JPRS ID: 8275 METEOROLOGY AND HYDROLOGY DECEMBER 1978

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iTFEBRUARY 1979
FOUO NO. 12
i OF 2
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JPRS L/8275
' 13 February 1979
MET'EOROLOGY AND HYDROLOGY
NO, 12, DECEMBER I978
U. S. ;OINT PUBLICATIONS RESEARCH SERYICE _
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JPR5 L/8275
13 February 1979 =
METEOROLOGY AND HYDROLOGY
No. 12, December 1978 ~
u
Selected articles from the Russian-language journal
METEOROLOGIYA I GIDROLOGIYA, MoscAw.
CONTENTS
PAGE
Natural Components of' Sma,ll Samplea With a Large Number of
_
Parameters
~ (N. A. Bagrov)
.
1

Some Characteristics of Wave Orographic Cloud Cover Over the
Middle and Northern Urals
(T. N. Bibikova)
14
Statistical Indices of Spatial Distribution of Precipitation in
the Experimental Meteorological Polygon
-
- (V. M. Muchnik)
28
Increase in the Visibiltty Range of Laser Beacons in a Fog
- (0. A. Volkovitskiy, V. P. Snykov)
37 `
- Spring Restructuring of the Temperature and Pressure Field in
the Southern Hemisphere
(L. A. Uranova)
51 _
Relationship Between Atmospheric Pressure and the Level of the
Northwestern Part of the Pacific Ocean
(S. S. IaPPo, et al.)
61
Equilibrium Model of I,angmuir Circulation in the Ocean
~
(A. A. Zelenlko)
70
Improved Models of Water Discharge and Evaluations of Accuracy
of Its Measuremeat by the " Velocity -Area" Method
a (I. F. Karaaev)
82
- a- [III - USSR - 33 S&T FOUO]
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I.*Uk cl!.,l~ ICIAL IItiP; ON1,1'
A
CONTENTS (Cont;inued)
Page
Determiriation ot' the Pfirametera of Ground Permeability From
UnstaUle Ini'iltrntiou CtLrves
(V. M. Iknlsov)
93
Evaluation of Soil-Climstic Conditions Appli(sable to the
Cu.ltivation of Winter Wheat
(z. v. s-oisyuk)
105
Forming of Archives of Observational Datr for the Firat Global
bcperiment GARP
(0. A. Aldukhov)
112
:utomation of Collection, Processing and Analysis of Oceanographic
Information on the Basis of Small Electronic Computers
(V. A. Volkov, et al.)
122
Methods of Image Recogaition Theory in Problems Involving
llnalysis e,nd Prediction of Meteorological Fields
(Yu. V. Semenovskiy)
130
Twenty-Fifth Anniversary of the Transcaucasian Scientific
Research Hydrometeorological Institute
(G. G. Svanidze, Z. I. Tskvitinidze)
142
Work of A. A. Friciman in the Field of Hydrology
(Ye. S. Selezneva)
150
Review of Book by V. V. Kupriyanov: `'Hydrological Aspects of
Urbanization" (Gidrologicheskiye Aspekty Urbanizatsii)
Leningrad, Gidrometeoi2dat, 1977
(A. V. Karaushev, B. G. Skakal'skiy)
158
Seventieth Birthday of Nikolay Aleksandrovich Bagrov ..e.........
163
Sixtieth Birthday of Vaeiliy Ivanovich Sapozhnikov
164
At Institutes of the State Commission on Hydxometeorology
(N. N. Pocigayskiy, G. V. Gruza)
166
Cunferences, Meetings and Seminars
(N. P. Smirnov, E. I. Sarukhanya.n)
170
Notes From Abroad
(B. I. Silkin) 174
- b -
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.
PUBLICAT,CON UATA
English title : Nleteorology a.nd Hydrology No 12,
Dea 78
_ Russian titlP . METEOROLOGIYA I GIDROLCGIYA
Author (s) . N. A. Bagrov, T. N. Bibikova,et al.
Editor (s) . Ye. I. Tolstokov
Publishing House . GIDRONER'EOIZI)AT
Place of Publication . Moscow
Date of Publication . 197$
Signed to press ' . 28 Nov 1978
Copies , 4030
- COPYRiGHT : "Meteorologiya i gidrologiya",
1978
- c -
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FUk c1FFiCTAI, USL UNLY
UDC 551.509.314
- NATURAL COMPONENTS OF SMALL SAMPLES WITH A LARGE NUMBER OF PARAMETERS
_ Moscow METEOROLOGIYA I GIDROLOGIYA in Russian No 12, Dec 1978 pp 5-14
- (Article by Professor N. A. Bagrov, USSR Hydrometeorological Scientific Re-
search Instirute, submitCed for publication 14 July 19781
Abstract: A new method is proposed for comput-
ing the natural orthogonal components in a
case when the volume of the sample is less than
the number of introduced random variables. This
Procedure makes possible a considerabl.e reduc-
tion in computation work and in some cases one can
solve the full problem for a symmetric matrix,
earlier beyond the capabilities of modern elec-
tronic computers with average capacity. Some
- historical comments are made in passing.
