 f5� PO \ _ ~
~ /
5 ~ 5~~ f5 \ / ~30
~ \ ~ ~ ~
~ \ ~ !0 ~ ~ ~ `
~ \ \ C x ~ \ ~ /
3 ~ 5 \ 1�
\ y~�
~ f5
. 0�
t0 0 ~ L x
Figure 10. Indeterminacy in the depth of occurrence of the
re�lected (1) and refracting (2) boundaries caused
by the effect of the slone angle R/2zm=5, i=50�.
The ascend:.ng direct~on (m~=2�) is known (a),
unknown (~e~=~) (b).
The practical importance of the last condition can be illustrated by the
following example. Let us comnare the errors in determining the depths of
occurrence of the foot of the earth''s crust under the conditions of
platform regions (z=40 km, ~=0) accordin~ to the soundin~ data usin?
reflected waves with bases o.f ~,1=200 km (transcritical reflections) and
1C2=100 km (reflections near the critical an~le) with fised error at a
calculated velocity v. Using the second equation of systems (II.7), we
find the magnitude of the error ratio for x=1C/2:
2 2
~"`Z),~~ _ + l~ ~ 2,8.
m Z Z
~ z~o~ ~m + j2 .
Consequently in the ~iven example~ deczeasing the base ~rom 200 to 100 km
leads to almost trinle decXease in ambi~u~ty.
The depth error as a r~~sult of inexact assigrnnent o� the velocity in the ~
covering medium in the case o~ refracted waves (see the second ~ormula
in system (II.8)) does not denend on the size of th~ sounding waves and
is identical in the entire source-receiver ran~e.
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In practice by the sounding data ~.C is expedient to determine not the
vertical depth z, but the depth h along the normal to the boundary, ~or
the value o~ h is more res~istant to the e~~ect of the slope angle of the
boundary, especially for relat3,vely~ sma11 bases. It is possible to be
convtnc:ed of this, in particulnr, hy comp3rin~; the co~�respondin~, errors
in the vnlues oC z and li nt the cenCral polnt n.C eh~ souncl~Ln~ br - ~n�
rt-i
In the presented expressions hn is the vertical pro~ection of the beam tra- -
jectory in the given layer, vn_1(hn-1) and v~n are the velocities at the
foot and in the cover of the layers respectively with the indexes n-1 and n.
The remaining notation is clear from Fig 21.
The angle ipl of approach of the beam to the observation line is found by
the formula
iol = aresin ~-01 - cpl, (II.4S)
k
The value oi the apparent velocity vk is defined in terms of the vertical ~
and horizontal time field gradients (see II.42).
' s I
� � y? .
.
~ tor
~
~ ~n-~
I ~R
n ian -
~ ~ hn
I Wr�?
~I ~
_ ~o~ S~
n
Figure 21. Substantiation of the transition to the new obaervation
level.
I-- observabton~line; II reduction level.
Applying formulas (II.4II), (II.47) and (II.46) successively, let us
calculate the values of ~x and Qt in all layers (beginning with the first)
for the beam reachin~ the point~S. The values o� 4x1 and Qtl are found
analogously �or the beam emergin~ from the source 0. ~or reduction of the
soundin~ OS to the new observation line ~O1S1) the time must be changed
by the amount
~T = - C~ Otn ~ ~tn) ~
~
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the sounding center is shi�ted along the x-axi.s by
, d,x = 2 ~x,t, - ~ vxn),
f and the sounding base is altered by the amount
_ 4L=--(~'~xn-{-~`c1x�).
The summation is carried out with resnect to all layers between the ini[ial
arid the new observation lines, The values of ~x and at are positive on
recalculation downward, and as they are negative on transition to the _
observation lin~ above the initial level. The corrections oT, ~x and ~I.
_ are calculated for the required number of points of the initial time f.ield; -
the new field is constructed by the corrected values.
Instead of the calculations by formuias (IT.46) it is possible to use the
radiation patterns for the �iven laws vn(z). In the special case where the
velocities in each layer are constant and the boundaries are curvilinear,
equations (II.46) acquire the forri:
~xn = 12n t~ Zrtr -
hn . (II.46')
~tn an Cos in
Still oreater simplifications are obtained in the case of the horizontally
stratif ied medium:
~xn hn~n
�e ~
V - �ri
(II.46")
hnvk
~tn = ~
vn~v? - u; � '
I
Here vk i~ the value of the apparent velocl.ty at the intersecCion point of
the day surface b;~ the seismic beam,
Appearance of Surface Inhomogeneities in the Ti_me Field
T,le shall consider the travel time difference o� the wave in the presence of
a surface inhomogeneity and without it with unknown position of the source
in the receiver as the surface distortion~ In the latter case the upper
- inhomogeneous part of the section is replaced by a homogeneous medium with
' the same velocity as in the undexlyin~ rock. On the dif.f,erent field isolines
the in�luence o~ the surface distorti.ons turns out to he distributed
! differently.
Actually, we have two field isolines tl(x) and t2(.x) which correspond to
the bases Q1 and k2. At an arbitrary point of the profile x the Cime tl(x)
will contain the effect of the inhomogeneities at the points x~Rl/2 and
x+kl/2 where the corresponding source and receiver of L-he oscillations are
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located. The value of t2(x) will be distorted by the inhomo~eneities at the
points x-R~%2 and x+k2(2. Consequently~ the time distortiona tl(x) and t2(x)
can turn out to be di�ferent with respect to r~a~;nitude. -
r , � t~---a-
l*
� LS---~ _
G~
~ '~-Lp-+'
Cp
~ b�0
0 i~ $ 2
~o y
~
~ \ U
Fi~ure 22. Appearance of the surface inhor.?o~eneities in the
time field
a-- ti.me field; b-- section and beam diagram
A characteristic e~;ample of the appearance of the surface inhomogeneities
in the time field is illustrated in Fig 22 for the case of relatively simple
structure of the medium and reflected wave soundings. For R,�0 the section
with low velocity vp is intersected by the seismic beam twice for different
positions of the soundin~ center. On the lines k~=const two anomalies in
time are recorded which are separated from each other by a distance close
to the corresponding value of Q~.
- In practice the values of the velocities in the upper nonuniform layer ~
(in the low velocity zone and for operations by the deep seismic soundin~
method, in the series of loosely compacted sediments) are usually signif icantly
less than in the lower medium; therefore it is possible to ne~lect the depen-
dence of the surface distortions on the an~le of approach (exit) of the
seismic beam at the foot of the nonuniform layer. Then each uoint of the
profile in which the source or the receiver o~ the oscillations is located
can be assigned some magnitude o~ the distortion b(x) which does not devend
on the sounding base. Under thi~ condition the equation of the field iso-
. lines with the paramter k~ is written as follows;
t~ ~x~ = tf (x) -I- S (x - 2 ) -I- 8 (x -V- 2 (iI.49)
where t'~(x) is the undistorted time. ~
~n the special case ~�~here the function s(x) is linear, the distribution of
the time field distortions does not depend on the magnitude of the sounding ~
bases. A11 of the isolines wi11 be distorted identically. �
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Peculiarities of the Time Field w;~th Ar.ea Observat3ons
_ If the set o� soundings with the bases which vary in some interval is
_ placed in an area (in t}~e observation point x, y), then, just as before,
referring the times to the centers of the corresponding soundings, it is
possible to construct a number of isochron maps for fixed values ot the
bases As a result, we obtain the surface field t(x, y,R~). Let us
consider its peculiarities for the reflected and the refracted waves.
The surface time f_ield is nonuniform, for the ti.me of arrival of the wave
depends on the azimuth ~y which wi11 be reckoned from the~direction of drop
of the boundary (see Fig 9, d) for soundings with ~ixed base and invariant
position of the center.
Tn the case of reflected waves
t,p = ~ Y4h2 li (1- sin= cp cos2 (II.50)
where � is the total slope angle o� the boundary; h is the depth along the
normal to the boundary at the center of the base.
The minimum time will be obtained ~oith orientation of the souncling base
across the strike of the reflecting surface
- tl = ~ Y4h2 -f- l'~ cos2 cp, (II.50`)
the maximum time will be obtained for the strike direction
t.~ _ ~ y~f~~2 + i;. ~~r.so-~~
From the preceding three equations it is possible to derive the following
expression:
tw = t j cos2 ti. sina (II.50"')
permitting the required calculation of the fields. This expression can also
be interpreted in the sense that the spatial time field of the reflected -
wave is characterized by two functions: tI,~x, y, R) and t~;x, y, R,.),
Knowing these functions when solving the direct prob~em, it is possib~e to -
construct the field t~,~ (x, y, R~ ) for the given arbitrary~ oz~entation of the
individual soundings in accordance with the transformation (TT,50~").
The ambiguity of the field t(x, y, k, ) at each noint of the observation
~ surface can be characterized by the ~ifference between the maximum time
and the time for orientation of the sounding at the arbitrary lzimuth ~a
~ 58
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~t~p = tn - t~p = t p 1- 1- 1+
4h9 S1I1` (PCOSZ i~ ~
1~
' ~ t g(1- j~1- sin' ~ cos~ (II.51)
The time difference is maximal for soundings which are located along the
strike and across the strike:
1 sin= < t 1- cos cp).
~tmaz=~~-11.=t~ 1- ~~l- 1+~ihs ~ p~
~
~j~.Jl~~
Analogous relations for the head ~aaves have the form:
t~ _ 2h ves t~ uf V1 - sin~ y~ cos~ t~%, (II.~2)~
r
2h cos t ~r~
tl = ~ U cos c~, (II.5~ ,
~ r
t 2h cos t+ l~ . (II.~2")
. ~ = v J'
The corresponding relation between the times is exnressed by the relation
t � j 2 l z
f,y - t ~ - Y~ V ( r ) sinz ~ -y- (t p - tl v ) cosz (II.52,~~y
In the given case the value of 1~~/~boundary enters into the time conversion
formula.
For the time difference ~t~ and ~t~X we have:
. ~t,~ = t tq = U~ (1 - 1- sinz cp cosa (II.53)
Otma= = t~- tl = v~ (1- cos W). (II.53') .
The amb~,guity of the surface t:Ime ~ield increases with an ~,nczease in bhe
slope angle of the reflecting and xefracting boundaxies, k'ax �~0 the field
is unique. By formulas (II~51F) and (II.53~), it is possible to estimate
the degree of ambiguity for spec~.~ic conditions, The extended seismic
boundaries in the earth's crust usually fiave small slope angles measurable
by the first de~rees. There~ore for deep seisr.iic studies in the ~a~ority
of cases it is possible to neglect the dependence of the time on the sound-
ing azimuth. If the slope angles are large, the effect of the ambi~uity '
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o~ the time ~ield can be excluded by xeducing the time to some defined
direction, for example, the strike d~,zection, In this case the correctlons -
to the observed values o~ the times are ca].culated by the formulas (IT.51)
and (II.53), The azimuths ~ reqiiired to calculate the corrections are
determined by the isochron maps or by the structural maps constructed in
the first approximation without considEring ambi~uity of the field.
For a complex structure of the medium, the necessity �or cons-Ldering the
ambip.,uity of the field t(x, y, R) caused by an anisotropy oF the velocities
_ can occur. The effects causecl by the dependence of the hoiindary velocity
on tlie azimuth when studying the surf~ce of tlie platform basin hy refracted
waves can be especially significant.
As is noted above, the field t(x, y, in the observation plane has
ambiguity even for the simplest models with a Plane inteT`face and uniform '
medium.
In reference [94], which is a further developr.?ent of the theory of spatial
reflected wave soundings, the possibility of the construction of a unique
field of some ma~nitude P~ determined by the measurements on the orthogonal
cross soundin~s with orthogonal orientation in the observation plane is
demonstrated. Here the uniqueness of the field is maintained with great
accuracy for a quite lar~e set of standard models. This has o.ffered the
possibility of strict solution of the inverse problem [96J.
In conclusion, let us point out that the theory of time fiPlds developed
above in recent times has begun to be used in structural seismic prospectin~
both in the solution of the problem of isolating signals against an inter-
ference background and for more proper solution of tlie inverse problems.
g3. Peculiarities of the Identification of Waves and Use of Their Dynamic
Characteristics
iJhen working with the sounding procedure, we are dealing with waves excited
at various points and recorded on short installations not connected to
each other. Under these conditions, for wave identif ication it is impossible
to use the known rules of positional and transpositional correlations
which presuppose the presence of continuous observations and placement of
observation sources f ixed in a def ined way. In the spot sounding procedure,
use is made of the so-called discrete wave correlation in which, along
with analyzing the wave field, broad use is made of the a priori data on
the general laws of the geometry of the a.nvesti~;ated medium and its physical
properties.
Tt~e dynamic characteristics of the oscillations which play an i.mportant role
in wave identification carry valuable information about the properties of
the medium, including those which cannot be relilbly investigated only by
the data on the travel times of the elasttc waves recorded for low-detail
observations. Therefore the attraction of the dynamics of the observations
to obtain additional information about the deep structure even in the
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reconnaissance research phase is natural. ~xistin~; methods of solving this
problem hasically have been calculated for the use of seismic recordings
i.n a wide ran~;e oE distances �rom the source with careful monitorin~; of the
conditionA t}int the excitation pointa and recording of the oacillations;
therefore thcy cniinc~t he uaed in the spot eoundi.n~ procedure without con-
ytderin~; its specifLc nr~ture. ~
= Peculiarities of tidave Correlation During Reconnaissance Prospecting Research -
- Tlie discrete correlation, in addition to the sounding procedure, is used in
one form or another in the works designed to obtain hodo~raphs, above all,
' dotted and piecewise continuous. The wave identification conditions in these _
cases are not identical as a result of the peculiarities of the observation
systems used: and these conditi-~ns reduce to the following.
, If we depart from the instability of the conditions at the goints of excita-
tion and reception o.f the oscillations, then the basic causes of variation
of the characteristics of the tracked wave along the prof ile can be con- ' _
si~ered to be the variation in structure of the investigated medium and
- inconstancy of the distances from the source to the receiver. As a result
of inconstancy of the distance, significant alterations of the wave picture
are possible: the reflection-refraction conditions of the waves vary, at
certain distances these interf ere with other oscillations. When working on
obtaining extended hodo~raphs, the two mentioned factors have an effect.
The conditions of discrete correlation in the spot sounding procedure are
more favorable, for the observations are tnade with low-variable sounding -
bases selected in a relatively narrow region of the most reliable generation
of the tracked wave. Accordingly, the recorded wave f ield is ~ore stable,
its variation along the profile (or with respect to ar~ea) is primarily caused -
only by the structural peculiarities of the medium.
The basis for the investigated discrete correlation procedures is the prop- .
osition of the existence of sustained seismic boundaries commensurate with
respect to extent with the dimensions of the investi~ated section which
correspond to stable reference waves. Z~lith thickening of the observation
network, the possibility appears for tracing waves from less extended
boundaries and waves with more variable characteristics.
The requirements on the reference waves are different for different observa-
tion systems. For the spot sounding operations, stab3lity o~ the wave
characteristics in a relatively narrow range of distances from the source
is sufficient. The recording of re~lected waves in the v~.cinity of the
angles close to critical where the reflections often predominate with respect
to intensity although it is not always possible to congtruct sufficiently
elongated hbdographs by them can be a situation which is characteristic
and frequently used in the sound~.n~ procedure, When obtaining the hodographs ~ .
the stability of the character3stics must be observed over signi~ica~ltly
lon~er intervals and distances from the source.
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The discrete correlation is based on ~oint use nf three ~roups of atrributes:
wave, physical and geological. -
_ The firoup ~F wave ~~ttrihiites tnclt~des icinemnt~ic and dynaml.c ~ar~~meCerA ~f
the wavea taken Prom the seismograme: the tr~v~l times, a~Parccit vclocity,
relative intensities, apparent per~.ods and other characteristics oL- the
oscillations. A study is made o~ the relationsof these parameters for -
different waves considering the laws of variation on removal from the
source. For ~eliable determination of the wave parameters, as 1 rules it
is suff icient to have a recording of the oscillations at one point.
nistributed installation of the seismographs no less than 0.5 to 1 icm long
is needed. As a result, the nossibility aPpears of not investip,atin~ the
waves with short cophasalness axes and estimating the apparent velocities
- and their relations for different wav~s. It is desirable to make a Chree-
component recording of t11e oscillations to monitor the reRularity ~f: the
waves ~oith respect to their polarization characteri.stics and involve othPr
types of waves, in particular, coMposite taaves, in the deciphering of the
structure.
The physical attributes are based primarily on the data obtained as a result
of the interpretation of the effective, boundary and stratal velocities
of elast ic waves. With proper identificatlon of the waves, the velocities
found, thea.r distribution with respect to depth and alon~; the profile (over
the area) must not contradict the laws existing or nresupposed for the
investigated area. This requirement is not absolute. The presence oF
contradictions serves only as grounds for repeated critical analysi.s of the
correlat ion. The matchin~ of the independent deL-erminations of the velocity
with respect to waves of various types, tying to the data with respect to
other physical properties (density, electrical activity) in accordance with
the existin~ correlations has ~reat significance.
_ The geolo~ical attributes (section attributes) encompass the morphological
characteristics of the surfaces with which the seisMic boundaries are identi-
fied. ~)e have in mind the depths of occurrence of the houndar-les, the slope
_ angles in ther~, curvatures, thickness of the layers, matchin~ oi the struc-
tural plans on different section levels characteristic of the given area of
_ the peculiarities of the structtiral forms, and so on. The basis for this
~;roup of attributes is ]cnowled;e of the ~;eolog~r of the area and analo};ies
with similar territories.
The relations of the different attributes have a lar~e role in cliscrete
correlation. P.e~;ional and local relations are usecl !'or the distribution
' of the nhysical properties of the rock with the pecu_liarities oF geoloaical
structures, the dependence of the caave narameters on the moclel of the
medium characterized by ~eolopical and nhysical. attr.ibutes.
The source of information for substantiation of ti~e discrel-e correlation
attributes is the results of detailed seismic onerations pertaining both
to the study of L-he wave field and to the structural Iaws and pronerties
of the earth's crust and tops of the mantle. In adclition i:o the laws of
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Cc:neral nature, as a rule, it is necessartiT to consider the peculiarities
of tl~E~ tipecif ic arels. There�ore, alon~; with an~.lysis of th2 r.iater.ials with
res~~ect ro otl~~r. territories with a similar ~;eolo~;ical situation, usually
~ I~c~P~rc~ bc~;;inni n(; work j,l tlie new area erect~l pnrametric ohaervntione ~re
m~1de by the method of plecewi.se continuoue profilin;; to ~liscover the local
pecu:li~irities of the ~,rave ~ield.
In connection with broad use, along with the ~~~ave attributes of the data on
thP properties ~f the medium, the nrocess of discrete correlation cannot be
considered as an j.solated, initial step of the interpretation. This process
continues in the steps of deterr.iinin~ the elastic properties of the mediur.?
and construction of the sections and structural mans. The noncorrespondences
in the results ootained nrovide a basis f_or investi~ation of other versicns
of the wave correlation.
Let us discuss t~ao peculiar~ties in the method of reconnaissance prosPectin~
research important to the discrete wave correlation.
The first peculiarit}~ is ~oint application of waves of different tynes -
(reflecte~, head, refracted). T�lhen using individual correlation attributes
and their interrelations, it is necessary to consider the corresponding
peculiarities for the diff erent waves. In addition, further nossibilities
appear for control of the correlation with respect to the criterion of non-
contradictoriness of the results obt~ined b;~ u~aves of different typ ea.