[Text] The expansion of mPteorological fields or in general a random vector
in natural orthogonal functions has found extensive application since the
publication of [3]. This method is presently given ciifferent names by dif-
Cerent authors: the main components method, expansion in empirical or -
::tatistical orthogonal functions [1, 7, 8, 121, or the Carunecr-Loeve e:tpan-
sion [S]. All these names have some basis. However, with respect to the
_ latter, it should be noted that one of the first studies in this di.rection -
_ was made by Hotelling and dates back as far as 1933 [11], whereas the studies =
by Carunen.lnd Loeve,judging from the citations in [6], date back to 1947
and 1945-1946 respectively.
Now we will briefly examine the entire problem using matrix calculus. ,;ssume
there is a random vector F of the dimensionality n, that is, having n com-
ponents, in general correlated with one another. Its covariation matrix is
- written in the following way:
F,f-', F,Fz . . . Ftt'n
M _ PF F=F, FzF= . . .
F�F1 F�F. . . . F�PR
~
1
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FOIt (lFFTCIAL U:;1. ON1,Y
lierr_~ the asrerisk is rhe transposition sign, whereas the line at the top -
is the mathematicnl expectation symbol (empirically the averaging sym-
bo1),
Iluwvvi-r, In hocli tlii-or(,1 Irn l niicl I) rtict trnl p rohlom;i it t: rnn,+tdor;ihly
mere eoiiveiilenl lo deul willi u ver.tor w1C12 uncorrelated compoients. 5ome- -
rimes, however, instead of the F vecl�or, especially if- it has a very great
dimensionality, it is desirable ro exrinine some approximation of it. In
' both these problems the result is achieved by a linear transformation of
the F vector
F=UA, (2)
where U is the transCormation matrix-operator (in general, inverse), and
r1 i.s the new vector. The transEormation (2) will retain the general dis-
persion of the Fvector iF U is an orthogonal matrix, sa that UU* = U*U -
= I. In actualiry, under t}iis condiCion we wi11 have
F*F=A*U*UA=A*:1.
(3)
~ If the U mutris columns are selected in a definite way, for example, in
the form of a set of values of some orthogonal functions in a grid of
equally spaced points, it is possible to obtain an expansion of the F
, vector using these functions. This assertion follows from the simple
fact thaC the transformatioti (2) can be written in a more expanded form
F=UOIA1+ U02AZ+ + UOnAn,
_ (4) -
wliere Ak is a component of the A vector and Upk (k = 1, 2,...,n) is a col-
- umn of the U matrix.
f.~or example, if as the U matrix we take the matrix
1
1
0 1
1
0
1 -1
1
-1
0 1
'
1
0
-1 -1
ttien after normalization of its columns we obtain an expansion of the F
vector in trigonometric functions. The first column of this matrix repre-
tients the cosine of zero, repeated four times; the succeeding columns are: _
t�os 21t t, sin 21t t, cos 4Tt t for t= 0, 1/4, 2/4 and 31/4. If the last
column of this matrix is replaced by zeroes, we obtain an approximate
(broken) expansion. Similarly it is possible to obtain an expansion of
the random vector in Chebyshev polynomials.
2 -
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FoR oFrzcr.nL usE ocvLY
; Ilowever, in a gencral cnse rhe components of the A vector here will '
not be muCually orthogonnl, On the orher hand, obCaining mutually ortho-
~ gonal Limponents of the A vector can be one of the purposes or the Crans- ~
_ formation (2). In particular, it was poinred out in [4] how, knowing the
c:ovariation maCrix oF the F vecCor,it is possible to form the triangular
mtttrix U, by means of which it is pQSSible to obtain a vector with un-
correla'ted components. Dy means of a special normalization of the U mat-
- rix ir is even possible to achieve an equality of the general dispersion
= of both vectors, that is, retain equations (3).
Among all the transformations of this type the most modern, and probably
_ the most natural wj.ll be a transformation following from a representation
_ uf the covariation matrix of the F vecCor through the covariation matrix of
the A vector
' A1 U.4A"Ua'. `
_ If it is now necessary to have a diagonality of the covariation matrix of
the A vector
~
%.2 Q
%2 =
_ AA"=.\- ,
v '
0 ~n -
we will have, assuming the U matrix to be orthogonal, -
,1? = FF* = UAU-'.
- 'fhis formula shows that the ill, ;k2,..., )Ln values must be the eigen-
values of the covariation matrix M(we will always arrange them in de- -
creasing order), whereas the columns of the U matrix give the corres-
ponding eigenvectors. The transformation (2) of the-F vector from such
_ ii matrix has anottier extremal property that it gives the most rapid con-
vergence of series (4) in the sense of an approximation to the general
clispersion of the F vector. .
Thus, the expansion (4) with satisfaction of equation (5) is obtained in
o "natural" way from the properties of the F vector itself.
liowever, historically the situation had developed in such a way that de-
spite the fact that the fundamental principles of the main components or
ii.ztural components methods have been known since 1933 they evidentally did
not initially come into broad application. Accordingly, in the 1950's,
when the possibilities of electronic computers became well known, meteor- -
ologists had to discover this method anew. This is indicated by the first
3
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"meteorologicttl." publicm, that is, the
- dimensionality of the F vector is greater than the sample volume. And
such a relationship between n and m is undesirable (by means of a dPCrease
_ in dimensionality of ttie F vector) or is impossible (by meana of increas- -
_ ing ttie sample) to change. Such circumstances are rather frequently ob-
served in prognostic practice in meteorology. It makes sense to call
samples whose volume is less than ttie number of introduced variables
(m < n) "small samples." For a small. sample it is possible to simpli�y con- -
,;iderably the computation of the eigenvectors and the eigenvalues of the
covariation matrix.
In this case the covariation matrix FF* will have a very great dimensional-
ity (n x n), but its rank will not be greater than m, that is, not less
LI1111 (ct - m) of its ei� envalues will be equal to zero. In this case in
place of tlie matrix Fr it is necessary to examine the matrix F*F, whose
(limensionality will be n x m. Iienceforth we will assume that all the eigen-
vcil�es oE this latter maCrix will not be equal to zero.
- i1s Is known, the eigenvalues of these two matrices [8] coincide; in his
stucly [9] V. L. Sklyarenko used a simple relationship between their eigen-
vectorG. I3otli these postulates are demonstrated �rery simply. First of all,
for the second (small) matrix we will write a formula for raduction to a
cliagonal form
_ F*F=VAV*.
4
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Fui; 1-'i c; i ni, u;;K OvI,~~
~~iF - vAv*. (7) .
J We will mtiltiply this equarion (it makes no d3fference whether From the
right or Ieft) hy irself.. As A result, by virtue oE the property W* = T -
F*(FF*)F=VA2V*;
or aFter the obvious transformations
(1/*F*) (FF*)FV=A2. (g)
= I3ut this is the formula for reduction of the covariation matrix FF* to
diagonal form. Expression (7) makes it possible to conclude thati the col-
timns of the FV matrix are orthogonal. The column of this matrix can be "
arehonormalized by mulriplying on the righe by A'1/2 and then it wi11 be-
(-ome nn ortliogonal matrix of the eigenvectors of the FF* matrix; the diag-
unal matrix ./1, becomes the matrix of eigenvalues. Thus,
= U= FV:1-11=, (9)
This ~s tlie basis of ttie relationship between the eigenvectors of the FF*
~ ~ind F F matrices. Incidentally we obtained proof of the equality of the
- flrst m eigenvalues of Chese matrices. Iiere it must also be noted that
Formula (9) determines only the E-irst m eigenvectors of tlie FF* matrix.
,
- Formula (9) gives a significan*_ representation of the initial matrix
F= UA'1s V.
(10)
This irnown formula [1] is extremely rarely cited in the academic litera-
ture.
- By a simple multiplication this formula leads back to formulas (5) and (7).
lJe note that ttie U matrix in formula (10) must, in accordance with the
rules f.or multiplication of matrices, h;ave a rectanQular dimensionality
(n x m), that is, contain eigenvectors corresponding only to the numbers
Ai, not equal to zero.
, Now we will turn again to formula (2). If the F vector is represented by
' the sample matrlx (6), then the vector A must be represented by a matrix;
in the case n> m the matrix of eigenvectors U will be inc.omplete since the
eigenvectors for filling up this matrix will not play a role in any case.
liut it follows from this that the A matrix must be square: m x m.
al1 nl2 . . . Ql m
A _ n:t a2: . . . (izm
- pm I am ~ . . . Qmm
5
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FoR 01?rrc;iAL usi: Ocvi,v
r\n el.e.menl of the F mutrix, according ro (2), is expressed by the formula
- 1- o L" Un I "I k+ Un : fI ' k -i- Un m p m kI
wtlicli makes it possible to wrile a column of the F inatrix in the torni:
Frj Urs ns/,
s (12)
where the Up S symbol designates the s-th column of the matrix of eigenvec- tors U.