The second pectiliarity is the ~reat e:cCent of tt~e inv~sti~ated seismic pro-
files and re~ions encompassin~ nonuniform blocks of the earth's crust with
distin;uished seismological conditions and wave picture. Therefore the
basic assumption regardi.n~; the maintenance of the seisr~ic boundaries and
the waves correspondin~ to them o~ten is made not for the entire territory
as a whole, but only within the limits of one or several compaz-atively
uniforn bloc?:.s, the transverse dimensions of ~uhich usually do not exceed
several hundreds of kilometers. On makin~ the transition from ori.e t~lock
to another, sharp variations in depths of occurrence of the seismic sections,
wed~ing out of the individual layers, curtailment of the tracing of certain
boundaries, and variation in the propagatior.. rates of the elastic oscilla-
_ tions are possible. All of this can lead to differences in the discrete
correlation attributes and their interrelations ior individual blocks of
the earth~s crust. Consequently, a careful analysis of the seismic record- ~
ings made is needed directly during the course of the field operations for
introduction of the corresponding corrections to the observation technique.
~'eculiarities of Using Dynamic Wave Characteristics
These characteristics, whi.ch are highly sensitive to the properties of the '
medium can be used to obtain in�ormation about the deep structure~ Th~
information about the peculiarities of tfie medium whish are weakly mani~
fested in the lcinematic parameters of the elastic waves recorded in a
~parse low-detail observation is especially valuable. ,
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l~Ult Ul~ I~ IC 1A1, iI5E ON1,Y
The usual methods of util~.zing the dynamic characteristics, as a rule,
cannot be used without alteratxons in the method o~ spot soundin~ as ~z
result of the specific nature of the worlc, A charac~erlst-i.c featt~re o.E
� the operations is frequent chan~i.ng o[; the osci.l.lat-ion excitat:~on and
recordin~; P~jnLs, seP
I
I
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ror the ~nown value of the boundary velocity v0 we find t0 expressed as
follows:
t ~
to = t� - i, . II.a7 '
~ r
Solving the last two equations ~ointly, we �ind that t'~ is equal to the .
value at the point having the x-axis:
x= 2(1 ~ tg i. tg 2~.
Thus, at the point with the x-axis 2(1 ~ tgi�tg 2l the value of t~ is
\ /
equal to tH/~/~boundary�
When usin~ a single-point observation system (s,ystem A) for determination
of t~ it is necessary to know the value of the boundary velocity vboundary
which can be obtained for soundings by the more complete systems of observa-
tions, by the KA7PV refracted wave method profiles.
The expression for the relative error in tp as a result of the error in the
boundary velocity has the form
mt� ~ ~ 1_=- -
t� �r ~tn�r l~ �
If it is known that the slope angle � is small, then tg i�~tg 2-0~
and for the x-axis of the depth ref erence point we obtain the approximate
formula x=k/2. The relative error assumed when using this formula is
expressed by
m, tg ~ � �B 2 .
�7
x i-tB 2 -
Spot Sounding Systems. Keeping the assumptions made, let us consider the
observation system with two blast points O1 and 02 and two reception
points A1 and A2 having observed times tl and t2 respectively (Fig 24, a).
According to the duality principle, the times tl and t2 can be carried
over to the point O1 and O2. Thus, i~ the orip,in of the coordinates is
placed at the point O1, then -!n the x, t coordinate system we h.ave four -
points (K, L, G, H) with the coordinattes: -
K(S l,, t,), G(0, t~,
_ L~lt~ t~)~ H(s~ t,).
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- 'L'he equztI.on ~E tlie straight lines running throug,h the points K and L
has rhe ~orm
'x-(S-I-i~) -
1~ ~yi la) = it - t~. (II.58)
The straight line running through the goints G and H is described by the
equation
.
S = _ ~1 ~ (II.59)
:
a ~ � t ~ -
- t ~i L 'tQ - - - - - - - - - tia
~ -
, ~ tC
H -
- ~ f~~ K~ tn tti t~
to to ~ hl M ~ N
~ S LQ R ~
0~ 02 A Z A~ a a b c a e f z
U U
U~ y L~ V
Figure 24. Derivation of the calcuJ_ated formulas for soundings
by the refracted wavQ *~~ethod in the cases of :
a-- two sources, 'b three sources
For the times tl and t2 it is possible to compile the followir~g equations:
ti = toi -I- v1 sin (i - (II.60) -
ts = to~ -f- l~ sin (i
Here tpl and t02 are the values of t~ at the blast points O1 and 02. The
equation of the line tp running through t01 and t02 is written as follows;
x t - ~01
S =pf r ~pi �
; Considering equations (II~60)t we have
i
, t-ti-~- tU sin~i-W)
x (II.61) _
~ S r~ - l~ sin (i - ti -f- lU sin (t -
u
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S~?�::ng equations (II.58),(II.59~ and (II.61) jointly, we find that all
tl~ree lines intersect at one point i4, the coordinates of which
~ Zt
xm~ = R ~
i + s (IT:62)
t,li - til~
� tM- Il-ls ' ~
Thus, for observation systems of this type (D in Fig 23) it is possible to -
find the value of tp and the x-axis xto to which this t~ belonga. Let us
note that in this case tp and xt~ do not depend on the boundary velocity in
the slope angle of the boundary Now let us find the boundary velocity.
Subtracting one equation of (IT.60} from the other, as a result of simple
algebraic transformations we obtain:
(tl- tE) (R S) cos ~
X
vr - ~ = 2 _ (R - S)'sinz ~ . ,
~ i s) Ua
(R - S)a sin9 cp a
~ ~~R - S)s sina cp -f- (R S)a cos3 f va - (tl - t'~
X 1 ~ 1 (tl - ta)Y (R S)a cos~ ~ _
~ (II.63)
Let us present the e~;pressions for determining the values of t~ and Vboundary
in the case of the system of elementary sounding made up of three blast
points and three reception points (see Fig ?_4, b) without intermediate
calculation.
Proceeding analogously to the previous case, we fiiid the equation of line tp
in the form
af--bd af -
x ~~ta - tb~ ~~a - tc~ a - ce 1 ~ a/ - ce [ab (ta - t~~ - ac (ta - tb~j
to=ta~"" af-bd ac-ab .
aj-ce
~ . (II.6!.) ~
The f inal formula for the boundary velocity has the form _
(af - b~ cos ~ ~ ~
v~ - [(af - bd - 2ab) tQ {bd - ce) - th (af - ce) t~ (aj - bd)j � II.65
ta - tb - 2ac (af - bd) -'La6 (af - ce)
The investigated s~unding system pexmits us to obtain other simpler systems '
of the type D1, D2, D3, B1, B2, E1, E2, and so on(see Fig 23).
69
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The three-point system with subsequent match~i.ng of the observation noints _
; with the blast points (see F~.g 23, B1), which is a special case of the
above-investigated ~eneral three-point system, is of: the greatc~st intereat.
In thie case the time tp is determined by the formula (IT.54), and the
~ following expression is valid for the boundary velocity:
I 21,i~ cos cp (iI.fi5')
vr ~i (T - ~o~ -I- l~ l7 - ~s) .
For small boundary slopes, it is admissible to consider cos ~=1,
i
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CHAPTER III. RE^10TE-COi1TP.OLLED TAY'GA SETSMIC SYSTLM
~l. Functional Diagram of the Equipment
The structural diagram of the equipment is presenL-ed in Fig 25. One set of
the equipment includes an arbitrary number of portable remotely controlled ~
six-channel ma~netic recorders with reel-to-reel tape drives, one dispatch
station for generating the remote-control signals and time marks and also
the base reproduction unit on which the magnetic recordings are reproduced,
the seismic signals are filtered and the seismograms are recorded on a
photo~raphic carrier. During the seismic stud3es, these elements function
as follows.
The dispatch station, which is made up of an�instruction coder ~nd a power-
ful radio transmitter, is installed at the blast point. A time ~:oop is'
connected to the instruction coder.
Any forn of transportation is used to install the seismic recorders at the
planned observation points, the number of which is limited only by the
_ number of recorders available to the seismic crew. At the observation point,
two three-channel seismic cradles with groups of seismic receivers and a
radio receiving antenna are connected to the recorder. Then the recorder
is put in the ready mode where the electric power is supplied only to the
radio receiver and a special remote-control instruction decoder, and it is
_ left unattended at the observation point.
_ The recorder will stay in the ready mode until the radio transmitter from
the dispatch station begins to transmit a special si~nal generated by the
coder.
The dispatch station is switched to the transznission mode when all of the
recorders have been installed and.the charge is ready for detonation.
~ The remote control si~nal generated by the coder is simultaneously an
encoded time mark signal.
The signal transmitted from the dispatch station is received by the radio
receivers of all the recorders and goes to the decoder inputs. At one of
, the outputs of each decoder there is a servo relay, and its other output is
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connectecl to the i.nput of the circuit for recording the time mark signals
on magnet~.c tape. The servo relay switches on the power of the tape drive '
mechanism on the recorder; the seismic signal on amplifiers, modulators
and time mark recording circuit, that is, it switches the recorder to the
record mode. On completion of the transient processes after switching on
the power supply, the recorders are ready to receive seismic signals.
Thirty to 40 seconds after switchin~ on the dispatch station, the charge
is detonated. This generates seismic waves and simultaneously breaks the .
l-.y:~.e loop connected to the coder. The sudden breaking of the time loop
clianges the structure of the time mark signals, recording the blast time.
Then, a calibrated interval after the blast time, the structure of the time
mark signal returns to the initial structure and varies subsequently with a
given period with high accuracy. This process will be investigated in
detail below.
All of the processes occuring in the coder are transmitted over the radio
channel to the recorders and by the time mark recording system they are
recorded on ma;netic tapes simultaneously with the seismic signals.
The decoders of the recorders are constructed in such a way that the servo
relay remains connected during the entire time interval that the signals
~ transmitted from the dispatch point are present at the output of the radio
receiver, independently of the changes in their structure.
On expiration of the defined time after the blast, sufficient for the
seismic wave to travel from the blast point to the most remote observa~ion
point, the dispatch station is switched off. As a result, all of the
recorders automatically return to ready and remain so until it is necessary
to record seismic si~nals from the next blast. After processin~ one segtnent
oE the profile or area, the recordera are gathered up and installed at new .
observation points, and the magnetic tapes with the recordings are reproduced
on the base reproduction unit and processed.
For the case where it is not possible to record the blast time by a time
loop, a special mode is provided in the coder. In this case the coder
generates a cyclic code with an ambiguity period comparable to the maximum
rravel time of the seismic waves, and the blast time is determined by the
recordings of a recorder installed in direct proximity to the blast point.
When developing the Tayga equipment it :Cs necessary to solve two prit!iary
problems:
1) Develop a highly efficient channel for r.iagnetic recording of the seismic
signals on the magnetic tape corresponding to the requ~~iements d~.scussed in
Chapter I, �3~ '
2) Develop a highly noise-resistant radio remote control system especially
_ designed to contrc~l the operation of tfie distr~buted seismic recorders and
" simultaneously providing for time gridding of the received information and
the blast time.
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~
~ ' -
I ~ TAP
6t1
il/~ - -
I Pn AW hP nnn I
- -
~ r----- ~ i nn ~
~ W ~PA i Hf1 Mf2 Mf3 h1f f5 Mf M( MfB ~
~
I ~ ~ 4M1 4M: M ~;M M M (K~1 ~
nn
= L----~ ~ i yf y2 y3 y4 '!5 y6 i
~
~ 2 ( ~ _ CeucManpueMr+uKU I
-
� r--------------------, ,
~ Fif'8 'lBKA 4AK NNB 3 ~
I Mfl y86 4A6 ~6 y~6 I
~ t1f6 y85 4A5 L5 I y~5 ~2~ ~
~ a I
~
I M(7 y84 4A4 E4 ym4 I
~
I~ Hf4 yB3 4A3 L 3 ym3 m I
~
' ~ t1f3 y82 4 2 E 2 y~2 ` ~ ' -
~ . i tlf'I y8f 4J~1 E1 yro1 i -
~ nrt yene p,ne ~
~------------------~_J
Figure 25. Structural diagram of the Tayga equipment
, 1-- dispatch station: M~P ~~ine loop; III coder;.
IIPD radio transmitter. 2-- seismic recorder: P1I radio
receiver; DIII decoder; '~cP servo relay; 'sn recorder
power supply; TDP ready switch; .tntic tape drive;
~I~~~ magnetic tape; AfI'1 to Ml'8 ma~natic head unit;
3ntB time r.:ark recording circuit; ~Tl~,ri . to ~ints frequency
modulators of the seismic channels; Y1-Y6 seismic signal
ar.?plifier; PI~ detonation compensation channel p;enerator.
3-- reproduction unit: :~rtac tape drive; r~~~ ma~netic
tane; r~rl to MI'~3 magnetic head unit; YBMB, YBKD, YB1 to YB6
reproduction amplifiers and ~iu}IS,-*~:z~+,~~ ~IJ1 -t-~qIIR
frequency demodulators of the time r.iark channels; detonation
comPensation and seismic channels resnecta.vely; t1FiB detonation
~ compensation channel inverter; E1 to E6 a~dders; Y~1 to Y~ 6
low-frequency filter amplifiers.
i Key:
' 1. seismic receivers -
2. galvanometers
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42. Seismic Signal Magnetic Record~,ng Channel .
- rrom the point of view of such c~~aracteristics of the recording channel as
ttie climensiong, r~ass and energy conaumption, the proper selection of the
_ struct�re of. the seismic signal magnet~.c recording channel has important
significance. In tl~e seismic equipment the moat widespread is a direct
recording with fiigh-frequency magnetization; a recording with frequency
and pulse-width modulation was used somewhat less broadly [122J. In recent
years pulse-code or digital methods of recordinp, have begun to be used more
and more intensely in the foreign and Soviet seismic recording equipment. -
These recordings are superior to the analo~ recording with respect to
accuracy of recording the signals on the magnetic tape, but they require
significantly higher magnetic tape drive speeds and significantly more complex
electronic systems to convert the analog signals to di~ial form. This
leads to the fact that the r~.ir;ital r'ecording systems are essentially inferior
to analog syster~s and appreciably more complex than the latter from the
point of view of economy. Therefore when developing autonomous, highly
economical, small-size equipment the application of digital recording systems
is inexpedient.
The analysis of the analog systems for recording seismic signals indicates
that the direct recording with high-frequency magnetization is less wide band
at?d requires minimum magnetic tape drive speed. Therefore, this type of
recording is primarily used in the autonomous seismological equipment with
continuous magnetic tape drive as occurs in the abbve-mentioned Cherepakha
and Zemlya equipment. Iiowever, the dynamic range of the recording with this
recording procedure does not exceed 40 decibels, which is its basic dis-
advantage. In addition, in order to insure this recording range it is
necessary to use wide recording and reproducing magnetic heads which are
shielded well from each other. Therefore in the Cherepakha equipment, for
~ example, for parallel recordin~ of information on 8 channels of which only 6
are used for recording seismic information, the width of the magnetic tape ~
is 25.4 mm. This automatir_ally complicates the tape drive mechanisms and
increases its size and weight. _
Frequency and pulse-width modulation are approximately equivalent from the
point of view of wide-band nature and, consequently, the requirements on the
magnetic tape drive speed [29J.
The FM-recording is preferable prima~ily because it does not require the
application of wide ma~netic heads and good shielding between them in the
module. In contrast to direct recording with magnetization in FM--recording
it turns out to be possible to hav� 8 to 9 para11e1 recorded channels on "
a magnetic tape 12.7 mm wide using standard magnetic head units designed for
pulsed methods of recording~
It is known that the basic source of interference limiting the dynamic
range of the recorders with ~T1 recording 3s inconstancy of the magnetic tape
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drive speed with respect to the recording and r.eproducing magnetic heads
[3, 291.
Therefore, for recorders with FM-recordin~ i.t is necessary either to construct -
the precision tape drive mechanisms with very lo~a instability of the tape -
drive speed or to use effective methods of controlling this problem, usually
called tape drive detonation. These procedures are well lcnown and are
described, in particular, in references [3, 29].
The first procedure is unacceptable for building portable, autonomous equip-
ment, that is, it is impossible to make highly stable tape drives
suff iciently Pconoc;iical and simple. Therefore it is expedient to consider
the following problems: what level of detonation is admissible when record-
ing seismic signals, how does the detonation influence the accuracy of the
recording, what does the effectiveness of controllirig it depend on, and what
are the maximum admissible values of the dynamic range.
From the point of view of using FI~i-recordings of seismic signals when develop-
ing the Tayga equipment, a theoretical analysis is made in order to answer
the questions. The results of the analysis were used in the process of
constructing the equipment.
In references [2, 29J it was demonstrated that the detonation of the tape -
drives leads to the occurrence of two types of interference, one o.f which is
multiplied times the useful signal (multiplicative component of the inter-
ference), and the other issummed ~vith the s~gnal (_additive component of ttie
interference). The first type of interference leads to spLrious modulation
of the useful signal, that is, to its nonl.inear distortions; the second type
of interference limits the dynamic range of the recording for this inter-
f erence exists at the output of the reproduction channel even in the
absence of. the useful signal.
The depth of spurious amplitude modulation of: the useful signal is determined
by the sum of the detonation coefficients o� ~he recordin~ and reproducin~
tape drives.l
If we permit, as provided for by the standard for analog seismic equi~mentt
3-percent nonlinear distortions of the use~ul si~nal, then in the equipment
it is possible to use recording tape drives with a detonltion coefficient
of 2.-2.5%, and reproduction units with 0,5~1% detonation coefficient,
inasmuch as it is semistationary and the only one for. a lar~e group of
recorders.
_ ~
1The detonation coefficient is the ratio of the maximum deviation of the
instantaneous tape drive speed to its average speed m=~v/vaverage'
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Thus, from the point of view of the adr~issible level of multiplicative _
nois~~ in the seismic equipment recorders, it ttirns out to be possible to
~ise very simn].e tape drives. Iiowevery in thiR case if the total detonation
coefficient oF the recording and reproducing tape drive is 3~, with a '
frequency modulation coefficient of 0.6-0.7 the level of additive detonation
- noise will be abot~t -30 decibels f_rcm the maxj.mum signal, that is, the
dynamic range of the recording channel will not exceed 30 decibels, which
is clearly inadequate.
The analysis of the known method of suppressing the additive component of
the d~tonation interference by recording the reference frequency si~nal
on the magnetic tape simultaneously with the frequency-modulated signal
demonstratecl that the additive noise can be completely suppressed under
defined coriditions and, consequently, the dynamic range of the recorder
will in this case become inf inite with resp ect to this type of interference.
Of course, in a real systeM it will be limited by the interference of some .
other nature. T�1e shall discuss this problem below.
j�Then developing the Tayga equipment, it was demonstrated theoretically and
experimentally that the degree of suppression of the additive detonation
noise essentially depends on the structure of the device suppressing this
noise and the stability of the carrier frequencies of the frequency modulators
. used.
The adoption of special measures with respect to stabilization of the
narameter of the electronic circuits of the equipment and the development
of the corresponding schematic for the device to sunpr~ss additive detona-
tion interference have made it possible to expand the dyanmic range of
seismic recorders to 60 decibels or more (see rig 26).