' Lxpression (12) is prec:lscly an expansion of the F vecCor (its realization)
in natural orthogonal functions (in eiRenvectors of the covariation matrix).
'I'he coeEficients of this expansion aik constitute the matrix (11), derer-
miied by a formu.la wtiictl is the inverse of ('L).
A= U*F. (13)
It is easy to see that ~
AA*=r1
or otiierwise =
aok ' aIl k = ll ~ --(i ~k = ~.k. (14)
Thus, the spur (FT*) = spur (AA*). _
According ro (11), t'ne A matrix contains only m2 elements, whereas the F ~
matrix contains n x m independent elements. T.n order to express the lacking
_ nm - m2 = m(n - m) elements we use variab].e U. The latter in incomplPte
form contains a x m elements, of which only the m2 elements determined -
- from the V matrix are independent. The remaining m(r, - m) elements were
:ilso expressed precisely using the U matrix in accordance with (10).
Ilowever, this indicates riiat the evaluation of the covariation matrix FF* _
hy meniis of the matrix r(n x m) is rather fair.
Similarly, iC is possible to express the F* matrix through the matrix of
t-igenvectors of the F*F matrix. lJe will have
F*=VB. (15)
' '1'he li matrix in this formula has the dimensionality (m x n). Ustng ttie ele-
nietits of t}iis matrix it is possible to derive a formula similar to (12)
For ttle rows of the F inatrix (or the columns of the F* matrix).
Fko= bi kVoI f-b, kVo.,Y . . . ~ bmkVOk� (16) -
6
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1 FOk 0FFICIAL U5L ONLY
,d
Similarly to formula (14), we can obtain
.
k o bR o ` bk i + + bRm
' '1liere is a Himplc r_orrelation between the matrices A and 13, following from
(2) and (15); equ;ir_in;; the right-hand sideg af these fnrmulas (wiCh trang-
positioning), we obtain -

A= (VBU)*. _
We write, in accordanre with (9),
F= UA=FVA- '12 A.
~
We multiply this equation on the left by V*H'* and on the right by V; we ob-
tain
- A = ,1A-10 AV -
or
_ A = A112 V�' (17)
71iis formula can also be dertved directly by a comparison of formula (10)
:ind :i macrix analoque of formula (2).
'I'he prinripal merit af formula (17) is that in order to obtain the A matrix
it is not at all neceKSary to return to the roatrix of initial data F.
.\5sume now tF;at it is necessary to find the regression of some variable 2
to the 1;arlables F1. FZ� ���,Fn the components of the F vector, a sample
of whiclt was given by t.he matrix (6). The sample of the variable Z will
evidently be represei.red by a row of the volume m(of m terms). We will
seek a rexression not directly to the variables F1, F2,..., Fn, but to the
.~.riables of the A matrix. In this caae the regression equation can be
written in the following form:
A -
Z= c, alo r ez Q,t� 4- e,,, Qme, ~18)
Wliere ~1� Ez,���, tm are coefficients w}iich fvr the time being are un-
1tine of these systems. It follows from our direCt observations of clouds
of tlic Ac l.ent t,:7e [tiat the lifetime of a system Consisting of Wave oro-
aphic cloud!4 varies from 2 hours 30 minutes to lU hours. The individual
lenticular clouds entcring into the system concinuously change form and
qiLe. T1ie velocities oE liorizontal change in individual clouds of the Ac
lent type vary from 1 to 3 m/sec and their iifettme is 12-50 minutes.
The processiny, of the stereophotograrcmetric pho[ographs indicated that in-
(ftvidual Ac lent pulyated, that is, the lenticular clouds developed in a
definite reKion and at some moment in time attained their taaximum size.
"hen the r_iouds beRan th decrease in volurae until they had completely di >.rind shear occurred with a Fradient of 8 m/sec per kilometer.
,1s in ttie rrecedinK rase, in the oncoming flow therr was a cottsiderlble '
laver wi.th a small. vcrr.ical temperature gradiectt. At altitudea from 1.5 `
ta 3 kn the vertical temperature p,radient - 0.4�C/100 m.
"ihus, not only tndirectly, but alyo instrumentally, it was possible to es-
tablish that the izifluence of th-I [itals kange iq manifesCed in the field
i+i orogranhir_ c' oucl covcr for a dinr_ance nf morc thatt 150 km.
We nate iti cc,nr.lusioi rhat the Northern Urals is exceptionally favorable
far leeuard wave forration. When ttiere are westerl}' air flows the cloud
systems consistinQ of clouds of the Ac lent type correspond to a tWO-dimen-
sional pattern of f]oW.