The structural diagra~ of the device for suppressing the additive detonation
interf.erence used in the Tayga equipment differs from those known from
the literature [2, 29 or more]~by thz fact that the subtraction of the
detonation interference frnm the si~nal reproducible in seismic channels
is done before the filtration operation, that is, before generation of
the low-frequency component. At the same time the effect of instability of
- the phase characteristics of the filters on the quality of the noise
suppression is excluded. _
~ In the LIJ~i~ to LI,~G and ~Rx~ frequency demodulators (see Fig 25, 3)
univibrators are used which Qenerate a train of square pulses of constant
amplitude and duration. In the seism~c channels the repretition frequency
of these pulses at the LI,I~1-t3A6 output is modulated by the seismic
si~nal and noise, and in the detonation compensation channel at the ~Ax~
output Che square pulse repetition frequency is modulated only by the
detonation noise, for in each seismic recording the rtrs magnetic head
records the ref erence frequency signals from the I'HZIstabilized oscillators
on magnetic tape (see Fig 25, 2). The inclusion of the HHB
inverter at the ~,i~KA output in the reproduction unit permits 180�
shifting of the detonation interference phase in the compensation channel
with respect to the detonation interference in the seismic channel.
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, Q
~ ~c rr+ax
� V
Q,fUc mar. .
. i
' qOfUc max
,
' , b
. , ~ -
~c max
~~c max
qOf(~ max
0,00lU~ ~
uc LO .
' ~^W � \ . , . '
I ~ipure 26. Oscillograms characterizing the operating c}uality
of the ma~~tetic recordin~ and reproduction channel
Fre4uency of the descrzbed sa.onal 2~ hertz. Uc max is the maximum
sign~tl recorded by the recorder w~th ampliPication coefficient of
0.75. The oscillograms of tlie s3gnals reproduced without detoi~ation
, compensation (a} an~I with detor~ation compensation (b).
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'I'l~e tiu~~~~re:~:; Lc~n of tLe ~ldditive detonfll-ion inter~'erence is realized hy
_ 5uccr~as i.ve summ~ t-.ioi1 of. two trains o� sauare ptilses from the outputs of
tf~e corr.espondinp, frequenc}* demodulators and from t]Ze output of the 11i{f3
_ inverter in the F.l to E6 adders. As a result, the instability of Che phase
characteristics of the law-~frequency X~1 to Y@6 filter amplifiers, which
~;enerates seismi^. signals in the corresponding cliannels, has no in�luence
on the quality of. rhe detonatj.on noise suppression. -
- Oscillograms are presented in Fi~ 26 ~ahich demonstrate the quality of the
seismic si~nal magnetic recording channel. of the Tayga equipment. `
Ttie seismic recordin~ unit with dynamic recordino range of 60 decibels
- using simple and highly economical tape drives was built for the first time
in the USSR. In addition, it was demonstratEd theoretically and experi-
mentally that the dynamic range of somewhat more than 60 decibels is the
maximum admissible range, for it is then limited to the effect of the ~
spurious amplitude modulation of the pulse sianals reproduced from the
magnetic tape.
~ On the basis of the studies performed, reel-to-reel tape drives have been ~
developed for the seismic recorders of the Tayga equipment with drive from ,
_ the highly economical DC motors with a detonation coefficient no more than
2% permittin~ para11e1 recording of the information from six-channels and
- two auxiliary ones on the tape 12.7 mm wide. The ma~netic tane stored on
t~e reels driven at 9.5 cm/sec provides for successive recording of more
than 10 blasts with 3 to ~S minute recordings of each blast.
�3. Radio Remote Control System
The radio remote control system of th.e Tayga system is designed for perform-
ing the following operations: 1) switching the recorders to the record
_ mode; 2) shaping and recording the Iarge and ar.?all-scale time mark signals;
3) transmission of the blast mark signal to all recorders; 4) disconnection
of the recorder from the record mode and transfer of it to ready.
- As follows from what has been discussed above, the remote control system G
_ of this equipment has been built so that the recorders are switched on by
~ the time mark signals, and they are switched off automatically after cessa-
tion of the transmission of the coded time mark si~aals from the dispatch
station. This has greatly simplif ied the remote control system as a whole
_ and the recorder decoder in particular, which is extremely imnortant, for ,
its economicalness determines the electric power intake in the ready mode.
The coder of the remote control system shapes the time mark signals, the
~ structu.re of which permi.ts reliable tim~ ~riddin~; of the in~o~nat~on
~ recorded by aIl of. tr~e seismic recorders~ The reference noint o~ the time
- mark scale coincides with the blast time. This offers the possib~.lity of
multiple transmission of the blast time mark signal after calibrated time
intervals during one session. The block dia~ram of the coder and the
y struceure cf tha time marks are presented in ~i~ures 27, 28. " .
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a .
_ ~
I m
sr I AQ A5 rr I
r
. ~r ~
- ~ ~ ~
~;r rcnr ~r Kl15. (
I ~ ~
,q2 Kn2 yy ~M ~c I
~ ~
~ Aa Kns ~2 Kna i r~n
l___~,_ ,_-J
. ~ rc paBuonepe6amvuay ~i~
~ I - - - i - - i .
3f A~ A5 A6 I
; ~ I . -
I'
jJ,1 KII1 ' E i ~AT ` �
I I . '
A2 Kn2 ~ .
~ I ~
R 3 ' YJ13 f 2 Kl14 I -
I ~-J_~~- ~
~ rc pa8uonepe8amwuny ~1)
Figure 27. Block diagram of the coder: a-- when operating with
- the blast time mark; b-- when recordinF the "uncontrolled blasts."
sr master oscillator; 1zi -zr.a frequer.tcy dividers;
x,~1-x~~5-- switches; E1, E2 adders; ~T shaping trigper;
YY preset unit; YC clear circuit; ~r~ blast tiMe pulse -
- shaping circuit; MlI time loop.
Key: ~
1. to the radio transmitter
T~,e coder- is ma.de �un of. three basi.c modules; tl~e module for shap~ng the
subcarrier ~requencies - I-;~ siiaping the mark~ng frequencies II, and
shaping the time mark structure TTT.
~ 79
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a
7M~a15~20~25~J0 T TM T TM2
i . .
- ' .
~ ~~f
; i ~ Mo,~teHm e3pbraa
. ~
20c
T~ 4c 1c 3C 2C 2C 3C !c 4C
. . . . . . .
-
~f~ ~PQ ~~J
Figure 28. Structure of the time mark signals at the input
of the radio transmitter and shape of the time
- mark re~ording on the seismogram
a-- when ~aorkin~ with the blast time mark; b-- when recording _
"uncontrolled blasts."
Key:
1. blast time
The quartz-stabilized master oscillator of the coder ~enerates a signal of
siiff iciently hi~h frequency which is simultaneously fed to the D1, D2 and D3
dividers which generate the subcarrier frequency signals fl, f2, f3 and
the dividers D4, D5, which shape the marking frequency signals. The sub-
carrier frequencies fl, f2, and f3 are located in the radio telephone
channel band of 0.3 to 3.0 kilohertz. The oscillation periods of the marking
frequencies T,~;, and T;~? have values �rom the following series: T~=30 milli-
seconds, 25 milliseconc~s, 20 milliseconds, 15 milliseconds and TM2=1.5 seconds;,
1 second and 0.75 seconds. Every set of equipment has its own combination _
~f values of subcarrier and marking �requencies. These values are estab-
lished by replacin~ the division coef~icients D1, D2, D3, D4, and D5.
- The shaping of the time mark signals is realized by module III in the
following way. At the time the coder is scaitched on by the preset unit (YY)
the shapina trig,ger (~T) is set to the position where the switch I{JI1
is closed, and the switch ~~JI2 is open~ For a closed time loop (MTi) the
blast time pulse shapin~ circuit (~P!) keeps,HJIS in the open position.
~he subcarrier frequency signal fl ~oes through I~JI1 and the adder E1 to
the input ofI~JI4, and the subcarrier ~requency signal f3 is fed to the
inPut of the IfJi3 . The I{JI3 and K,n4 switches are altesnately closed ~
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I
~ox orrr.c,r.Ar, crsr ~~rrt.Y
by the signalG which cor.i~ f.rom the o~posite arms of the output trigger of
the D4 fxequency divider, at the same t~.me maniPulating the subcarrier
' �requencies fl and f~ at the innizt o� the adder ~;2., the ~~;tnur ~C .~�~hi.ch ~is
connected to the input of tlie radio transmitter, Thus, the frequency
maniPul.~ted si~;n~l is radiated i.n~o spZCe befor.e l}~ie b139C time. The kcylnn
frequency of the subcarrier frequencies fl flnd F3 _Ls e~ua1 to tlie marlcin~
frequency f~ which determines the scale divisions of L-he f1.ne time marlc
scale. The recorders are switched to the record nositj.on by the shaped
signal.
At the time of detc~nation of the charae, the time loop ?~21I is broken, and the
state of the ~Pt circuit is switched, ~~hich through the YC initializes D4 and
D5, changing the state of the shaning trigger ~T so that OCJ~i opens and }{,n2.
_ closes. Simultaneously, the ~i4 circuit closes . As a result, from
- the time o~ the blast the .feed of the suhcarrier ~requency ~'ip,nal fl ceases,
and the si~nal of the subcar.rier �requency f2 be~ins to go through the pC,n 2
and the adder El to the input of the `}~(J(~ e rlow the marlcing f-requency sigr~al
fl,ql will manipulate the subcarrier frequency f2 and f3 at the input of E2
- using K,jt3 and E(~~,,, The state o� the shapino tria~er ~T does not chan~e
until the first pulse goes to its countin~ innut throu~h from the D5
output, which shapes the signal of the second markinp frec~uency ~M2 giving
the lar~e time scale divisions. Then ~T onerates in~~the counting mode,
mani~ulating the subcarrier frequency fl and f2 at the input of 3;1 usin~
, ~ 1tJ11 and ~(~2. in accordance with the large divisions of the time scale.
Clearin~ il4 and D5 at the blast time aiitomatically ties the reference point
of the ~ime scale to the blast time. This not only creates defined convenience
when processinp the seismograms, but it also increases the noiseproofness
of the transmission and the blast time mark, .for it repeats after calibrated
- intervals in accordance with the large time scale divis3ons. The division
coefficient D4 ar.d D5 are selected so that an inte~;ral number of frequency
neriods fpql will be laid out in one frequency period fp.T2.
If it is impossible to record the blast time by usin~ the time loop, the
structure of the coder shown in Fig 27, b is used. In this case the lar~e
time scale divisions are given as before by manipulation of the subcarrier
frequencies f.l and f2 using the shaping tri~g~r ~6T, which operates tiere
in the mode of separate startin~ of. the outputs of the D5 and D6 dividers
which give the frequencies f~i2 and fM3� I.f we select fr42=1/5 hert.z, and
fM3-1/4 hertz, then the shapin~ trig~er ~T wi11 shlpe the code of the large -
~ time mark divisions with a repetition period o:C 20 seconds as shown in
Fig 28, b. This code permits a unique time coor.dination o~ I:he seismograms
~ for any tyPes of regional seismic opexations,
Thus, in the coder of the remote contro]_ system for t~he Tay~a ec~uipment
it is possible to transmit the blast time mark s:iPnals, the signals of the
large and small tir~e mark scale divisions to ttie observation points and
control the operation of the recorder by manipulating a11 three subcarrier
frequencies.
_ 81
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The decoder of the remote control syatem of the Tayga system is designed
- for isolation of the signals emitted from the dispatch station against the
backpround of various types of signal interf erence, switching the recorder
to the record mode, reduction of the time mark signals to the initial form
~or recordin~ on the ma~netic tape together with the seismic aignals.
'I'iie hlock c: t~~~;rrim of the decoder to~ether with the time mark ai~nal recording
:+yatc~m ~ire ~~rr.r~enlecl in Flg 29.
The signals emitted from the dispatch station are generated as follows.
From the output of the radio receivers PII, the signal goes to the inputs
of three para_llel-included subcarrier frequency filters (~1, ~2 and ~3),
which improve the signai-noise ratio, far the filter pass band (~1, ~2 and
~3) is a total of 300-400 hertz on the --3 decibel level. Then the signal
is rig,idly limited with respect to amplitude by the OI'P Iimiter, and it is
fed sir~ultaneously to the input of threa~such subcarrier frequency filters.
The outputs of ~1 and ~2 are connzcted to the detector ~1, the output ~3,
to D2. The detector Dl passes a,positive halfwave of the signal of the
subcarrier frequencies fl a.nd f2, D2, the negative halfwave of the signal
of the subcarrier frequency fg, performing the function of an inverter.
After summation of the detected signals i.n the E adder, the signal is fed d
to the input of the ~*T1 filter which is tuned to isolate the marking frequency
fpsl. The transmission band of the ~M1 filter is very small (1-2 hert~); -
therefore a sinusoidal signal ot marking frequency is generated at i~ts
output, which is detected by the detector D3 and is fed to the input of the
inte~;rator. On appearance of the signal at the input of the inte~rator,
the voltage at its output increases slowly, reachin~ the response threshold
of the threshold circuit IIY after 10-15 aeconds, which includes the servo
relay L1I', and, in turn, the latter switches the recorder to the record mode.
~ ~r---------------~
~ ~ ~
~ ~q~ E Ra I
an m2 ora ~2 I
~ ~ " I
~ ~3 ~3 A2 � I _
ny
T '
~
I KfIQ Mf Kl11 y~ ~8 i NP I
I f----~
~ ~ ~ ~ ~ ~ _ _ ~ ~ J .
- Figure 29. Block diagram of the decoder and the time mark
racording circuit.
PII radio receiver; D1, D?_, D3 amplitude detector; ~1,
~2, ~3, ~M1 subcarrier and marking frequency filte'ts; O1'P
amplitude li~iter; E--- adder; x-~-- inte~rator; JIY threshold
circuit; IIP servo relay; ~B phase shifter; xnt and xnz
switches; MI' magnetic head; Y~ shaping circuit;
I-- decoder; II time r�~ark recordin; circuit.
82 ?
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The isolated marking frequency signal in the decoded channel turned out to
be out o~ phase with respect to the input signal; tt~cre; ore the piiase shi.f Ler
~B shi~ts the phase of the signal so that the Pulse�fronts of rectangular
shape of the marking frequency formed by the Y~ shaper tvill coincide with
the switchin~ times of the markin;; frec~uencies at the decouer input. The
swjtcheg liJll and ~i,;l~ are al.ternt~tely clo;aed ~~nd openecf, feedin~; the ~uh-
carrier f:requency si~;na.1s f1., CZ or �3 from ~h~ outnut oF the corresporiding
filters to the input of the magnetic head :�IP,
Thus, the shane of the current in the magnetic head corresponds exactly to
the shape of the signal emitted by the dispatcher station. The sequence ~
of described filters realizes the optimal al~;orithm f.or generation of signals
of known shane against a background of random interference to the degree to
which thj.s can be done using the R, L and C-circuits witl~out significant
complication of the field equipment,
~i~ 30 shows the exPerimental c~rve charac~erizing tt~e noiseproofness of
the clecoder. The voltage amplitude of the outnut of the marlcing frequency
filter ~M1 is plotted on the y-axis, the ratio of the effective si~nal
voltage to the ef.fective voltage of the fluctua~ing interference at the
input of the decoder is plotted on the x-axis.
As is obvious, the siqnal amplitude at the output of the ~i~il depends sliQhtly
on the signal-noise ratio at the input o.f the decoder to values of U~/Unoise
- =0.4, and it decreases to the 1eve1 of 0.7 of its maximum value for
Usinnal~Unoise-0.33. The fine line on the 0.4 volt level denotes the
defi~~ed experimental interference amplitude at the outp~it o:E the ~Ml under
the effect o� fluctuation interference on the decoder input. The dash-dot
line on the 0.5 volt level denotes the experimentally determined value of
the interference amnlitude at the output of ~M1 under the effect of the
most dangerous nulse interference on the input of the decoder: namely, the
pulse interfer.ence was s~mulated by a plane of pulsed si~nals with repetition
frequency of the marking frequency of f~,ql, off-duty factor of 2, where the
pulse was made up of the sum of the si~nals of three subcarrier frequencies
fl, f` and f3 of idential amplitude. 7'he interference of the more dangerous
type in practice is not encountered.
The theoretical estimate of the probability of false responses in the
presence at the �ilter output ~ril of an inertialle~s threshold device with
response threshold of 2.1 volts ~ives a value of 10"13 [13], which is
unconditionally entirely suf.ficient, for the r.ela.abil.:i.ty o~ the structural
desi~n of the recorder as a whole will be appreciably worse.
The integrator I~I between ~r11 and the threshold ci~~cuit ]IY is introduce~3
for reduction of the probab3,lity of t}te sunpression of the signal by the
pulsed interference. ~rom the operatin~ conditions of the seismic recorder
it follows that even brief disconnect~,on of the tape drive is inadmissible
during recordin~. If at the filter outnut ~PZl there is an lnertialless
threshold device any time at an interPerence pulse exceeds the effective
signal voltage of the innut of the decoder even for a short time so much
83
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~eaz QHt ;1)
lHO~om!
a ---r------------
I
- ~nop'2,18 _
P ~
~ ~ I(:,) C4)
' ~ ~ UM. uf;n ~ 0,5 B. U~u.q~nyKm=Q4 9
~ T~
, Q2 0,4 0,6 0,8 !,0 1,2 l+
_ ~x
Fi~ure 30. Voltage at the output of the marking frequency _
filter of the decoder as a function of the signal-
noise ratio at its input
Key:
1� uoutput~volts) 4. Ufluctuation 0.4 volts -
3. Uthresh815 voltsolts
pulse
that the voltage at the oubput of the filter ~M1 drops below the response
threshold PY, the recorder will disconnect. The probability of such cases,
which is very high as a result of the effect of atmospheric interf erence .
and signals from outside radio stations, will become insignificant when the
integrator is included at the PY input. When the voltage at the outvut of
~M1 as a result of signal supnression by the interference drops below the
value corresponding to the response threshold of IIY, the voltage at the output
of the integrator be~ins to decrease slowly, gradually approaching the
response threshold of IIY, that is, quick disconnectian of the recorder does
not take nlace. If the interference was brief, then the voltage of the
output of the integrator will be restored.
The theoretical estimate of the nrobability of suppression of the si~nal by
_ fluctuating noise indica.tes that if we admit the possibility of disconnecting
the recorder when suppressin~ the signal for more than one second (this
condition determines the time constant of the inte~rator), the probability
of disconnecting the recorder will be auite low. However, the ~ost real
danger is presented by the pulse atmosnheric interference; therefore the
val~~te of the time canstant of the integrator H must be such that the
recorder will disconnect no ~aster than 3 to 5 seconds after suppression of
the signal. The introduction o~ the intzgrator decreases the probability
pulse responses, 4Then develop3.ng the radio remote control system ~or the
Tayga equipmentt the following rest~lts are achieved.
1. The nroblem of insuring autonoz~ous oneration of the seismic recorders
after installation at the observation points is solved.
2. The coder of the disvatch station of the equipment has been developed
which will insure reliable control of the operation oP autonomous seismic
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r~>corderti, tl�~ certified time coordin~tion o~ tl~e recordinns obt~inecl by
tl~e c1l5tributc~d recorciers, recording of. the seismic oscillations excited
hy tl~~ "uncontrolled" sources (industrial explosions, atr bombs), trans-
- mi~sion of: tl~e blast time mark sip,nals and tiie time marks by u hi~hly
reliahle method.
3. A his~hly economical system has been developed for the receiving channel
of the remote control system insuring hi~;h noiseproofness of it;
The decoder permits realization of a reliable remote control o� the operation
of the seismic recorders when the signal at the output of the radio r.eceiver
is hardly heard against the noise background, that is, when the operative
telephone communications betcaeen the dispatch station and the observation
point in practice is impossible;
- The system for generating time mark signals insures reliable time marking of
the seisr~oarams obtained;
- The tests of the remote control channel have demonstrated that for various
noise levels at the input of its receiving channel spontaneous inclusion
of the r.ecorder does not take place (including under the effect of powerful
atmospheric interference).
Structural Design and Tasic Technical Characteristics of the Tayga
Equipment
As a r.esult of the described studies in the field test of. the model, the
2xp, and the second, ~or L~2x~.
In the case of refracted (head) waves ~or the construction of the boundary
and detertiination of the boundary velocity over the entire profile it is
necessary to have direct and counter summary hodographs tied at mutual ~
points. This system is realized for several direct and inverse correlation -
paths havin~ no less than one common point. Let us limit ourselves to tyino
the paths in one direction by the criterion of parall~lnes~.o� the over-
lapping hodographs when the position of the binding counter path is not
required for construction of the swmnary hodo~raph. The conditions of .
economicalness of the observation system are the same as for the re~lected
waves. The observation systems of the refracted waves for the cases of
L>xp and L,xp (Fig 62, d, e) have common receivers for the direct and
return paths.
The following expressions were obtained in refexence [61] for determination
of the number of sources (qn~ i.n the ~.nvestlgated cont~tnuous observation
systems. .
Tn the case of reflected waves
- zo
L.> 2x
~ L 4 OL' ror o,
3zo - - zo 2 ' 1, ~
4n= OL2 c1G 2 2 2z~LL-1,ror~ L xo, -
3xo-~-L_I-zo-~
4n - AG ~L 2 I ~ 2 S QG I' - 1, fo?: L G xa.
(V.2 ) ~
, z �s ox_
I
~ I
I ~
_ y2 I -
f~
va a
- ~ ,
P �x 9 ~ �x- ti
~ r
s P �x ~ d 4 ~i- b
l
iv
~ . i ~
_ x p o. q o~ ~_D -
' I
l (
~ ~v
._a
_ . a p �a a p 9 D
I
~ I ~
' ~ I
I
iv
D
~ Figure 62. Schematic of cqnt~,nuous (a, b~ c, d) and
snot (e) observations,
Trom the summary it follows that tlie number of sources is determined by
the values o~ the ratios ~~/L and L/~L (Fig 63, a).
The number of seismic recordings (Sn) ~n the investigated cont~.nuous
observation systems in the case o~ reflected waves is I6~~:
s- 4x" eL 1 (V~ 3)
n AL(Oz+
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wliere /~x is the seismic channel step size. -
'Tl~e numher of record~.n~;s j.n the case o~ refracted waves considering elongated -
ovcrl~7pping hodop,raptis wlll be
4xn ~~L ' 1~ `L ~ L 1~ f ' (V.!!) -
Sn ` ~L ~x T + ~G - ~x -
where f is the exte~lt of the ove~-lap section of the over].appin~ hod~graph,
Sounding S}~stems. Tn order to construct the seismic boundary (reflecting
or refracting) and for detei-mination of velocities in the medium it is
necessary to have cwo isolines of the time field over the entire profile.
By the observed values of the times on any isoline the depth o~ occurrence
of the seismic boundary can be found. Therefore in order to insure the -
required density (d) for determination of the depths it is sufficient that
on each isoline the times will be found every 2d interval. The substantiated
density of the calculation points for the velocities will be half as much.
The observation density obviously must not contradict the reliability
conditions of the discrete correlation. Usually this contradiction is not
obtained inasmuch as the decrease in detail of the investi~;ations, the
requirements on the accuracy of the wave correlation are reduced simultaneously.
_ ~n b
~d
!0
8
6 ~
~o
4 ~ 1(>21
%n Q ~ 0~75(f 5) _
4ro - - - - - 2 O,SU,O) .
dL ~ ~ ~ 0,25(0~5)
I I O,s 0
~ ~ ~ I 0,8 ~
~ 04 ~
- 2x I ~ ~ ~ ~
dL ~ 2 ~ ~ 0~2 ~ ~
o ~
dL I I ~ 0~f25 0,25
0, >
~ ~0 2xo ~ o,o~ qo2 o,oa o,~ 0,2 o,a qs ~
e~ . a~ �L a~ . E
~~,qure 63. Compar~.son of the labor consumpt:lon o~ continuous
spot observa,tions~
a-,^ ratio o~ the number of sources in the continuous abservation
sy~stems by refracted (.1) and reflected (2~ wavesi b---~ comparison
of the number of sources for continuous and spot observationa;
_ c; the values oi' L/xp are ~3.ven in parentheses Por the reflected
waves), _
_ 166
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_i
The requirement of economicalness of the sounding system usually reduces to
- the minimum nt~mber of source; it is also not necessary to set off repeated
blasts at each point. These requirements are satisf ied if each source is
made common for four sounclings. ShiPting the source along the proCi.te wi.tli
; A mean steP aize 2d, we ohtzin the rec~u~red ob9ervr~~ion rlent;~ity.
i The sounding system for the reflected and refracted wave~ corresponding to
~ the discussed conditions is presented in Fig 62, c. The numUer of sources
in this system will be
j _ 9a = L~ a-I- 1~. ( V.5) .
, ,
The number of seismic recordings (Sd) will be determined, assuming that each
sounding contains a devica with n channels (usually n=6).
~
Sd = 2n ( -I-1~ (V.6)
~
~ Comparison of the Continuous Observat~,n and Sounding Systems. Let us find `
I the magnitude of the ratio of the numlar of sources in the sysr_~s. In the
case of reflected waves using formulas (V.1) and (V.5), we oUtain
Q=` = Z~~r ~-f- I- ~1 f 1 iS ~V.7~
qd (x~ 5) .
or neglecting the small values cF 8/x~ and ~L~x~,
Qn ~J J., 1
N ~ ;
~4a ~ ~ol� ~~'~,7~~
In the case of refracted waves, using forr.iulas (V.2) and (V.5), we find: _
~ n_~02 ~ b r3zn~, L_ I- x~ I, i I_ 1~.
1 OL - Z 2 , (V.B~
d
88 L ~ x~~
9~ ~ o I x I/- A/.S f L �
3 - - 1 -
a t~ eG r1 so l, fox L< xo� (V.8')
l /
_ In both cases (reflected and refracted waves) the ratio qn/q~ depends on _
the values of b/~L and L/xp . Tn the coord~,nate system c~n~qd~ 2Q~pL~ on
' the double logarithmic scale this function ~.s depicted ~.n the form of
~ a family of parallel straiQht lines w3.th the parameter L~xp (see F;ig 63, b).
The ratio of the number o~ sources tn the continuous observation and seisr~ic
systems increases with an ~,ncrease in the values of B~aL and L/x~~ k'or
d/~L>0~25 and ~or any values o~ the parameter L~xp~ the sound~ng systiem
will contain fewer sources (qn/qd>1~~ When d~OL sur�ace. For t:his puxpose l.et us select
the corresponding sections on tlie south end o.f. tl~e Irtysh tr:~verse and o~l
- t~e I:han~y-t~ansiysk-Kolpashevo-': omsk traverse. 'Che r. ef er.ence points o f- L-hc
depths will be selected every 50 kr.i.
The correlation grap:isfor the depths of occurrence for the I, II ancl M
boundaries are presented in Fig 78. It is demonstrated thnt the depths to
the ~ boundary differ little at all points. Between the deprhs 111 and hpq
. and also hII and hri there are quite close mutual correlations (see Fig 78, b,
_ c). The correlation coefficients (r) are equal to -0.34 and -0.79 -
= respectively; the mean square devi~ '~or~ (a) fro~n the re~ression "lines are
+l.l and +1.8 km. The increase in depths hp2 corresponds to a decrease in
the value of hI and hli, that is, the inversion rela~ion is establ.ished for
the ~orr~s of. the surface relief of the mantle with the higher-J,yin~ boundaries
inside the consolidated crust. The dc~ths of the boundaries I and II
(Fig 7, d) are related by a direct c~i-relation (r=+0.79, Q=+J...9 Icm), that
~s, these surfaces occur in general matched.
- � hl,x,H b~
8 ~o
0 00
h~'~ 6 � o
4 0~ ~p o o ~
-o---~-a---o o 0
2 � 4 � � o
o �
~ 34 36 38 40 42 44 I1~M KM 234 36 38 40 42 4Q hM,K.k
:c ~
n~n~ o o �
- 26 �
~ o0 0
a o
24 ~
0
e
2~ ~p � o �oo
0l5 0 -
20 ,
0
o � o 0
'!8
a o0
16 �
34 36 3B 40 42 44 hM,xM 0 2 4 6 8 10 h~,K~f
' Figure 78. Correlation graphs of the depths of occurrence of
~ the sei.sm~,c boundar~.es (,i.nside of the [Jestern
' Siberian nlat~orm)
, 197
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I.et ~is consider the correlations of the thicknesses (H) of the layers
~-I, I-II and II-24 as a function of the *_otal thick.*~ess of the earth's
crust (Fig 79). The thickness o.f, the upper layer (~-I) varies cliscontinuously
from 0 to 2--4.5 km. The zero valuzs correspond to the complete wed~;in~ out
of: the investigated layer and they are coordinated with t}ie sections with
tl~ickened crust (39-44 ~n). The secor~d ~roup of values is characteristic
for the crust 34-38 lcm tl~ick.
The thickness of the second Iayer (I--II) has a weak tend~ncy (r=-0.49) -
tocaard some decrease with an increase in thickness of the crust (see F~g, 79,b).
The mean square deviations from the mean value (~15 km) is +2 lan, that is,
the thickness of the layer is relatively sustained.
A very close relation is established between the thickness of the lower layer
(II-M) itselr and the total thickness of the crust (r=0.94, a=+1.8 km).
The thickening and thinnin~ of the entire earth's crust in its lower layer
coincides (see Fig 79, c). As a result of the inversion relation of the
relief of the II and P4 surfacea, the thickness of the layer bounded by them
is most invariant. The total scale of its oscillations is approximately _
2 tiMes more than for the entire thickness of the earth's crust and it exceeds
by 3 to 4 times the variations for any other layer.
Thus, in the internal part of the Western Siberian platform with relatively
sustained thickness of the sedimentary mantle there are inverse (inversion)
relations of the depths of occurrence of the surface of the mantle with the
higher-lying boundaries oi the consolidated crust. The most inconstant is
- tre thickness of the lower layer of the earth's crust, and its thickness
- varies in general in accordance with the variation in thickness of the entire
crust, but with approximately twice the amplitude.
H _ ~w � H,w-l~~~N c o
~ o
6 0
~ 24 0
o~
0 0
2 0
zo ~
~ J4 d8 4z hM~xH
JI _ RM b ~ '
I! Il
10 o J6 0�~
o ' �o
0
~ o
f6 0 ~ o � 12. `~jO
wo~,~,o 0
~ ~
00 ~
8
1f
~ 38 '~2 I7M~KM 8~ ~8 2 hM~KM
Figure 79.. Correlation graphs for thicknesses of the layers of =
the earth's crust (the insi~e nart of the `~estern
. Siberian platform)
198 �
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The relations for the lateral zone o.f the Western Siber~an platform, that is,
for the sections of transition to the mountairi frame, are important in
_ connecrion with the discovery o� the causes of f.ormaticr~ of an enormous _
depression in the territory o.f the Western Siberi.an lowland,
It was demonstrated above that on makinp, the tr.ansitior~ from the exposed areas
to the inside sections of the platform, a reduction in thicl~ness of tile
_ entire earth's crust takes place, especially its consoJ.i~lated series. Let us
consider what changes occur inside the crust in tl~i.s case.
The variation in thickness of the layers of the earth's crust !.n the section
~ of articulation caith the exposed Tom'--Koiyvanslcaya foJ.c~e-] zone in the vicinity
of Tomsk consists in the following (see Fig 71). For su~mersion of the
~ boundary from the level of the day surface to a depth of 3 km, the Lhick-
ness of the upper layer of the consolidated crust boundel by the ~ and II
surfaces (the I boundary was not es..~blished in the investip;ated section),
remains,:,.in practice, invariant, for the ~ and II boundaries occur matched. -
The thickness of the locaer layer (II-NI) decreases re~ul-~.rly from the exposed
nart to the inside zone of Ehe platfo~-m. The reduction in thickness of thi.s
layer is about 6 km and within the li irs of accuracy of the initial data
- coincide with the decrease in thiclcness of the consolidated crust (the
~-ri layer). Consequently, the variation in thickness of the consolidated
crust takes place wholl_y as a result of its lower section. The buildup of
the layer of the platform sediments to 3 km only half compensates f_or this
effect; therefore the total thickness of the earth's crust decreases in the
direction of the internr~l zone nf the platform.
The variations of the deep strt~~ture close to the ones discussed above are
also visible in the schematized section throu~h the Sverdlovsk intersection
(see Fig 67). The eastern submersion of the surface of the exposed folded
rock in the Urals is accompanied by a reduction in thickness of the earth's
crust basically as a result of its lower layer. On the nrofiles to the south
of Barabinsk (see Fi~ 68) and in section adjacent to ~iorthern I:azakhstan
~ (see Fig 70), the thickness of the crust is also reduced in the direct:ion of
- the submerged pa~t of the platform; the upper layers occur almost matched,
with an increase in depth, inversion of the structural forms takes place.
The discussed characteristics of the relation of the sei.smic boundaries at
different depths make it possible to propose the probable cause of formation
of the broad riesozoic-Cenozoic depress~.on made by sedimentary rock in the
territory of the ?destern S~.berian plat~orm~ The ~~ohorovj.cic di~continuity
~ and series of deep boundari,es 3.nside the earth~s crustt ~.n the opinion of
~ the ma~or~,ty of researchers [14~ 125, and so on]~ are s~condary and super-
posed. During the course of geolo~;ical development, the displacement of
; these boundaries to other hypsometr~.c levels and the variation of their
~ shapes a,re ~ossible~ The cause can he reconstructi;on o~ the lower part of
the earth~s crust zn the territory of the modexn depression. The Mohorovicic -
discont~.nuity and the boundaries of the lower part of ~he crust were
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shitted to liiglier Ievels. As a result, the rock density incxeased in th~
trans~ormeG part oF the section, and tl~e isostatic equilibrium of the broad
territory was disturbed. This led to gradual downwarnin~ of the earth's crust
o~~er an enormous area accompanied by fillin~ of the depression formed by sed-
_ iment. 4
The inversion relation existinR at the present time for tt~e relief of the
upner and lower boundaries of the cr~st can b e explained '.~y the fact that the
amp litude of the de*~ression was ?ess by comparison with the initial disnlace-
ment oP the loiaer horizons upward along the section. ror this reason, the
thickness of the earth's crust remained diminished. The total maQnitude of
the ascendin~ displacement of the Alohorovicic c;iscontinuity can be anproximately
determined bv the difference in thicknesscs of the consolidated crust ~aithin
the limits o.f the '�Iestern Siberian platform and in its mountain framin~
regions which is on the average equal to 10 l:m.
~ xhe basic results of. analyzing the structural peculiaritles and the properties
of the consolicated earth's crust in [destern Siberia at different de~ths ~
consisted in the followin~.
1. ^he variability o.f the denths of occurr~nce of the ~eismic boundaries and
the thicknesses of the layers cf the earth's crust, as rule, increases,
with depth. The nonunifor~nity of the natural distribution of the elastic
wave velocities decreases sharply with an increase in depth only in tlie very
upper part of the section (Uetween the ~ and I boundaries). The deeper zones
~ of the earth's crust, if lirzited to the investigation of nonuniformities
w~th horizontal dimensions of more than 100 km obviously do not differ
si~nificantly from the upper part of the mantle with resnect to degree of
homogeneity of the elastic nroperties.
2. The common relation for the entire territory is the inverse relation
between depths to the basement surface and the ?'Iohorovicic diseontinuity.
The broad denression of the []estern Siberian platfor~ which in the investigated
area over the basement surf ace has amplitude of about 4 km, corresponds to
uplift of the surface of the mantle with almost double amplitude and reduction
of the thickness of the consolidated crust on the avera~e by 10 km with respect
to the folded framing re~;ions. In the majority of. cases, the inversion rela-
tion of the relief o~ the mantle sur~ace and the higher-lying boundaries in
the consolidated crust is noted.
3. The thickness of the lowex ~"basalt~.c") layer is most inconstant and
varies in accordance with the thickness of the entire earth~s crust. However,
the thicknesses of the layers o~ the u~per (~'~ranite" and "sedimentary") part
of the section frequently vary~ corresnondingly, and the~;r total thickness
Pluctuates by un to 10 km,
4. On the basis of the peculi.arit~.es o~ the variation o~ the deep structure
on makin~ the transition from the mounta3.n frame to the 4Jestern Siberian
platform it appears probable that th.e cause o~ downwarping of the platform
territory during the Mesozoic and Cenozoic A~es was reconstruction of the
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lower part of the earth's crust as a result of the ascending dj_splacement
of the Mohorovicic discontinuity with conversion of part of the crustal rock
to mantle r~aterial. The disturbance of the isostati.c equilibrium tliat
occurred led to the formation of a broad, long-lived sedimentary basin over
the area of the modern ~lestern Siberian lowland.
Blnck Structure of the Earth's Crust ir. 'Jestern Siberia .
Isolation of Blocks and Fractures. The followin~ peculiarities leacl to tile _
concept of the block structure of the earth's crust. Over the extended (100 km
or more) sections of the nrofiles the depths of occurrence of the seismic
boundaries, the thickness of the earth's crust, and its dismemberment
vertically, the thicknesses of the individual layers and the elastic wave
velocities vary little. In the narrow zones of articulationof such sections
throu~hout the entire series of cons '.idated crust, all ar the majority of
the mentioned parameters vary sharply. Frequentl~~ these zones are the tracing
boundaries o.f certain seismic surfaces. The amplitucies of the sharp variat~ons
in relie.�`_ of the seismic boundaries (in the form of f.ler:ures or with dis-
continuities) usually are 3-7 km. The thicknesses of the layers can vary ~
still more. ~he discontinuities of the boundary velocity and the basement
su"r�aced reached 0.5-1 km/sec. In eor~e cases the averaQe and stratal veloci-
ties vary noticeably.
The sections with susta?ned dee? struc~.ure are considered as blocks of the
earth's crust. In the articulation zones o` the blocks, in all probability,
lar~;e abyssal fractures have bee developed, many ot which penetrate the
entire thickness o` the crust a~~.~ t?ossibly the tops of the earth's mantle.
The majorit~� of abyssal fracture~ appeared in the ba-avitational and magnetic
fields in the form of extended zones of intense positive ma~netic anomalies,
gravitational "stens" and a change in structure of. the anomalous tields.
This permits more certain isolation of the zones of the probable abyssal
~fractures and tracing of them to si~nificant distances fr.om the seismic
traverses.
Dy the set uE indicated attributes for a significant part of. the T~Iestern
Siberian platform and certain regions of its folded frame, a diagram of the
blocks of the earth's crust was drawn (see Fig 74), ~.~here the larp,e blocks
whicl? appear throu~hout the entire thickness of the earth~s crust and are
delimited by fractures reaching the to~s of the mantle are isolated. At a
number of points, the finer blocki.ng is reflected which caas discovered only
in the uPper part of. the consolidated crust. The intersecting zones of
abyssal fractures in the northwesterly and northeasterl,y directions predominate,
and fractures are noted with almost meridional and latitudinal strikes. -
As a result, an important characteristic of the structure o.f. the earth~s
crust has been traced: the presence of a mosaic system of large an~;ular
: blocks with horizontal d~,mensions of lOQ km or more, Let us briefly character-
' ize the individual blocks.