B L Bi.IOGEtAP1{Y
' i. Iiibikova, T. t+., Ir;ubyuk. A. F., Trubnikov, B. N., "Conditions for the
Fornaeion of Ac lent in the Crimean Region," TKUbY TsAO (Transactions of
t}ie Central Aerological Observatory), No 47, pp 85-91, 1963.
2, I3ibikova, T. N., Uyubyuk, A. F., Kozhevnikov, V. N., "5ome Results of
a Comparison of Theory and Observations of Wave Clnuds," TRUDY VIII _
VSF:SOYU'I.NOY KONFFRE1dT5II PO F I7.IKE ODLAKOV I AKTIVNYM VOZUEY5TVIYAM
(Transactions of tiie Eighth All-Union Conference on the Physics of
Cloucis and Artificial Modification), Lettingrad, pp 430-441, 1970.
1. !)yubyuk, A. fi., Bibikova, T. ll., Trubnikov, B. N., "Influence of Moun-
taiti Topography and the 5ea on Fortn.ation of Summer Cloud Cover Qver
the Souttiexn Crinea," TRUbY UkrNIG*tI (Transactions of the Ukrainian
Scientific Research Nydrometeorologieal Institute), No 26, pp 74-85,
1961.
'6
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4. byubyuk, A. P., t3ibiknva, T. N., "Conditiong for Formation of Cldud
Cnver in Uependence nn Orography," TRUUY GGO (Trangactions of the
Main Caophynical Observatory), No 171, pp 130-143, 1965.
5. Uyubyuk, A. F., "On the 1'hedry nt Lee P4ountaitt Waves for a Riye with
an AXbitrery profile," tZVE5TIYA AN SSSR, FIZIKA ATMOSFEitY I OItEANA
(News of t}ie USSit Academy df 5Cienceg, phygics of the Atmosphere and
Ocean), Vol IX, No 3, pp 235-246, 1973.
Uyubyuk, A. F., Hibikova, T. N. , Trubnikov, B. N. ,"Snme Physical prop-
erties nf Ac lent," ME'TEnitOLOGIYA I ClbftOLOGIYA (MeCeorology attd Nydro-
logy), No 4, pp 3-9, 1963.
7. Kozhevnikov, V. N., Kozoderov, V. V., "Theoretical I'icture of F1ow
Around the Crimean Itange in the Ynlta Itegion," IZVCS'TIYA AN 555it, FIZ-
IKA AVt05FEItY 2 OKEANA, Vol VI, No 10, pp 979-988, 1970.
Kozhevnikov, V. N., "Grographic Digturbances in a'Itwo-bimenaional 5ta-
tionAry I'roblem," IzVCSTIYA AN 555R, FIZIKA A'I'MO5FEItY I OKEANA, Vol IV,
Nn 1, pp 33-52, 1968.
- 9. Kozhevttikov, V. N., I3ibikova, T. N., Zhurba, Ye. V., "Orographic Atmo-
spheric Uisturbances Over ttte NorChern Urals," IZVESTIYA AN 555It, FIZ-
IKA A'TMOSFEItY I 0lCEANA, Vol XIII, No 5, pp 451-460, 1977.
10. 5ovetova, V. D., "Influence of the Urals Itange on the Evolution of
Frontal Cloud Cover," TRUbY TsIP (Transactions of Che Central InsCiCute
oE Forecasts), No 79, 1959. -
- 11. Khrgian, A. Kh., "Influence of the Urals Range on Cloud Cover and Pre-
cipitation," METEOROLOGIYA I GIDROLOGIYA, No 3, pp 11-17, 1961.
12. Alaka, M., "Aviation Aspects of Mountains," SJMO TECNN. NOTE, No 34,
1960.
13. La:rson, L., ''Observation of Lee Wave Clouds in the Jamtland Mountains,
Sweden," TF;LLUS, Vol 6, No 2, pp 124-138, 1954.
14. i.udlam, F. H., "Orographic Cirrus Clouds," QUART. J. ROY. P4ETEOROL.
5oC., Vol 78, 1952.
27
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UbC 551.509.616 -
5'I'A'fI5'CICAL INUICE5 OF 5J'ATIAL UIST1tIIlU'TION 0F PRECIPITATION IN TliE
I:XHRIMi'sNTAL MLTEOEtOLOCICAL I'OLYGON
MOyCOW ME'I'I,OROLOGIYA I CtUROLOGIYA in Itussian No 12, Uec 1978 pp 25-30
[Article by Candidate of physical and MaChematicul 5ciences V. M. Muchnik,
llkrainian 5cientific Reaearch Hydrometeorological Instituee, gubmitted for
publication 28 March 19781
Abstr.nct: Astudy was made of Che character-
isttcs of the precipitation field in the Ex-
pertmental Polygon oE the Ukrai_nian Scientific
Itesearch Hydrometeorological Ittstitute. The
presence of sCable local nonuniformiCies over
the territory of the ExperimenCal Meteoralog-
iral Polygon (EMP) is demonstrated.