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The Altaye-Sayan folded renion has been studied by the seismic method in
sections of the Tom'-Kolyvanskaya zone, Salair, the Kuznetsk trouQh and
partially in Gornaya Shoriya. The earth's crust in the Tom'-Kolyvanskaya
folded zone which corresponds to the individualized blocl: I was up to
45-46 km thicker and exceeds the ad~acent b locks by 5 to 7 km with respect
to thickness. The reflectin~ boundary II inside the earth's crust lies
at a depth of about 22 km, that is, 4 km deeper than in :he adjacent part
of tl~e :Jestern Siberian nlatform.
The higher-lying part of the section does not contain clear elongated
boundaries and can in the first anproximation be considered as the gradient
medium with velocity buildup from 5.5 km/sec near the day surface to 6 km/sec
at depths of 3-5 km.
Block 2 corresponds to the exposed part of the Salair anticlinorium and the
adjacent section of the T�?estern Siberian platform. The hlock is bounded by
abyssal fractures 20 km east of Barnaul and at the boundary with the Kuznetsk
trouFh. The inversion relation of the M and II seismic boundaries is
characteristic: the foot of the crust is downwarned to depths of about 40 km,
and the II boundary is unliFted. The uppermost part of the section is made
uP of. rock coith high elastic wave velocity (6.0-6.3 km/sec).
Rlock 3 coincides with the territory of the Kuznetsk trough. The thickness
of the earth's crust is 38-41 km, that is, 5-10 lan less than in the adjacent
mountain reRions, the articulation with which takes place with respect to the
abyssal fracture zones. The refractin~ boundary I in the unper part of the
crust is characterized by variable values of the boundary velocity (5.1-6.5
km/sec) and depths o.f. occurrence (7-1~ lan) in all probability corresponding
to the surface of the intensely metamorphosed f_olded base of the trough.
The structure of the se~imentary series above the I boundary is characterized
by the stratal velocity isolines according to the refracted wave data.
The Yenisey ridge and the western edge of the Siberian platform are inter-
sected by the seismic profile with respect to the latitudinal course of the
Angara River. The Yenisey ridge (block 4) borders with the ~Iestern Siberian
platform along the abyssal fracture. On makin~ the transition to the rid~e,
the thickness of the crust increases from 41 to 47 lan, and the seismic surfaces
I and II cease to be traced. The nropagation rate of the elastic waves in
the upper nart o~ the crust o� the Yenisey rid~e increased (6 kr,i/sec). The
mean velucity in the entire thickness o.f the crust in the meridional direction
is'anproximately 0.2 lcr~/sec more than in the latitudinal direction, which
together with the absence of the sustained boundaries inside the crust probably
~ indicates the latitudinal develo;~r:ent :.n it of submeridional disjunctives
propagated to the depth.
On makino the transition to the western edge of the Siberian platform the
thickness of the earth`s crust decreases smoothly to 38-41 km, and at depths
of 8-15 laa the ref lecting boundary was established which can correspond to
the surface o~ the Archean base of the nlatforr.i.
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_ The tJestern Siberian platform is also broken down into a series o~ l~rge
blocks with different deep structure of the earth~s crust.
The extreme eastern block 5 is located between the Yenisey ridge and a con-
tinuation of the Kuznetsk-Altay zone of abyssal fractures. The thiclcness of.
the crust is increased (to 44--45 km) by comparison coith the acijacent sections
of the platform. At depths of 20-22 kzn, the reslecting boundary II is
traced. The higher refractin~ surface I has a sharply dismembered, oUviously,
block relief (4-11 km) and variable values of the boundar}~ velocity (6.2-6.6
~ km/sec). Obviously this boundary corresponds to the surface oL ~he day _
= crystal basement. The layer between the I and ~ boundaries probaUly is
moderately dislocated, weakly metamorphosed sedimentar; rock from the
Paleozoic discovered in the ~iven reQion by dee~ wells under the rieso-Cenozoic
- nlatform mantle. The inside structure of the eastern block is nonunif.orm.
In the section of the P,aska basin I boundary is down~oarped by 3-4 km,
and the Mohorovicic discontinuity is uplifted to 41 km. In the same sscL-ion
reclucti:on of the values of the boundary velocity is noted at the I surface
and the mean velocity to the II boundar.y. _
Block 6 in the east is bounded by th~ .K.uznetsk-Alray fracture zone, in the
- west, bv the fracture in the vicinity of the mouth of tlle Tym River, and in
the southeast it is articulated ~aith the exnosed Tom'-;lolyvanslcaya zone.
The southwestern continuation of the block has not been investigated. The
thickness of the earth's crust is 37-38 km. The II boundary occurs in the
depth range of 20-22 km. The refractirc~ surface I in the basement has been
established only in two limite~ sections, bein~; the bottom of the basins
with lownwarp amplitude of 3-~. t:m and no more than 100 km across made up of
relatively weakly metamorphoseu rock, Over the remaining territory of the
- block the upper part of the basement is a gradient medium, just as ~vithin the
limits of the Tom'-Kolyvanskaya folded zone.
Blocks 7 and 8 which are sharply detected by the structural peculiarities
have been established correspondin~]yo un the Ob' (the section between the -
villages of Aleksandrovskoye and Ust'-Tym) and the IrtVsh (the vicinity of
Cherlak) traverses. There i~ much in common in the deep strucrure of these
blocks: rock ~~ith high (6.1-6.4 km/sec) elastj.c wave velocity goe~ to the
surface of the 'basement, the earth's crust has a thickness o.f more than 40 icm
and is thickened by 4-8 km with respect to the adjacent sections, The
inversion of the structural forms ~.s clearly exhibited: downwarns with respect
; to the M boundary correspond to upli,fts of the TI and I surfaces. The
western boundar~ o~ both blocks is the Omsk fxacture zone intersecting the
- entire j~7estern Siberian localand. [d~th respect to magnetic field peculiarities,
the block 7 j.s traced to the north to the Arctic Ocean, and block 8, to the =
, rep,ion of exposed structures :in Northern F:azakhstan where it is the uplifted
part of the Caledonian structures. Possibly the invest~~ated blocks ~orm a
s~ngle buried structure extendi,ng sevexal thousands of. k~.lometers 100--200 km
across, which cuts throu~h tfie basic znosaic system of angular tilocks. At
approximately the latitude of ~msk, this structure is disturbed by the
transverse fractures of northwesterly stri~e; the complex structure of the
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earth's crust was discovered here which di�fers from that described
above.
Bl.ocks 9, 10 and 11 4~ere studied alon~ the latitudinal course o.f the Ob'
_ River. The thickness of the crust varies little (36--37 km). The II boundary
rises successively From block to U1.ock from 2.5-26 km in the west to ?_1 km in
the east. The ref.rac~ing boundary I with sustained deptt~s of occurrence
(6-8 lan) and a houndary velocity of 6.2-6.4 lcm/sec has been established in -
a11 the blocks. The velc~~ity at the surface of the basement is somewhat
locvered, and it varies 1 ittle (5. ?.-5. 6 km/sec) .
- Rlock 17_ is boiinded on ~he south by the sublatitudinal fracture in the
vicinity of. Tobol'sk, and it;is traced to the north to Khanty-Mansiysk. Gn
making the transition through the southern fracture, the structure of. the
unper part of the consolidated crust (see Fig 74) and the nature of the
- recordings of the elastic waves from the M boundary vary. The thickness of -
the crust o.f the block is ec~ual to 35-36 km. The reflecting boundary II is
noted only in its northern half at depths of ??.-23 km. The upper part o� the ~
consolidated crust is nonuniform: the boundary velocity on the basement
surface varies from 5 to 6 lcm/sec, and the depths of occurrence at the
~ refracting boundary in the body of the basement are sharply variable _
(4-10 ~:r1) . Signif icant diff erences in the structure of. the upper part of
the consoliclated crust do not permit joining of. this block with the block
adjacent to it to the east of Khanty-rlansiysk.
P,lock 13 was established in the central part of the Irtysh traverse; in the
southeast it is adjacent to the Omsk fracture zone and is divided into the
eastern and western parts bounded by the fracture which appeared only in the
upper part of the crust. In the east, the velocities at the basement surface
are reduced (5.4 lan/sec), and at depths of 5-8 km the refracted boundary I -
occurs. In the west the I boundary does not exist, the velocity at the ~
basement surface is high 6.(3 to 6.1 km/sec. The seismic boundary I in the
eastern section o.bviously cor.responds to the bottom of the large (with an
amnlitude of up to 5 km) downwarp in the basement f ill~d with relatively
weakly metamorphosed sedimentary rock. The mantle surface is submerged by
35-38 km. The velocity buildup with a depth in the rock of the mantle
obviously takes place appreciably more slowly than in other sections.
In the vicinity of Omsk, block 14 has min~mum thickness o~ the earth~s crust
32 to 34 irni for the ent~re investigated territory. The upper part of
the basement is made up of rock with low elastic wave velocity (5.1 to
_ 5.4 km/sec). Ins3.de the crust two boundaxies have been establ~.shed;
reflecting at a deptfi oP 27 lan and refra.cti,n~ at the 6-7 km level.
The peculi,a~ities of the velocity distribut~.on connected with the block
" structure of the earth's crust? ~.n addi.tion to the nrocedural signi~icance, ~
are imnortant as valuable in~ormat~,on ahout the propexties of the deep
structures ~�~ithin tfie limits of the inhomogeneous blocks.
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Initiall} we shall consider the resultant data on the mean velocity obtained
by the corresnonding recalculation [115] of the e.f.fective velocities
determined by the reflected and refracted ~aaves. Fig ~0 shows. the mean -
velocity as a function of depth v(h) for standarci blocks. Tt~e ~raphs per-
~ tain only to the consolidated crust. The ori~in of the coordinates for ttie
depths is matched with the ~ boundary which in the exposecl regi.ons coin-
cides with the day surface
By the functions v(h) the blocks with dif:ferent sL-ructw-e of the tops of
; the consolidated crust are most sharply distinguished. The bloclcs for whicl~
the high-velocity (6.0-6.4 km/sec) roclc reaches the ~ bo~~ndary are
characterized by the largest values of the mean velocity an~ the ntinimum
values of its vertical gradient (see Fie 80, 1). In the mountain frame,
they include the section of the Salair rid~e, within the limits of the
Western Siberian platform, blocks % 3 and others denoted. by the dotted ]_ine
~ in the diagram (see Fiu 74).
_
~~r.M/c
~ .i 6 7
. ~ 3 2 1
20
i
_ I
- 40
Il~ KM
Figure 80. Characteristic oraphs of the average velocity in
the consolidated crust as a function of depth:
1-- in block 7(the Tdestern Siberian platEorm); 7_ in the
blocks of the 4lestern Siberian platform containing a series of _
low-speed rock under the ~ boundary; 3--- within the limits of
the Kuznetsk trough~
Key: _ ~ -
1. v, km/sec
The blocks which are wides~re~d ~in the terr~.tory o~ the plat~orm with a
layer of relatively low-~speed ~5,0~5~7 km~sec) rock bounded by the ~ and I
sur~aces axe characterized by lowex values o~ the mean veloc~.ty at all
depths and higher vertical velqc~ty gx'adient (~'i.g 30~ 2), The noted
peculiarities o� the function v(h) are still more sharply ~rian~.fested ~or the
block corresponding to the Kuznetsk trough (X'i~ 80~ 3)~ Here the upper
layer has a very great thi.ckness (about 10 lan), and the velocities are sti11
lower. The latter obviously is basically caused by~ the absence of the
compression effect within the limits of the platform as a result of the
i Chick platform mantle.
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Th~e separation of the consolidated crust into the "granite" and "basaltic" _
part is widesnread. This provisional provision by the geophysical data
permits approximate determination of the large differences in the petro-
- graPhic composition of the crust in different sections inasmuch as the
rock of basic (basaltic layer) and acid (~ranite layer) composition is
characterized hy dif.ferent velocities and densities. Th~ traditional
separaCion of ehe indicated layers by the deep seismic sounding data
reduces to the fact that one of the intracrustal seismic boundaries is taken
as the so-called Conrad surface separating these layers. This choice
usually is provisional: for detailed seismic studies several discontinuities
which are similar ~uith respect to their properties have been often estab-
lished, and the stratal velocities in the isolated layers do not remain
constant. All this leads to significant difficulties and ar~bl.guity in the
comparison of the various blocks with resnect to thicknesses of the granite
and basaltic layers with traditional isolation of them.
Below, another anproach is used to the separation of the consolidated crust
- into two provisional layers. In the lower (basaltic) layer the velocity is
assumed to be constant and equal to 6.8 km/sec. The higher-lying part of the
crust to the ~ boundary is joined to the upper ("granite") layer. The
' velocities in it are taken equal to 6.4 lan/sec belo~a the I boundary, and in
the interval between the ~ and T boundaries, in accordance with the actual
data for the investi~ated section of the nrofile. Knowinp, the thickness of
the entire consoliciated crust and the mean velocity in it, it is possible to
- calculate the value of the ratio of the powers (a) of the upper and lower
layers. The absolute value of ~ denends on the selection of the velocity in
= the lower layer, and therefore it is provisional. However, when comparing
these values for different blocks, it is possible to determine the difference
~ of the latter with respect to their "granite" and "basaltic" parts. The
- values of q for l.arge blocks in [destern Siberia were described in the dia~ram
(see Tig 81).
Si~nificant differences of the blocks conn.ected with the deep structure with
respect to ma~;nitud.e of the thickness ratio of the granite and basaltic
layers which varies from 1.1 to 3.3 have been established, The low values
- (2.0-2.6) are characteristic for a large group of blocks (the first group)
with a layer of relatively low~veloci.ty rock under the ~ boundary. The min-
imum value of q=1.1 is charactex'~sti,c of the Kuznetsk trou~h where this layer
has maximum thickness, For the blocks o~ th~s group~ decreased thickness
of. the crust by comparison w3,th the ad~acent sections is also characteristic.
The hi~h values of q=3. 0-3, 3. were obtai.ned ~ox the second grou~ of blocks
with h~,gh (6.1-6.4 lan~sec~ veloc~ty~ on the ~ surface. k'or the ma~ority of
such blocks, the total thickness o~ the earth~s crust is relatively
increased (Salair and Y'enisey rzdges~ blocks 7 and 8 in the Z~lestern Siberian
plat~orm). The noted peculiariti,es ax'e explained by the characteristic
- sections through the di�Perent ty~pe blocks (Fi~ 82): in the blocks of the
first ~roup the provisional "basaltic" layer is thicker, and its surface
has a grown-over form with respect to the intracrustal boundaries.
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I u / u ii
I
~ XAMTW-NAMCNi1CK~ 2~~~ II ` Q i' LOORM
(1)
_ ! J 11 ~ AAEKCAHAPOOCKOE
- ~ J,311 ~a a~ '
`a Z>> r~~ /~l ~,5~~ 215 \~\CHN~.C~CK 3
~ 070 0 bCK tlO// ~ OS e`\~ JjO~
~ - ~ ~ Q s KOA A\\E8D
' I J' 1 2~4 \ /l Q ~
~y. , ~ yl a Z~6 )p\\\~ .
~ @ ~ Q \ ~ riOMCK O ~
' 2 6~ 32~ ?'1~ 2,5 3~ 6 Z
, ii /
i /6\ NWNM 2'2 . 6APA6 OOCCN6NPCK~(
l J t~
OMCK Z 1~9 ``ri~ B`~
i ~ Z,5 ~o~\ ~ Z 3 2,7 4
~ ' ~
L 7 ry/~y es 2~3 \1 ~ 5
~ ~
~ ~ / ~6
. ,
, ~
' ~ O1 ~7
, ~
; Fi~ure 81. Diagram of the t~~ickness ratio oE the granite
and basaltic layers -
1-- deep seismic soundin~ profile; 2-- crustal-mantle
~ fractures (a) and fractures in the tops of the basement (b);
' 3-- abyssal fractures with respect to ;eological data;
, 4-- ratios of the thicknesses of the "granite" and "basaltic"
layer; 5-- numbers - the block; 6-- sections with high
velocity on the bas~ ,.1t surface; 7-- boundary of the folded
frame of the ~destern Siberian platform.
Key:
1. Khanty-Mansiysk 7. Barabinsk
2. Aleksandrovskoye 8. :lovosibirslc
3. Yeniseysk 9. Tomslc
4. Tobol'sk
5. Kolpashevo
6. Ishim
~Let us try to Ui~ae t~;e ~.~s^si,ble~ .Qeo~o~ieal -inter.nr~t~~tian o~ the ~resented
data. The blocks of the first ~roup wi:th an ~.ncrease i,n the ''basaltic"
layer and higher position of the M boundary exnerienced relative subsidence
in the premesozoic time, which was recorded by the formati.on of a layer
between the ~ and I boundaries~ and ~n the Kuznetsk trough, its sedimentary
; execut.ion. The second ~roup of blocks' chaxacreri.zed by thinner "basaltic"
layer and deeper r1 boundar}~t were upl~.fted at the same time~ as a result
~ of which the deep rock with high elastic veloc~,ty reached the ~ surf.ace,
and in the exposed re~ions, the day~ surface, The possible cause of vertical
movements o~ the blocks leading to si~nificant changes in the upper part of
the consolidated crust could be the nonun~.~orm conversion of the lower part
of it to the mantle mater3al, disturbing the equilibrium of. ad~acent blocks.
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In the blocks of ~ne first group this transformation was mani�ested more
strongly; the t~lohorovicic discontinui~~:y turned out to be anpreciably uplifted, -
and the higher-lying rock of the earth's crust increased in wei~ht. The
latter is recorded by increased thickn~'~ss o~ the "basaltic`' layer, the thick-
ness of whicli in this interpretation is~ considered as an index of the degree
of conversioii of the lower part of the crust itself.
Ttie estimation of the isostatic equilibrium of the blocks of the earth's crust
is of interest for determination of the tectonic activitv of the individual
regions of the investi~ated territory. It is known [5, 7, and so on], that
the disturbance of the isostatic equilib,rium can be considered as an indica-
tion of the modern activity of the ~iven section of the earth's crust.
Usually zhe ~tudy of isostasy is made by ~.he ~ravimetric data; there are
examples of using t~rnt ~~a 8~0 -
r ~
~ ~ tl~-8,0 -
h~ KM
. U~=5,5 1~ 2 ~j,il,M 3 h6=1BK ~i ~=6,2 5 �-Cy0 6 C 6Q 7
Fi~ure 82. Charactez~.st;tc sei.sm~c sections w~th prov:isional
"basaltic" lay~er (crasshatched),
1-- boundary veloc~ty~~ lan~sec~ 2-~ abyssal fracture zone;
3-- sei,smic boundazy~ 4~~ thi.ckness o~ the "basalt3,c" layerj
5-- mean velocityt km/'sec7 6-- veloci.ty isolinesi 7~~ numUers
o~ the blocks of the earth~s crust.
Key:
1. E~leksandrovskoye 6~ Barnaul _
2. Us t~--Tym 7~ Us t~~Naryk
3. ~lestern Siber~an plat�orm
4. Salair ridge
, 5. Kuznetsk trough
; 209
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Within the limits of the platform itself the pressure at the selected level
is appreciably more sustainedr it does not go out of the range of 14.47 to
14.62 kbars. The difference ~n va,lues for adjacent blocks exceeds 0.1 kbars
rarely. Let us present comparative data with respect to the tectonically
active region of transition from the Asian continent to the Pacific Ocean
[21]. Here the deviatians from the average pressure are 0.3-0.4 kbars, and
they reach 0.9 kbars for the ICurilo-Kamchatka Arc and the ad~acent deep-water .
trench. The corresponding deviations for the Western Siberian platform
are almost 10 times less. Consequently, it is possible to consider that the
blocks of the earth's crust of the Western Siberian platform are in a condi- _
tion very close to the isostatic equilibrium. The level of pressure compensa- -
tion is located immediately under the mantle surface; therefore the isostasy
of the blocks is caused by the peculiarities of the mass distribution inside
the earth`s crust. Some nonequilibrium is noted in the boundaries with the
re~ions of folded framing of *he Western Siberian platform. Let us formulate
the basic conclusions pertaining to the block structure of the earth's crust
in the territory of ~destern Siberia. -
1. The earth's crust in the Western Siberian platform and adjacent exposed
regions has a mosaic-block structure. Within the limits of each block the
thickness of the crust, its layering, the depths of occurrence of the seismic
boundaries, the thickness of the layers and the elastic wave velocities are
relatively sustained. The blocks have horizontal dimensions from 100 to 200 km
to many hundreds of kilometers, and they are bounded by fracture zones reach-
ing the tops of the mantle. The boundaries of the blocks in the majority of
cases have appeared in the magnetic and gravitational field anomalies, which
has made it possible to interpolate the da'ca to large distances from the
seismic profiles and to obtain a concept of the spatial structure of the
_ earth's crust in a significant area. In the exposed sections the seismic
blocks and fracture zones are a deep continuation of the geological structures
, lcnown near the surface.
2. The ratio of the thicknesses of the nrovisionally isolated "granite" and
"basaltic" layers is in regular relation to the block structure of the
~ region. The "basaltic" layer is thickened in the blocks with a thick layer
of low-velocity rock in the upper part of the basement and with relatively
reduced thickness of the crust. A possible cause of the differentiated
vertical movenents of the blocks 3.n the premesozoic time essentially changing
the structure of the unper part o~ the basement was nonuniform conversion
of the bottom of the crust to mantle material,
3. In sp~te of the s3.gnif~,cant nonuniformit~es in the dee~ structuret the
investigated territory of ~lestexn Siber:~a is in a cond~,t~,on wh~ch ~.s close
to isostatic equilibrium the pressure fluctuations at the compensation
level (.~50 lan) are appreciably lower here than in the tectonically active
- regions. The blocks o� the earthFS~crust w:tth~.n the boundaries of the
Western Siberian plat~orm are tfie closest to equilibrium. Some nonequilibrium
of the platform territory wi,th respect to.;sections of its folded~.'frame is
noted.
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4. The discovered peculiarities of, the block stzucture of the consolidated
crust constitute the basis for more reliable tectonic rep;ionalization of
the basement of ttie ~�Iestern Siberian platform witi~ respect to the entire set
I of geological-geophysical data, which, in addir.ion to independent prospecting
' significance, in accordance with the princi.ple of inheritance o� geoloaical _
; development, is imnortant for discovery of the laws of the tectonics of the
' platform mantle and the re~iunal. variations of the lithologic-�acies
composition of the components o~ its sedj:mentary complexes containing oil
and .g,as deposits.
~
~2. Studies of the Basement o~ the Western Siberian Platform
Information about the structure of the basement is needed for reliable tectonic
regionalization, on which the scientifically substantiated prospective plannin~
of the prospecting for various miner~ls is basecl to a si�nificant de~ree.
Accordingly, it is necessary to note two basic aspecr_s of tlle study of the
basement. ~ .
First, in the near future the require~l increase in oi7. and gas reserves ~aill
~ be realized not by prospecting produc ive complexes of rock in the platform
mantle, but, nossibly, as a result of discovering new oil and gas-bearing
I formations in the more ancient deposits. For the southern nart of the _
I Western Siberian platform, finding Paleozoic oil under the Meso-Cenozoic
~ platform mantle is already now uruent.
i
Seconclly, the study of the base~n~nt presupposes the use o� the principle of
inheritance of the geological ~ elopment of the platform mantle and the
basement. The inheritance is L~~~ clearly manifested in the young platforms,
to which the Western Siberian platform belongs, ~ahere the discontinuity in
time between the formation of the mantle and the postgeosynclinal folc~ing
of its base is relatively small. The regional differences in the structure
and the development of the basement in accordance with the principle of
inheritance can cause si~nificant peculiarities of the tectonic conditions
and the conditions of sediment accumulation of the platfnrm formations,
which are the reservoirs for the oil and gas; ther.efore the tectonic regional-
ization of the basement must be given special attention.
Unril recently, this regional~.zation of the basement of the tJestern Siberian
platform remained to a~reat extent ambiguous~ based primarily on the analysis
of the gravitational and magneti.c anomalies w~.th extrapolation of the layer
established in the mountain frame of the platform, to the internal closed
regions. The role of the most exact geophys~.cal method seismi.c prospecting
was relatively small. The tedious studies l~y the corxelation refracted
wave method ~I~IPV) were bas~cally~ lim~.ted to the local sections and d~.d not
give an idea of the regional structure of the basement, ~
The re~i.onal studies o.f the sur�ace o~ the basement by the sounc?inr nrocedure
in the traverse version were actually carried out along a11 of the navigable
rivers of Western Siber3a in the 1960FS. The total extent of the investi-
- ;ated traverses reaches 15,000 1cm. The rTovosibirsk, Tomsk and Krasnoyarsk
Main AdMinistrations, subdivisions of the Glavtyumen'~eologii Administration, _
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the IGiG Institute of the Siberian Department of the USSR Academy of Sciences, _
and the ZapSibNIGNI Institute participated in the work. In recent years, -
area studies of the basement have been made in the southern parts of
Western Siberia in order to study not only the surface of the pre~urassic
- basement, but also its internal three--dimensional structure to a depth of
up to 10 lun.
A discussion is presented belo~a of the basic results o.f the work in the
Tyumen' Oblast and in the southern part of Idestern Siberia.
~ Studies in Tyumen' Oblast
In this larFest`oil and gas-bearing region the spot sounc~ings by the
refracted wave method (Chapter II, ~4) were used to study the basement sur-
face by the regional traverses (the GlavtyYUnen'geologii crews made about
5,000 km of river traverses, the ZapSibtlIGNI Institute investigated the -
ground traverse alon~ the Tura-Tobol-Irtysh Rivers); small and large-scale
area surveys were made o� the basement surface.
Sounding systems of the B and E type were used (see Fi? 23) with careful
introduction of corrections for the oscillation phase (considering the
characteristi.c features of the form of the wave recording), the depth of
submersion of the explosive charge, the lo~o--velocity zone, the relief and
the displacement of the blast and observation points from a rectilinear
profile. All of this insured increased accuracy of determining the parameters
of the medium on comparison with the drilling data (see �1 of the given
chapter) the error in the depth to the basement surfacd was 2-2.5y. Along
with the depths and boundary velocities, values were determined for the
_ vertical velocity gradient of tha upper part of the basement, usin~ the -
method [78] based on investigation of the nonparallelness of the elements
of the overlapping hodographs.
In addition to the solution of the regional problems, the procedure for
soundin~s by refracted waves was tested to discover the possibility of its
application for finding and preliminary study of the local structures with
respect to the basement surface.
Traverse Regional Studi.es. For characterization of this type of operation,
let us consider the results with respect to the standard Pecherakh-Froly
traverse (Fi,g 83), by the Konda se3,sm~,c crew 46/63 along the Konda and
Irtysh Rivers.
In the western part of the pro�ile (60-~140 lcrt~ the large anticlinal bend
is clearly fixed wh~ch corresponds to the intexsection of the Shaimskiy
- structural nose. The a,mnlitude of the hend ~.s 450~500 meters with a width -
of 80 km; the an~les of d3,p of the w~.ngs are about 40~.
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Then, bettaeen 140 and 170 km of, the profile, an anticlinal bend is noCed
which corresponds to the Bol'she-Tapskiy staell, Its dimensions with respect
to the given intersection are about 30 km, and the amnlitu~e is on the
order of 400 meters. The dip an;le of the ~vestern win~ of. the Tapskiy
- swell is about 1�, and the eastern wing, is si~nificantly steeper, about
3�SO'. [�Jith respect to value of the boundary velocities of 4.2-4.4 km/sec
in this profile interval, the basement is represented by the deposits of
the II structural stage. In the same section of the pro{ile, an increased
vertical velocity gradient is observe3. By the deen drilling data the
- basement in this region is represented by deposits which are standard for
the II structural-tectonic stage and are claasifiable as the Turinslcaya
series.
The Lugovskaya basin which is isolated in the 170-200 ~.m sectior. of the
profile has an extent on the order of 30 km with a magnitude of the downwarn -
:.J of about 300 meters. The din angl~ ,f the eastern and western sides ot the
basin are 2�12' and 3�50', respectively.
The Leushinskiy swell (200-260 km) previously isolated by the TT survey data,
is depicted in the TZ MPV refracted ~~~?.ve section as an anticlinal bend with
a width of 55 km, an amplitude of 70~ meters and dip angles of che wings of
2�10' and 1�10'.
~ast of the Leushinskiy swell, a monocl;nal of submersion of the basement ~
surface to the center of the riansiyskaya basin complicated by positive and
negative structures with horizontal dimensions of 20-30 lan and amplitudes
of several hundreds of ineters noted. In the eastern section of the
traverse, in view of the smali volume of operations, only the order of the
depths to the refracting horizon which experiences a rise from a depth of
3350 to 3207 meters is obtained. The R-1 Frolovskaya well encountered
limestone, from the roofs of which the refractin~ horizon is identified.
41hen comparing the T7. I~LpV refracted wave data with the results of. continuous
profilin~; by the reflected wave method by the river procedure, satisfactory
comparison of the results is observed on the whole. Some divergence of
these data is explained obviously by the incomplete matcliin~ of the MOV
[reflected wave method] and TZ riPV refracted wave profiles in plan vieca.
- In general, by the data from the refx'acted wave method the rep;ional and
local peculiarit~es of the relief o~ the basement surface are depicted more
sharply and ~.n greater contrast than it is possible to determine by the
data o~ the reflected wave method whi.ch, given the denths to the reflecting
horizons in the sediMentary mantle3 gives many peculia.rities o~ the structure
of the section in clear form. The i;~d~,v.~dual details o~ the basement
relief, even small in ma~nitudE, ~i,nd zefTection in the above~lying re~lecting
boundaxi.es, k'or example~ two anti,clinal bends in the vic~,nit~ of the
430 km pro~ile with small horizontal d~splacement are fi.xed to a depth of
2000 meters.
213
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' 214 ~
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- 'Piic timall-scale ~~rea regional operations with the ~;oal of. studyl.n~; the
hasement surf.ace by the TZ riPV procedure were carried out during two field
seasons by cre~as 36/64 and 17/65 on the Khanty~tansiyskiy geophysical trtiGt
in the Khanty-i4ansiyskiy, Sur~utskiy, Konda, 'Jvatskiy and the Tobol'skiy
Rayons. The total survey area in two generalized sections contains 153,00 km2
with an average density one determination of the depth to the basement
surfaces per 2,200 km2. The operations were performed by air.
- Let us present the basic ~eological-geophysical results ~vith respect to the
most interesting area in petroleum-bearing resnects located in the Surguts~:iy
and the Khanty-riansiyskiy Rayons. Here the aeroriagnetic and ~ravimetric
surveys and the aviation seismic soundings by the reflected wave methoci
- were performed, by the materials of which jointly with the results oF the -
detailed work using the reflected wave method and drillin~, the structural
and tectonic diagrams of the Mesozoic-Cenozoic Mantle were compiled. The
~ absence of data on the basement surface served as a basis ior statino the
TZ MPV refracted wave operations, inasmuch as it was recognized that the
clearest rePresentation of the tectonics of the Mesozoic mantle could be
obtained, havino a map of the basement surface available.
A comparison of the results of the TZ P~V surveys with the previous.ly
constructed structural-tectonic map of the basement surface compiled by the
surveys by the reflected ~oave method on a 1:1000000 scale and the gravi-
magnetic data indicates comparison of the majority of structural elements.
- 1?ere the surface relief of the basement according to the refracted wave data
appears in sharper form. The majority of positive structures (the Lyaminskiy .
Arch, the Trom"yeganskiy, Chernorechenskiy and Vyn~apurskiy dome upli.fts) -
correspond to intense positive gravitational fields, although other more
complex relations exist.
- The map of the boundary velocities constructed on the 1:2 500 000 scale gives
defined information about the material composition of the underlying rock.
On the whole the boundary velocity field is divided into two sections. In
the western part of the area, an increased value of the boti~nd~r~- velocity
is~observed. The isoline of 6.3 lan/sec outlines the most uplifted part of
Lyaminskiy arc. Within the lir.iits of the Chernorechenskoye and -
Trom"yeganskoye uplifts the boundary velocity decreases to 4.9-5.1 km/sec.
The vertical velocity gradient was determined by many of the soundings.
The nature of the field ~ is analogous a.n general features to the nature of
the boundary velocity f ield, In the vicinity of the Lyaminskiy arc, the
velocity gradient is r~inimal~ and i,n the most u~li.fted part ~.t is close to
zero. The maximum value of S(0.06--O~G7 l~lan) is noted on the ares of the
Trom"yeganskiy and the Chernorechenskiy domeRtype upli~ts, In the denression
zones o~ tre basement, the velocity ~radi.ent is somewhat less, on the -
order of 0,03-0,04 1/km.
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Tl~e complex interrelation of the various geuphysical fields to the values of
- tlie boundary velocity is discovered. In spite of the small volume of research
that has been performed, some laws are noted. In the onerations territory
it is possible to isolate two zones distinguished by the nature of the geo-
_ physical fields. The first zone corresponding to the Lyaminskiy arc and the
region adjacent to it is characterized by the sign-variable magnetic field, -
tl?e maximum value of vhoundary and the i~?njr~u~va].ue of Zt is possible to
pr.opose tl~at the foundation of this zone is complicated hy monolit~ic rock,
probably, crystalline shales or silicified limestones anc' dolomites
characteristic of the late Baykal geosynclinal complex.
The second zone coincides with the most upl;.fted part of the Sur~utskiy arc
and is characterized by the min;r.?um values of the boundary velocities,
maximum S, quite intense anomalous positive magnetic field and ne~ative
~ravitational anomalies. Obviously, ~aithin the boundaries of the Surgutskiy
arch, the basement is represented by weakly metamorphosed formations of
stage II with the development of effusives of basic comrosition.
The results of these operations indicate the significant prospectiveness of
the develonment of such studies in enormous territories still not covered by
seisr~ic exploration to the north and south of the latitudinal course of ~he
Ob' River. Considering these results, the Glavtyumen'~eologiya Trust and
the Ministry of Geolo~y of the USSR are plannin~; the soundings by the
refracted wave method in 1977--1980 over an area of 150,000 km2. Defined
possibilities are opened up in using such data for interpretation of the
gravitational and r.1a~;netic field anomalies.
The laree-scale prospectinp work by the spot sounnin~ method using refracted
waves was carried out in the Shaimskiy oil-bearing re~ion within the limits =
~f the so-called Shaimskiy structural nose. The worl: was performed during
two summer field seasons by the efforts of the ZapSibNIGNI Institute (1963)
~xnd nroduction crew 44/64 of the Shaimskaya petroleum prospecting expedition
(1964) with the goal of testing the procedures for finding and preliminary
_ study of local structures. Some 292 physical observations were made in an
area of 2650 km2, which Made it possible to compile a structural map of the
surface of the basement on a 1:200000 scale with an isohypse cross section
of 100 meters (see Fig 84).
As a result of the TZ PiPV re~xacted wave operations~ the general re~ional
submersion o~ the basement surface frrn!t southv~est to northeast to a depth
Prom 1600 to 1900 ineters was establi.shed. In the general submersion zone
the structural element of II order ~,s clear the Shaimsk3.y structural nose
previously noted by the data from the gravimagnetic surveys and bounded on
the west, the north and the east by the 1800 r.ieter isohypsea
A number of local order III structures have been i.solated (see rir; S4).
In the southern part of the area the northern periclinal of the Severo--
Teterevskaya structure was discovered. Then to the north the Tolumskoye
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I
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local uplift was discovered and outlined. Zt is brachyanticl:inal jold
extendecl in 1 meridional direction, The dimension of ~he strt~cture
wirh respect to the long axi.s is 1.(1-1?. km, and by thc~ short axis, h-7 lcm.
'I'li~ amplitude oE the uplift w~thin the 13mits of the c.lo:~cd lonn i.::
.1.20 meters. The dePth to the basement surf.ace In che arch part is 1.5~~iO r.~.
The Tolumskoye unlift is separated �rom the Severo-Tetez�evslcaya structurc
by a downwarp.
Plorth of the Tolumsk.aya anticlinal structure, the Semividovskaya local
structure is noted 4~hich has dimensions with respect to the outl.ining
_ isohypse of 1700 meters, 9x6 lan with an amplitude of 5~ meters. Northeast
of the Semividovsko~e uplift is the sma11 (5x2.5 km) Uiact~yanticlinal fold
of the northeastern strike with an amplitude of about a0 meters.
.
The western and eastern wings of the Shaimskiy structural nose are made
up of a number of local bay-like troughs, local depressions and..uplifts. -
In narticular, on the western wing, a small uplifted zone called the
Double Local Structure is noted.
A compa~ison with the detailed axea operations by the reflected wave method
per~ormed after talcing the TZ MPV surveys indicates that even insi~nific~int
structural neculiarities noted in the T7. MPV refracted wave method,
~ essentially only qualitatively find aoo~l confirmation durin~ beachhead
; . onerations. ~The detailed.seismic prospecting operations by the reflected
wave method have confirmed the Severo-Teterevslcaya, Tolumskaya,
i Semividovskaya and the Dvoynaya structures. ~
i
Of course, the constructions by the TZ MPV refracted wave method and by the
area surveys using; the reflected wave method in individual details sor~e-
~ times do not coincide, which is entirely natural in connection with the
~ different observation density for the detailed area surveys by the reflected
~ wave method and the prospecting TZ A1PV refracted wave method.
AEter performing detailed seismic work on the Severo-Teterevskaya and the
~ Tolumskaya structures, prospecting drilling was started leadin~ to the dis-
' covery of two oil fields (Severo-Teterevskoye and iolumskoye). The
drilling results confirm the h3~h accuracy of cletermininp the dep ths to
~ the basement surface by the soundin~ pracedure (see Chapter V, ~l, Table 3).