[Text] The organization of the Experimental Meteorological Polygon (EMP)
with a dense rain-gage network made it possible to solve many problems
relating to artificial cloud modification [6, 8]. tn selecting the territory
uf ttie EhP particula* attention was given to the absence of significant dif-
ferences ici elevation, major rivers and water bodies as factors exerting an
influence on the formation of preripitation [8]. Btit disCurbances of the
precipitatior, field must nevertheless exist, since in the territory of Che
I:MP ttself and in the nearby areas there are major industrial cities (Krivoy
It~ig, Uneprodzerzhinsk, Zaporozh'ye, Nikopol') and large water bodies (Kakh-
ovskoye and Dneprodzerzhinskoye Reservoirs). As is well known, large indus-
tri:il cLties exert an appreciable influence on precipitation in the adjacent
cerritory [1, 3, lOJ. Accordingly, in the EMP it is possible to eapect the
_ existence of fi singul.ar areal distribution of precipitation.
I,. F. iinKatyr' and A. I. Romov [2], making a study of shower precipitation
(Intenslty maximum greater Chan 6 mm/hour and duration less tiian three
liours) during June-August 1960-1962, discovered "permanent" maxima in the
western and castern parts of the EMP which were separated by a zone of min-
imum precipitation.
'I'he existence of local maxima and minima of precipitation over the terri-
tory of the EMP is of considerable interest in relation to the problems
involved in evaluuting the effect;.veness of modification [5, 6, 81. For
28
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examp.lc, thone r.Fisey nf modificntion whiCh relare Co a Cerritory with n
lur.ri1 Mtiximum nn the nvrrrige kive rxnpqcrnted vnluep in compariynn with
11uiclLtleueionH ciirrlecl cul for u tcrrlCory with n.lucnl minimum.
The presence of loral maximg and mittima of precipitation nt distnnces of
10-20-kro from one anoCher is a faceor which must be tnken inCo account in
ydlving a number of pressing problems: long-range forecasCing of the quan-
tiCy of,precipitaCion, plttnning of snwn arens, predicCion of the probabil-
Lty nf obeaining n hurvest nf a gCipulared 1eve1, orgnnizaeion of irriga-
tion syseetns, etc.
The problem of the existence of local maxima and minima during the modific-
- ution period (Mciy-AugusC) in convective c1otids was examined using precipiCa-
- eion data collected ar posts in the EMP during 1966-1970. As demonstrated
in [4], the result of modification of well-developed cumulus clouds during
this time period was less than 1% of the mean quanCity of precipitaCion and
could not exert an influence on its distribution. Therefore, artificial pre-
cipitation was not raken inCo account. T1ie author also did not Cake into
nccount the possible influence of microclimaCe on the conditions for meas-
uring precipiCaCion, since during the setting our of precipitation gages
particular attention was given to the absence of such influences. When pro-
cessing the data use was made only of those posCs whose observation series
had no interrupCion during the course of this time. As a resule, the mean
density of posts was about 1 precipitation gnge per 18 km2. These data were
used in constructing maps of the monthly and seasonal (May-August) precip-
Itation sums for the period 1966-1970. The maps were used in determining
the poyitions of the centers of the precipitation maxima and minima as the
geometric centers of closed isohyets. In cases when the isohyets were not
closed at the edges of the map, the position of the centPrs was determined
approximately. The accuracy in determining the position of the centers of
the maxima for the most part was 1-2 km and was greater than the accuracy
for the minima, which was 2-4 km.
Table 1
bimensions of Areas of Regions and According to Fig. 1
I 00.78Ct11 n__1___
I 1 t
I II+ I
III+
I 1V+ I `1 I
I I_
II- I lll_ I
S n�x2 ~
196 I
274 I 184 I
78 I 732 I
I 66 I
250 I 972 I 1288
As can be seen from the seasonal precipitation map for 1966-1970 (Fig. 1),
tn the EMP territory there are clearly definable regions of maxima and min-
Ima. The isohyet 180 mm can be considered the boundary between zones of in-
creased and decreased quantities of precipitation and the isohyets 160 and
200 mm can be regarded as determining the principal regions of reduced and
?g
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tncreased qunntiCies of precipitation regpectively. [1lenceforCh Che re-
_ gtons nf increased gnd der.reased quanCiCies nf precipitation will be des-
- tRnntecl ny regiong nnd respeCCively.] Ae n reyult, ir way possible
t o tlet lne the Io11nw1nK rhqiony of increnqed quuntity oC precipitation
('Cnble 1) : I+ in the northwest, II+ in Che southwest, III+ in thc
iiorth, IV+ not closed in Che sourhern part of ttic EMP, and witli a re-
duced quantity o� precipitaCioci: I_ not closed in the norChwesC, II_
in the snuCh, III_ large, taki.ng in glmose u11 tlie eastern pnrC of
ehc EMMP, wiChin which there is a rather 1arge intermediaee region wiCh nn
_ inCrensed quanriCy of precipitnCion.