The presented results indicate that the TZ I~1PV refracted wave method of
_ course cannot replace the reflected ~aave method (the continous profilinQ),
- but even under the cor~plex condit~,ons of the Shaimskiy district the
complexing of these General methods will permit the most ei'ficient selec- -
, tion o~ the areas for prospecting and oiitlinin~ local structures with _
. smaller expenditures o~ time and means, '
i
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�~'A 152`~'T\�,
.o o~1F~: .,r:. :'j 'Y - - � �
_ .~~~+~550 ~52ci'' 7 � ~ ~ ~ ' ~~~y,,~, �
_ o ..4. ' 4 'Op'~ / \ ~ ^ ~ . -~.v
~ o� ~ � g ~ j ~ `+p
~ ~
Figure B4. Com~ar~.son o~ the zesults of the TZ r~.'V refracted
wave method ~a:tth the data ~rom detail seismic proszpecting
b}r the re~lected wave method and drilling
1-- sounding centers :in utili.ch the depths to the surface of the
' foundation are obCained; 2-- outline of tfie petroleum deposits _
by the condition on 1,Tanuary 19677 3, 4-R isolines o~ the Uase-
ment surface with resnect to the data o~ tfie TZ PtPV refracted
. wave metfiod C3~ and by~ the data from the detai.l operations by the
reflected wave method oP the ShaiMSkaya and the K.hanty--tdansiyskaya
, oil prospecting ex~editions (4); 5--- the reconnaissance prospecting
drillfng wells and absolute depths to the crystalline basement.
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Area� Studies of the Internal Structure of the Tia~;ement in the Sotithern _
Par.t of the Idestern Si.berian Plat~orm
These studies were performed by the central comPlex ~eophysical expedition
of the Novosibirsk territor~.al geolo~ical administration joinL-ly with the
IGiG InstiCute of the Siberian Devartment of the USSR l~cademy of Sclences
over an area of. 100,000 kmZ within thc limits of. the Tlovosiblrslc, the Omslc
~ and the Kurg;an Oblasts in connection with the problem of discoverin~; the _
prospects of oil-bearing Paleozoic de~otis [6~f, 113]. 'Phe operations
were basically performed during the siimmer ca9.th mo~or transport~ti.on,
~ The seismic model of the uPper part of the basement an~l the choice of. ihe
re.f.erence waves for the regional area studies are based on the results
- of the traverse operations discussed in the preceding i.tem by the method
of deep seismic sounding and on the experience of studying the bottoms of
the platform mantle by the reflected wave method.
The reflectin~ boundary f, occurr3ng in direct proximity to the fc~ot of
the Mesozoic-Cenozoic platform mantle is traceci by Lhe reflecL-ed wave
method using the ordinary procedure.
The refracting surface ~ is studied in an area sounding networlc with bases .
- of 10-25 lun with averaae density o~ the points of determination of the
depths and the boundary velocity o� 7x7 lun. The discontinuous layer b
(see Fig 73) between the boundaries f and ~ obviously corresponds to the -
sedimentary-vulcanoo;enic rock of Triassic and lower Jurassic age included
by a number o� researchers in the composition of the II structur.al. sta~e.
~ The refracting boundary I is also traced in the area sounding, network. The
sounding bases are 40-60 km, and the spacing between their centers is
I 2-3 tir~es ~reater than when studying the boundary f.. The refracti.ng
' method I supposedly belon~s to the surface of intensely metamorphized
rock of the geosynclinal complex, and the layer c Letween the ~ and I
boundaries for the interpretation which is in need of confirmation by
deep drilling data, can be considered as the 1o~aer (Paleozoic) series of
rock in the structural phase II. The basic prospects of oil-bearinp
Paleozoic in the southern part of the Western SiUerian platform are
connected caith this ser~es. -
The indicated seismic sur~aces and the la,yers~.bounded by them a,re encountered
in various combinations. Sy the set o� data on the con~iguration o~ the
_ seismic boundar~.es and the velocity distribution i:n the med~umz three types '
of seis.mic sections of the basement are isolated which are 'investi~ated
; in detail in the nreceding item (~ee Fig 73)~ .
I The areas with dif~erent types of section are blocks of the basement
separated by almost vertical aby~ssal ~racture zones, The problem of the
area regional sei.sMic studies include the study of the ~ and I reference
boundaries to obtain data on the spatial srructure and properties of the _
basement to depths of about 10 lan with separation and tracing with respect
to the area of different blocks and the cleep fractures separating them.
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1 ~ ' ~
,3A 7npa (1) ' ~
~ ~
~ o ~ 2 ~3
Sp 1
~1
~ ~ta
/
~ e~~ ~ ;
~ ~ ~,~6~ ,
~ 1 ~
\ '
~ o~ 1 ~
J ~ _ J ,
as
. ~ ~~5~ 0 w
.
. ~ ~ ~'S ` ~ o ~ _
� ~ ~ ~ ~ 6u?ic~3 ~ .
~ ~ ~
r~ ~ e~ ~ ( ~ . ~~l
r ~ ~J ~
'~Q~'~ ~`b~~ � 3, `3~ ab ~ ~P's'~ 5
' ~ ~J ' r~� ~
oxac.~5 " ~"r� ~.`4A` ' l.,_'~
~ i ~
_ o``` ~ ~ ~.Q,b
::\`J// M1~
, \ ~ ~ . 111
, . ~ Z
~ ~
. ~n
~ r ,a
Figure 85. Structural nap of the ~ boundary
1-- isohypses, km; 2-- isohypses by the uncertain data and .
3 proposed.
Rey:. .
1. Tara
2. Omsk
3. Barabinsk .
The resultant constructions are presented in the �orm of three maps and
the section explaining them (see k'igures 55--88). The maps obtained contain
the following information, :
1. The relief o~ the re~xact~.ng sux�ace ~ with detail su�ficient for .
determination of the ze~ional stxuctures and the~.x complicating uplifts ~
and troughs with horizontal d~,mens~"ons o~' more than 10 lan. .
2. Area distrtbuti~on o~ the Boundary velocities in the rock underlying
the ~ sur~a,ce. ~ ~
3. TI~e contours of the propa~ation o~ great thicknesses (more than 0.5 km) `
of the layer b between.the boundaries ~ and ~ identif9.ed with the upper
series of sed3.mentary-~vulcanogenic rock o� the intermediate structur.al
stage. -
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~ 4. The thicknesses of the layer c between the ~ .
, . MoyCON(ABCmoan.,CS~ ~
~
' !l/eAe~Oee~u APdnuK ~ S
' %1edNU~ ~ 3uMepu s ~ 80'
~
' AaM6epma ,Qeueuc (AQCm~pv
~
; s ~
� � � ~8~ ~ i
. MuPiroru (CCCP) Z ~
� 1 2 ~9~ (1~
10G'
Figure 102. Diagram of the deep seismic sounding traverses
in the eastern Antarctica
1-- Antarctic stations; 2--- deep seisMic sounding traverses
Key:
1. Novolazarevskaya station (USSR) 9. Mirnyy (USSR)
.2. Sova (Japan) 10. Indian Ocean
3. Molodezhnaya station (USSR)
. 4. Kerp,uelen Islands
5. Mawson station (Australia) -
6. Amery Ice She1f
. 7. Lambert Glacier
- 8. Dav,is (Australia) �
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~
~ ~5)
~opoi Rpuac~o 4apnoaa lUe/le[poeeiu` eednuK 3uMepu 'a 6epet Nn2pud Kpucmedced
~ o C1) ~ao ~o ~ C2) aoo 4oo b 50o C~)
. - ,s-s,a
-�-s,o-s,~. o o ~
10 - srT-6,4
. 6~~_6~~
~ t1~P-6,0-6,1 ~ -5~8-59
o
t1~p-6~1-6~2 o p
_ ~0 ~1~=76-78 o d~p=6,0-6,1
- M ~1~= ~6-)~B ~.~-AI
~J~KM
O 1 ? 2 6,~ 3~ 4 w-~- S .
Figure 103. SeismiG section of the earth's crust in the coastal.
region of Eastern Antarctica
1 and 2-- depths according to the reflected 3nd refracted wave
data; 3-- velocity isolines according to the refracted wave data
(the velocities are given in km/sec); 4-~ zones of proposed -
abyssal fractures; 5-- bottom of the ice
Key:
1. Prince Charles Mountains
2. Amery Ice Shelf
3. Ingrid Christensen Coast
4. Beaver Lake
5. Amery Base ~
6' vmean '
�boundary
Characteristic Features of the Procedure. In order to record the elastic
waves, 12 Tayga recorders were used simultaneously. The recorders were
ad~usted to operate at low temperature. They were placed in special
thermostats with internal heatin~ maintaining an invariant temperature of
about 0�C for 2-3 days.
The equipment was remotely controlled from an aircraft and helicopter,
- where the 150 watt radio transmitter was placed insurin~ reliable remote
switchin~ within a radius of no less than 250--300 km.
The oscillations were introduced by detonating scattered charges weighing _
a total of 1~2,5 tons in lakes 60--100 meters deen.
The seismic observation systems used were similar to those used for opera-
tions in Siberia. In the first phase of the invest~.gations~ parametric
piecewise-,continuous observations were made in th.e distance range of
' 0-220 km from the source. These observat~.ons made it possible to study
the wave picture in the new region and substantiate the subsequent
sounding systems, the bases of which were selected equal to 40-60 km to
i study the intracrustal boundaries and 160~220 Ian' to study the surface of
the mantle by reflected and refracted waves. The recordiri~a of the
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subsurface waves characterized in detail in reference [41] do not diff er
significantly from the standard recordings in the continental re~ions.
The basic sounding traverse about 600 lan long intersected the Amery Ice
Shelf, along which an additional traverse was run.
The results of the investigations are presented in the section (Fig 103)
cutting across the geomorphological elements: the Prince Charles
Piountains, the Amery Ice Shelf under which there is an extended graben,
and Ingrid Christensen Coast.
In the seismic section it is possible quite clearly to distinguish three
block sections, within which the earth's crust is characterized by welded
constancy of the mean and boundary velocities, thickne~ses between
individual intracrustal horizons and depth to the ?fohorovicic discontinuity.
On the surface these blocks coincide with the enur,ierated geomorphological
elements. At the boundaries of the blocks a sharp change takes place in
the thiclrnesses of the layers of the individual seismic boundaries, the
total thickness of the earth~s crust and the velocities, that is, the
articulation of the blocks takes place along abyssal fracture zones
within which there are sharp variations of the seismic characteristics
of the earth's crust. The structure of the earth's crust in the blocks
- appears to be as fol.lows.
Prince Charles Mountains Block. The total thickness of the earth's crust
her~ is 29-31 kLn. Thickening of the earth's crust in the southeasterly
direction is noted with respect to a relatively sm~.ll number of observa-
tions. The boundary velocity at the Mohorovicic surface is 7.6-7.8 l~~sec.
The mean velocity in the entire thickness of the earth's crust is 6.1-
6.2 lan/sec.
Amery Ice Shelf Block. This block is characterized by sharp thinning of
the earth's crust. The depth to the Mohorovicic ;liscontinuity decreases
to 22-24 km. With respect to thickness the earth's crust occupies an
intermediate position between the continental and oceanic types of crust.
The western contact of the block along the t4ohorovicic boundary probably
appears not as a smooth uplifC of this boundary, but in the form of a
sharp scarp with an an?plitude of 7--9 km. In the northeasterly direction _
the t'n3,ckness o~ the earth~s crust increases to 30 km. The submersion
of the Mohorovicic discontinuity obviously takes place in a series of
scarps. The mean velocity with respect to the entire earth's crust is
6.0,6.1 lan~sec. The boundary velocity on the surface of the mantle is
7.6--7.8 km(sec. ~1s a result of the compres~ed times for the field opera-
t~.ons i.t did not appear possible to study the internal structure of the
crust ~.n the central part of the block. The refracting horizon I was
traced on the northwestern boundaxy of the block at depths of 7--8 km.
The problem of the na,ture of th~,s horizon sti?1 remains unexplained. One
of the probable propositions must be cons~.dered to be absence in tfiis
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section of a thick series of high--velocity sedimentary rock~ which is
- confirmed by the geological survey data.
Ingrid Christensen Coast Block. This block has a crust thickness of 30-32
km. The mean velocity in the crust is 6.0 to 6.1 km/sec. The
iior.orovicic boundary was studied here only by the reflectsd wave data; -
therefore there is no information about the boundary velocity. In the
upper part of the crust the refracting boundary I is submerged to a depth
of 4-5 km. The reflecting boundary IT constructed with mean velocity of
5.8-5.9 lan~sec is located at depths of 20-22 km and is uplifted in' ~he
direction of the Amery Ice Shelf.
The performed studies demonstrated the possibility of the successf.ul use
of the spot seismic sounding procedure to study the layered-block struc-
= ture of the earth's crust under the severe specif ic cor.ditions in
Antractica. The experience gained is important for plannin~ subsequent
deep seismic sounding operations in the coastal and internal regions of
this little-investigated continent and also when studyin~ Arctic regions. -
Interpretation of the Materials Obtained in the Vicinity of Verkhniy Lake
In this part of the ancient Canadian shield American geaphysicists have
performed spot ~eismic observations using a dense network and obtaining
a system of extended hodographs [147]. By the wave hodographs in the
first arrivals a numb er of researchers [139, 144, 146] have constructed
several versions of the seismic section of the ear.th's crust with two
refracting boundaries. One of them occurs at depths of 5-10 km, and the
second corresponds to the M surface (Fig 104). We performed a second
interpretation of the seismic materials obtained here by the spot sounding
procedure to compare their possibilities with the methods used by the _
forei~n researchers.
- The initi.al data for the interpretation were the time tables of the f irst
arrivals published in ref erence [147]. From the ~ntire set of data, the
times of arrival of the waves at distances of 250-300`~and 50-100 km
_ were selected. The f ields t(~c, R) were constructed by them for the
- refracted waves corresponding to the Mohorovicic discontinuity and the
upper refracting bouna~ry. Using the method of recalculating the.field
' with a decrease in bases (Chapter II, �2), isolines were calculated with
bases close to the x--axis of the initial point of corresponding waves.
The latter made it possible to find the boundary velocity distribution
and depth distribution without resort~ng to rigid assumptions re~arding
the model of the medium. The boundary~ velocities for the upper boundary
were found by the lines R=0 and R~50 lan; the depths to it were determin~d
by the l~,ne R~50 km. The Mohorov~.cic discont~.nuity was constructed by
~ the line R~,100 km~ z~nd the boundaxy veloc~.ty (3.1 km/sec) was calculated -
_ by the 1~.nes k=100 and 150 km~ The seismic sect3.on (see Fi~ 109) is not
inferior with respect to completeness of in~ormation about tfi,e structure
of the crust to the sections obtained by the other researchers, although
no more than 5 to 10% of the total nu~;ber of observations were used for
its construction.
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_ U~KM~C rl~
l
7
X~_x'X ~ X~~x`x_~ X~
f x~
~ .
3
~
~ ~v
~ ~ I ~ 2b0 . d00 ,RAD S00 6~ KM
t~
~
f 4 2 3
20
~ ~ ~ ~ ,
` 1 .
~ � ~
. ^ ~1'
'
60 . ' _ .4
/I~KM � ~
Figure 104. Comparison of the section of the earth's crust in
the vicinity of Verkhniy Lake (the Canadian shield) obtained by
- the spot soundin~ procedure (1, 1', with tl~e results of
Berry, et al. [139] (2), Smith, et al. [14G] (3) and . `
0'Brien [144] (4). 1-- the boundary was constructed with
constant mean velocities; 1' the same with variable velocity
(see the graph v in the upper part of the figure). vboundary
_ is the boundary velocity for the upper boundary according to
the spot sounding data.
Key:
1. v, km/sec
The construction b~,the sounding procedure, especially at the Pi boundary
diverge with certa~i~`~versions of the sections published by American
geophysicists (~i~; ~ 104) ~ The d~.verg,ences are most signif icant with the
results of tlne "tra.vel time" method j139~ 146], based on a number of
_ simplifyina assumptions about the model of the nedium. This method was ,
_ used to"obtain very sharp variations in thickness of the earth~s crust
from 24 to 60 lan which does not agree with the relatively little
d~,sturbed ~ield o~ gravitat~.onal anomalies in the investigated reg3on
(0-40 mgl, accordinQ to the data of j1~~9]). The best agreement of the
section, according to tI~,~sounding data, is noted with the O~Brien
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version [144] obtained by a qu~,te correct method w}iich is similar wi.tl~
- reRpect to �tts hn9:is tc~ tlie metli~cl of can~~.i~ntc~ p~int:a ot tlie h~ri~i
wnve.
The investi~ated example indicates that the spot eoun~iin~ procedure~
using special. time fields is expediently used for interpretation of the
� blast seismology data along with the methods based on using systems
_ of hodographs, especially 3.n cases where these systems are inadequate
for proper realization of the strict methods.
~
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CONCLUSIONS
The main results of this paper are the following; theoretical and
experimental substantiaion of a special procedure for performin~ regional
seismic studies o= the earth's crust and the top of the mantle in
inaccessible regions; the creation of an original design of equipmenC
for recording oscillations of the soil and subsequent processing of the
information; obtaining t~e new data about the subsurface structure of
Siberia on the regional level required for m~:.neral prospecting.
About the Procedure
1. The expediency of the step execution of the re;ional seismic studies
of all types (including the study of the folded basement, the deep zones
_ of the earth's crust and the upper part of the mantle) with subsequent
transition from the reconnaissance prospecting (lo~a-detail) operations
over broad territories to the high-detail operations in the sections of
greatest interest is demonstrated. The problem of the reconnaissance ~
prospecting phase is the study of the three-dim~nsional deep layered-
block structure and distribution of the seismic velocities in the medium
with details sufficient for characterization of the regional ~eological
_ structures and discovery of the nature of the lar~e-scale anomalies of
- the natural geophysical fields. The procedure of reconnaissance prospect-
ing operations must insure express trav~rse-ar.ea study of broad territories,
- including inaccessible territories; the required accuracy and quality
composition of the inforaiation must be obtained not as a result of compli-
cation of the observation systems, but by ~oint use of the waves of various
types ~rom the seismic reference boundaries.
2. The theory of the seismic soundings init3ally created for the .
refracted waves on the bas~s of the txad3tional hodographic approach was
developed ~or certain monotypic waves (reflected, head, refracted) and
arbitrary traverse and a,rea obseryation systems used in inaccessibTe
areas. The theory af the special two~dimensional and three~d~.mensional
~ time f ields which are a generalization o~ the concept of the seismic ~
hodograph to the case o� an arbitrary system of sources and receivers ,
was created, which has ~reat significance for the further development of
the methods of se3smic prospecting of any detail. The discrete correla-
tion of reference seismic waves recorded in the sounding system was
substantiated.
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3. The procedure was proposed and developed in practice for field
operations in the versions for profile (traverse) and area seismic sound-
in~ systems. These systems, made up of elementary soundings (the oscilla-
tion source and compact linear or area receiver), are effectively realized ~
- under complex surface conditions using river and air transportation.
The seismic oscillations are induced by group blasts in bodies of water _
or large (to 1000 individual charges~ groups of boreholes about 1 meter
deep. The methods of determining the density of the seismic observations
for the solution of the specific problema are substantiated.
4. The procedures were developed for interpr~etation of the experimental
data for reflected, head and refracted wavES~ including the ~oint use of.
wavAs of different types from the same boundary. The c?iscrete correlation
procedures for the reference waves based on the a priori data and data
obtained during the course of the operations on the wave field, the geo-
metric and physical properties of the medium are substantiated; the
process of wave identi.f.ication was formalized, obtaining quantitative �
estimates of its reliability. The methods of solving the inverse problems
using time fields have been developed both for simple models of the media
with local-plane boundary and for more complex models: multilayered media
with curvilinear boundaries, media with sharp surface inhomogeneities,
with horizontal and vertical velocity gradients. The proposed methods
permit suff iciently proper (for the problems in the reconnaissance pros-
pecting phase) interpretation of the experimental data, obtainin~ informa- ~
tion both about the configuration of the seismic boundaries and the veloc-
ity distribution of the elastic waves in the medium.
5. An objective estimate of the reliability and accuracy of the results
of the spot sounding procedure was obtained bq comparis~n with the deep
drilling and continuous seismic prospecting data under various geological
conditions from the areas of the ancient sh~elds and platforms to the
sections with Alpine a~e of the folding. The compnrison demonstrated tt~at
in the results of the sounding procedure significant surface sCructures
of the basement and the Mohorovicic discontinuity are correctly depicted
for the reconnaissance prospecting phase of the operations and also basic
characteristics of the velocity distribution in the earth's crust. The
depths to the basement surface are deterr.iined with accuracy of approx-
imately 100 meters (under the conditions of the ~,leatern Siberian platform);
the accuracy of the constructions with respect to the deeper boundarp,
including the M surface, is about 2 km; the errors in the velocities
usually do not exceed 0.2 km~sec.
About the Equipment
1. The requirements on the equipment for regional se~.smic studies in
inaccessible areas are substantiated, the basic ones of which are as
follows: high portability and reliab~.llty.with small size and wei;ht;
broad dynamic and flrequency ranges~ reliable tlne coordination of the
blasts and seismic informat~lon on a large number of scattered autonomous
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recorders operating without service personnel at the observation stations;
successive recording of the oscillations from several blasts without
preparatory operations, except remote control at a distance of up to
several hundreds of kilometers. The existing Soviet and foreign seismic
recorders do not fully correspond to these requirements.
2. The ori~inal, portable remote controlled Tayga seismic system was
developed which is specially designed for operations in inaccessible areas. -
A highly economical magnetic recording channel for recording seismic
signals using simple tape drives with a dynamic range of more than
SO decibels was built for the first time in the USSR. The noise-proof
system for radio remote control of scattered seismic recorders was built
which insures reliable time gridding of the information received at the
blast tir~e.
3. As a result of the field testing, the correspondence of this equipment
to the proposed requirements was demonstrated. The Tayga system has found
broad production application during regional seismic studies in various
parts of the USSR, including in the most inaccessible parts of Siberia -
and the Far East where previously such operations were in practice
impossible. The application of this equipment has greatly increased the
productivity of the f ield operations.
Results of Using the rTew Procedure and Equipment
l. The development of the new procedure and equipment, their broad intro-
duction into practice have made it possible to begin systematic regional
seismic studies of the basement, the entire earth's crust and the top of
the mantle over the broad inaccessible expanses of Siberia whera previously
such operations, extremely necessary to determine the deep structural laws
and for mineral prospecting, were actually never performed.
2. In the southern half of Western Siberia a fra~e network of regional
deep seismic sounding traverses has been created with a total extent of
6000 lan. Within the Western Siberian platform and its mountain frame
seismic stratification of the depths under the large crustal-mantle blocks
separated by abyssal fracture zones have been discovered. The data ob-
tained are important for more correct solution of the problems of tectonic
regionalization and serve as the basis for deep geological interpretation
of the entire set of geophysical materials. -
3~ In the territory o~ the ~rlestern Siberian platform in the broad
(15Q00 km) networ~ of reg~onal refracted wave sounding traverses and in
the indiv3:dual areas work has been done to study the morphology and .
physi.cal propert~es of the basement surface which axe ~,mportant ~.n ~
connection with o~,l and gas pxosvect~,ng~ In the Qmsk and Novosibirsk
Oblasts over an axea o~ 1Q0~00 km2 a study has been made of the internal
three~di~mensional structure of the basement w~.th isolation of the low--
_ velocity layers prospective ~or finding ~aleozoic petroleuia.
~
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4. In the Siberian platform the regional study of the basement (about
8000 km traverses) was made under extraordinarily complex surface and
subsurface conclitions of the Tungusskaya syneclise and also in the
southern (tlepskiy arch) and eastern (~akutia) regions. Theoretically new
data were obtained on the structure of the basement ancl the bottom of
- the sedimentary mantle required for proper orientation of future petroleum
prospecting work. The f irst informationabout the laws of the deep struc- _
ture of the earth's crust and the top of the mantle in the area of
development of kimberlite magmatism was obtained for Y~.kutia.
5. In the Baykal rift zone, which is the largest structure of its type
in Eurasia, the greatest degree of seismic study of the deep structures
- by comparison with other (foreign) continental rifto~enesis zones was
achieved in a short time (1968~~1975). The traverse (more than 4000 km)
and area studies encompassed the central part of the zone, its flanks
~ (including the region where the BaykalNAmur railroad is being built)
and ad~acent parts of the Siberian platform, Eastern Sayan and Transbaykal.
Alon~ with the general features of the deep layered-block structure, the
characteristics were discovered which are connected ~�~ith the active
tectonic process: the presence of a broad (more than 200000 lan~) upper
mantle re~ion with anomalously low seismic wave velocity (7.7-7~8 km/sec)
characterized by an average thickness of about 20 km and not having a
continuous connection with the asthenospheric Gutenberg channel; coordina~
tion of :the Baykal basin with the complex faulted zone above the edge of '
the anomalous region; the existence of an intracrustal seismic waveguide,
apparently to a significant degree controlling the course of the geodynamic
processes and the seismicity distribution in the ~iven region.
In addition to studying the Siberian regions, significant work was done
using the new procedure in two parts of the east coast of Antarctica
(the work of the 14th and 18th Soviet Antarctic Expeditions). The first
and still only seismic data for the sixth continent about the structure
of the entire earth's crust and top of the mantle were obtained. Valuable
experie~lce was gained in performing studies under~~the severe polar condi-
tions with a solid ice cover. As a result of using the sounding procedures
to interpret the t~last seismology material for the vicinity of Verkhniy
Lake (the Canadian shield) the expediency of using this material in the
case of incomplete hodograph systems insufficient for proper realization
of ordinary strict proc,edures, is demonstrated. The introduction of the
sounding procedure and the Tayga equipment was started in the Far East.
266
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y,
v"~ ~ BIBLTOGR~IPHY
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22. GEOLOGICHESKKOYE STROYENIYE ZEMNOY KOPY V SPBIRI I NA DAL'NEM VOSTOKE -
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29. Davis, G. L., PRIMENENIYE TOCHNOY MAGNITNOY ZAPPSI [Application of
Precision Magnetic Recording], Moscow, Energiya, 1967, 286 pages.
30. Yegorov, G. V., Yemei'yanov, A. V., Chichinin, I. S., "Devi~e for Remote
Control of a Seismic Recorder," USSR Author's Certificate No 244648,
BYUL. IZOBR., 1969, No 18. -
31. Yepinat'yeva, A. M., FIZICHESKIYE OSNOVY SEYSMORAZVEDKI [Physical ~
Principles of Seismic Exploration], Moscow, Izd-vo MGU, 1970, 105 pages.
32. Zverev, S. M., "Deep Seismic Sounding at Sea," MATERIALY MEZHDUNARODNOGO
SOVESHCHANIYA EKSPERTOV PO VARYVNOY SEYSMOLOGII [Materials from the
International Conference of Experts in Blast Seismology], Leningrad, :
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33. Zlatopol'skaya, A. V., Yanushevich, T. A., "Some Methods of Using
Quantitative Estimates of the Reflected Wave Correlation for the Discrete~
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[Discrete Seismic Wave Correlation], Novosibirak, Nauka, 1971, pp 111-120.
269 -
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34. Kabychenko, N. V., "Some Problems of Multiplexing Seismic Signals,"
SEYSMICHESKIYE PRIBORY [Seismic Instruments], No 6, Moscow, Nauka, 1.971
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35. Kabychenko, N. V., "Development of Multichannel, Radio Seiamic Equipment
for Deep Seismic Sounding," Author's Review of Candidate's Dissertation
- Moacow, IFZ AN SSSR, 1971, 19 pages.
36. KARTA TEKTONICHESKOGO RAYONIROVANIYA SIBPRSKOY PLATFORMY [Tectonic
Regionalization Map of the Siberian PlatformJ, Editor-in-Chief V. V.
Seminovich, A. A. Trofimuk, Moscow, Ministerstvo geologii SSSR, 1974.
37. Kirillov, F. A., "Seismic Blast Effect," TR. SEYSMOLOGICHESKOGO INSTITUTA
AN SSSR [Works of the Seiemological Institute of the USSR Academy of
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38. Klushin, I. G., "Isolation of the Geophysical Anomalies Smaller than
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[News of the USSR Academy of Sciences. Geophysics Series], No 2, 1959,
pp 189-196.
39. Kovalevskiy, G. L., "Experimental and Theoretical Studies of Diffracted
Seismic Waves Above the Low-Amplitude Dislocations of the Break in
~ Continuity," Author's Review of Candidate's Dissertation, Novosibirak,
Institutie of Geology and Geophysics of the Siberian Department of the
USSR Academy of Scienees, 1976, 186 pages.
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by the Deep Seismic Sounding Method," GEOL. I GEOFIZ., No 10, 1971,
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41. Kolmakov, A. F., Mishen'kin, B. P., Solov'yev, D. S., "Deep Seismic
� Studies in Eastern Antarctica," INFORMATSIONNYY BYUL. SOVETSKOY ANTARK-
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42. Kondrat'yev, 0. K., Gamburtsev, A. G., SEYSMICHESKIYE ISSLEDOVANIYA V
PRIBREZHNOY CHASTI VOSTOCHNOY ANTARKTICY [Seismic Studies in the Coastal
Part of Eastern Antarctica], Moscow, Izd-vo AN SSSR, 1963, 188 pages.
43. Kosminskaya, I. P., METOD GLUBINNOGO SEYSMICHESKOGO ZONDIROVANIYA ZEMNOY
KOPY I VERKHOV MANTII [Method of Deep Seismic Sounding of the Earth's
Cruat and the Top of the Mantle], Moacow, Nauka, 1968, 227 pages.
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i
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46. Krylov, S. V., "Causes of Anomalous Properties of the Upper Mantle in _
Che Rift Zones," GEOL. I GEOFIZ., No 4, 1976, pp 3-17.
47. Krylov, S. V., "Accuracy of the Results of Refracted Wave Seismic
Soundings," Geol. i Geofiz., No 4, 1964, pp 120-130.
48. Krylov, S. V., "Spatial Spot Seiamic Observation Systema," GEOL. i
GEOFIZ., No 2, 1968, pp 78-85.
49. Krylov, S. V., Golenetskiy, S. I., Petrik, G. V., "Matching the Seismo-
logical and Deep Seismic Sounding Data on the Structure of the Top of
the Mantle in the Baykal Rift Zone,", GEOL. I GEOFIZ., No 12, 1974,
pp 61-65.
50. Krylov, S. V., Yegorov, G. V., Dubovik, L. V., Bochanov, A. I.,
Yanushevich, T. A., "Deep Seismic Studies in the Kuznetsk Basin Using
Industrial Blasts and the Taiga Equipment," GLUBINNYYE SEYSMICHESKIYE
ISSLEDOVANIYA V ZAPADNOY SIBIRI [Deep Seisads Studies in Western
Siberia], Moscow, Nauka, 1970, pp 114-123.
51. Krylov, S. V., Kondrashov, V. A.,Mishen'kin, B. P., Potap'yev, S. V.,
"Application of Spot Seismic Soundings to Study the Earth's Crust in
the Western Siberian Lowland," METODIKA SEYSMORAZVEDKI [Seismic Explora-
tion Procedure], Moscow, Nauka, 1965, pp 71-91.
52. Krylov, S. V., Krylova, A. L., Mishen'kin, B. P., Mishen'kina, Z. R.,
Rudnitakin, A. L., Suvorov, V. D., Yanuiyevich, T. A., "Deep Seismic
Studies in the Southeastern Part of the Western Siberian Platform and
in the Altaye-Sayan Oblast," GEOL. I GEOFI~., No 4, 1968, pp 3-12.
53. Krylov, S. V., Krylova, A. L., Mishen'kin, B. P., Mishen'kina, Z. R.
Pudnitskiy, A. L., Suvorov, V. D., "Irtysh Deep Seismic Sounding Tra-
verse," GEOL. I. GEOFIZ., No 7, 1969, pp 11-20.
54. Krylov, S. V., Krylova, A. L., Mishen'kina, Z. R., Ryaboy, V. Z.,
"Results of Spot and Continuous Observations During Deep Seismic Sound-
. ing," GEOL. I GEOFIZ., No 3, 1966, pp 101-112.
55. Krylov, S. V., Mishen'kin, B. P., Krupskaya, G. V., Petrik, G. V.,
"Deep Seismic Studies in Transbaykal," GEOL. I. GEOFIZ., No 12, 1971,
pp 108-112. �
56. Krylov, S. V., Mishen'kin, B. P., Krupskaya, G. V., Petrik, G. V.,
Yanushevich, T. A., "Structure of the Earth's Crust by the Deep Seismic
Sounding Profile Through the Baykal Rift Zone," GEOL. I GEOFIZ., No 1, .
1970, pp 84-91.
57. Krylov, S. V., Mishen'kin, B. P., Mishen'kina, Z. R., Petrik, G. V.
Seleznev, V. S., "Seismic Section of the Lithosph~re in the Vicinity
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271
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58. Krylov, S. i~., Mishen'kin, B. P., Petrik, G. V., "Study of the Top
of the Mantle by the Deep Seismic Sounding Method in the Baykal Rift
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59. Krylov, S. V., Puzyrev, N. N., "Consideration of the Effect of the
Curvilinearity of the Refracting Boundary When Interpreting Seismic
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60. Krylov, S. V., Rudnitskiy, A. L., Mishen'kin, B. P., Krylova, A. L.,
" Mishen'kina, Z. R., Suvorov, V. D., Yanushevich, T. A., "Seismic Studies
of the Earth's Crust in w'estern Siberia," GLUVINNYYE SEYSMICHESKIYE ISSLE-
DOVANIYA V Zt1PADN0Y SIBIRI [Deep Seismic Studies in Western Siberia],
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V ZAPADNOY SIBIRI [Deep Seismis Studies in Western Siberia], Moscow,
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62. Krylov, S. V., Suvorov, V. D., "Interpretation of Seismic Data Under
the Conditions of Surface Nonuniformities," METODIKA SEYSMICHESKIKH
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63. Krylov, S. V., Surkov, V. S., Mishen'kina, Z. R., "Structure of the
Earth's Crust in the Southern Part ot the Western Siberian Lowland,"
GEOL. I GEOFIZ., No 1, 1965, pp 62-73.
64. Krylov, S. V., Krylova, A. L., Sergeyev, V. N., Suvorov, V. D.,
"Regional Area Seismic Studies of the Internal Structure of the Base-
ment of the Western Siberian Platform," METODIKA I REZUL'TATY SEYSMICHESKIKIH
ISSLEDOVANIY V SIBIRI [Procedure and Results of Seismic Studies in
Siberia], Novosibirsk, Nauka, 1976, pp 62-76.
65. Kuznetsov, V. L., "Problem of the Application of Area Blasts in Low-
Velocity Zones," MATERIALY PO GEOFIZICHESKIM ISSLEDOVANIYAM V ZAPADNOY
SIBIRI [Materials on Geophysical Studies in Western Siberia], Novosibirak,
1974, pp 69-74 (Works of the SNIIGGiMS Institute, No 30).
66. Kuznetsov, V. L., Bgatova, G. F., Alekseyeva, V. V., "Procedure for
~ Regional Seismic Studies of the Basement of the Western Part of the
Siberian Platform," No 1, 1972, pp 78-85.
I
~ 67. Kuznetsov, V. L., Bgatova, G. F., Alekseyeva, V. V., "Reconnaissance
; Prospecting Seismic Studies in the Southeastern Part of the Tungusakaya
' Syneclise," GEOFIZICHESKIYE ISSLEDOVANIYA V SIBIRI [Geophysical Studies
i in Siberia], Novosibirsk, 1974, pp 36-45 (Works of the SNIIGGiMS,
~ No 196) .
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68. Kuznetsov, V. L., Zaytsev, Yu. G., Nikishina, V. F., Sal'nikov, A. S.
Tkach, A. S., "New Seismis Data on the Structure of the Central Part
of the Tungusskaya Syneclise," GEOL. I GEOFIZ., No 7, 1975, pp 156-161.
F
69. KuzneCaov, V. L., Ocheretina, V. B., "Refiected Wave Amplitude as a
Function of the Group Blast Parameters ~!n the Low Velocity Zone under
the Conditions of tl:s Western Siberian Lowland," GEOL. I GEOFIZ., No 10
~ 1969, pp 86-93.
70. Kuznetsov, V. L., Strelkova, V. V., "Amplitude Spectra of the Reflected
Waves as a Function of the Group Blast Parameters," GEOL. I GEOFIZ.,
~ No 12, 1970, pp 105-109.
71. Litvinenko, I. V., "Procedure for Detailed Studies by the Seismic Method
of the Structures of the Upper Part of the Earth's Crust in the Examgle
of the Baltic Shield," MATERIALY MEZHDt~*1ARODNOGO SOVESHCHANIYA EKSPERTOV
PO VZRYVNOY SEYSMOLOGII [Materials of the International Conference of
Experts on Blast Seismology), Leningrad, 1968, Kiev, Naukova Dumka, 1969,
pp 79-88.
72. Mishen'kina, Z. P., "Interpretation of the Refracted Wave Photographs
in the Presen.ce of Vertical and Horizontal Velocity Gradients,"
IZV. AN SSSR. FIZIKA ZENII~I [News of the USSR Academy of Sciences. Earth
Physics], No 4, 1967, pp 84-91.
73. Mistren'kina, Z. R., "Characteristic Features of the Photographs of Re-
fracted and Reflected Waves in Certain-Continuous Layered Media,"
GEOL. I GEUFIZ., No 8, 1972, pp 80-93.
74. Mishen'kin.; B. P. "Use of Exchanged Waves for Deep Seismic Studies in
Western Siberia," GEOL. I GEOFIZ., No 12, 1968, pp 82~92.
75. Mishen'kin, B. P., "Theoretical Reflected Waves Seismograms from the
Linear Transition I.ayer with an Arbitrary Angle of Incidence," GLUBINNYYE
SEYSMICHESKIYE ISSGEDOVANIYA V ZAPADNOY SIBIRI [Deep Seismic Studies in
Western Siberia], Moscow, Nauka, 1970, pp 33-42.
76. Mishen'kin, B. P., "Application of Mangetic Recording for Deep Seismic
Studies," GEOL. I GEOFIZ., No 10, 1965, pp 118-127.
77. Mishen'kin, B. P., Krupskaya, G. V., Petrik, G. V., Seleznev, V. S.
"Deep Seismic Studies in the Northeastern Part of the Baykal Rift Zone,"
GEOL. I GEOFIZ., No 4, 1975, pp 71-78.
78. Monastyrev, V. K., UCHET YAVLENIY REFRAKTSII PRI SEYSMORAZVEDOCHNYKH ,
RABOTAI~i METODOM PRELOIrff~ENNYI~i VOLN [Consideration of the Refraction .
Pheno~menon During Sei$mic Exploration by the Refracted Wave Methods],
Moscow, Nedra, 1970, pp 90-98. (Works of the ZapSibNIGNI, Vol 17).
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79. Monastyrev, V. K., Bobrovnik, I. I., Konovalov, Yu. G., "Substantiation
of the Soundings by the Refracted Wave Method for Mapping the Surface
- of the Baeement of the Western 3lberian I.owland," MATERIALY PO GEOFIZI-
IC~ESKIM ISSLEDOVANTYAM V ZAPADNOY SIBIRI [Materials on the Geophyeical
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