4102 zJo 2co:e0 re`o
~'fn ~,~ho
~
1- ~j j ~vry
Gad
.,,C f3S ~V
i90 'lY `v 1
^ i00 4" fd.�7
U ~
0 200 1C~ 70A 1S(' ;CO 1~0
Fig. 1. Seasonal (May-AugusC) precipitation map of Che Experimental Meteor-
olosical Polygon during pertod 1966-1970. Regions of quantity of precipita-
tion: increased 200 mm) I+, II+, III+, IV+ and decreased 160 mm)
Table 2
Frequency of Recurrence of Centers of Precipitation by tQonths and ParameCer
p for 1966-1970
L(CIITP
1
( ~,I 0fl
2
I HIOIIh
1
I ~1 H1,1h
h
1 A8fyCT
5
_
t+,
23
29
3�1
22
103
_-S
37
43
41
36
157
4t �6
a-s
r)
72
75
53
265
p
0,14
0,�10
11.45
0,33
0,41
ni
0,26
0.28
o,Xi
0.26
0,X5
pz
0.48
0,52
0,.57
0,43
0,47
Key:
1.
Cenker
2 .
May
3.
June
4.
July
5.
August
6.
and
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�
'Pable 3
Crequency of Kecurrcnce of CenCerg and of Monehly Sums of
I'recipitation by Itegions nf precipitation and in 1966-1970
t+
11+
III+
IV+

I_ II
_
II
I_
-
-
hlec~u 1

~

I

I
d

+ I - + I
-
+
1-
MaA
N
3 wNb
3
5
0
11
2
4
1
1
1
l
1
2
0
2
0
0
G
1:
2 I
O 1 0 (
4
G
7
6 12
Q Nant,
5
I
2
0
4
U
0
0
1
II
3
I
0 0 1,

U()
2
6
6
~3
12
13
i 14
3 19
S rarycr
h
i
~
0
~
i
I
I
I
13
1
n
~2
1i
u a 2

I5
a3
17 sa
= Key:
1.
Montli
-
2.
May
3.
June
_
4.
July
5.
AugusC
Tab le 4
Values
of p Parame
ter
and Its
Confi
den
ce Limits pl
and p2
for Che
Itegions
and

for
1966-1970
i m
M Q
U j
lv ef
Oo
n
t
P
~
t
:
1+
17
16
0,04
0,71
1,00
11+
16
13
0,81
0, ;4
0,94
III+
I.5
IU
0,67
0,38
0,88
1 +
51
42
0,62
0,68
0.92
11_
17
2
0,12
0.02
0,37
III_
ti0
15
0,23
0,15
0,35
91
17
0,21
0,12
0,32
r
Key:
1. Precipitation region
i.ocal nonuniformities of the precipitation field in the EhP territory are
extremely significant. For example, the difference in the mean extremal
cjuantity of precipitation in the northern parts of regions III+ and III_
, 31
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excocds 90 mm, thtit iy, iy cnmr.irnble eo the mintmum v,ilue in rehioi ITi_
(1.1H tnm) atd conyCltuCey about linlf the maximwn vulue in the region I1I+
(21.9 mm). Idith a distnnr.c beeween theye poinCs oE 16.4 km the grttdient of
Llte mean quanCity of precipieaeion is 5.5 mm/km, C1tnC ig, is pxrremely greaC.
We will nlso compare the mean values of the quanCity of precipitation by
~ir.~ay in region CI[+ and the norehertt sector of regidn tIt_, deeermined as
ehe means of Che values Eor individual posts. 'I'his gives values of 205 and
145 mm respectively. Since the uxes of region III+ and ehe ttorCherti part
oE region 1IT-aee -iented paralle]. to one andttier, Clie distance between
them can be determined apprdximaeely. IC was found Char the mean VaLUp9 of
the quantity of precipitation in Chese Cwo areas of nbout 200 km2, whoqe
cixes are approxi.maeel.y 18 km npart, differ by 60 mm. Sti11 greaCer differ-
ences arc obCained when cnmparing daCa for regidna I+ and II+ with daea for
regions Ir_ ttnd IIi_, the diyeance beeween which does noe exCeed 60 km. -
Now we wi11 attempt eo answer the main question as tu whether these regions
.ire a resulC of n rntidom disCribution of precipiCation over the Cerritory
oE the Erm or yome consenntly prevailing factors. For this purpose we wili
determine the frequency of recurrence of centers of increased and de-
creased quanCities nE precipitation from the monttily maps for ench
yeat.
According ro Table 2, the number of ceneers in Jure and July somewhaC ex-
ceeds their number itt May and August. 5uc}i a variaCion in the frequency
of occurrence is possibly attributable to the fact thaC in June and July
separation between periods of precipitntion is greater than in May and Aug-
uat.
Since only the appearance vf centers of precipitatinn of two signs is pos-
sible, their distribution is binomial. Accordingly, for solving the prob-
lem of the exisrence of local disturbances in the disCribution of the cen-
ters of precipitation it is necessnry to check the hypothesis of an invari-
.tbility of the distribution parameters over the Cerritory of the EMP. For `
this purpose ;ae will use the parameCer p- m/n, where m is the number of
- centers and n is ttie total number of and centers. For final
- ::.7mnles the p p,irametcr can be v.7ried in some limiCs pl and P2, sCipulaCed
hv the selected confidence level. If the local disturbances of the precip-
i.tatinn field in the EME' nre great and the rcgions of increased atd de-
creasrd quantities of precipitation ar.e atCributable to them, it must be
oxpected that for the regions the pl and p2 values will differ consid- -
erably from ttteir values for the regions. In particular, there can be
_ eases when the entire interval of pl and P2 values for the regions
wlll fall outside the interval of their values for the regions.
[n order to determitie the confidence limits pi and P2 we will selecC the
suE H ciently high 99"/, confidence level. These limits will be obtained from
tlie p and n values using the nomogram cited in [9].
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'rable 2 ghnwg thar the p value fdr the entire Cerrirnry of the CMP, de-
Cermined on the bagis of nll dnCa (n - 265), is equal to 0.41 wieh the
cdttfl.dence limiCs pl - 0.35 and pZ = 0.47. From month Co motte}i C}ic p
par;imeter tind ity COIIEidet1CC intervnls experienCe gmall changes. mhig
;aupporty Ciir hypothryiq thnC the cundiCions Eor Che Eorm;ition oC precLp-
LL:.Il:ioii in the t;MI' vary lirtle during Ctie period or time May-Auguyt.
Now we will proceed tn an examinnCion of the frequency of recurrence df
r.eneers of precipitaCion by oblages.
begpite Chc fact Chnt there were 51 centers for all monChs in all regions
wirh a qunntiCy of precipiCaCion greater Chan 200 mm and 81 centers with
Iess ehnn 160 mm, Cheir number for individual monChs is inadequaCe for
ubeiiining convincing values of the p parameeer fnr individual regions.
'Cherefare, we will uge dnCa only from the 1age line itt Table 3 for deter-
mining p for individuul regions (except for regions IV+ and I_) for all
months, ttnd also for 'Y+ and for individual monChs.
It follows Erom Tab1e 4 Cttae tlte frequettcy of recurrence of the for
regions of precipitation differs sharply from their frequency of re-
r.urrence for regiotts. '1'hus, the minimum p vulue for regions is
equal to 0.67 (region III+), whereas its maximum value for regions
is 0.25 (region III_). In addition, iC is faund that both for the toCal
region X + and for the remaining regions, cited in Table 4, there is
iio superposing of the pl-p2 intervals with Cheir values for the j; _ re-
;;ion and the remaining regions. These dara make it possible to asserC
l�hat the conditions for the formaCion of precipitaeion over the CerriCory
uf tlie regions differ greatly f rom the cnnditions over the re-
};ions. In actuality, if it is assumed that the observed distribution of
centers of precipitation is random, and not due Co any local effects, then
the p value for the entire territory of the EMP is equal to 0.41 and falls
tn the confidence limits pl = 0.35 and P2 = 0.47 (Table 2). Comparing
ttiese vttlues with the values in Table 4 for individual regions, we see that
tn this case a.s well the confidence limiCs pl and pZ for all the re-
gions fall for the most part above their values for the entire area of
the IsMP, but for regions lower.
Now we will discuss the problem of the sCability of the influence of local
factors on the formation of precipitation over the territory of the EMP
with time. For this purpose we determine the values of the p parameter
:ind its confidence limits for the total regions of precipitation by months -
on the basis of the data in Table 3. -
According to Table 5, the value of the p parameter experiences relatively
::mall c}ianges with time both for the 71 + regions (from 0.75 to 0.92) and
for the 2;_ regions (from 0.05 to 0.33). At the same time, the intervals
I)1-p2 for the regions Z+ and V_ do not overlap one another for the per-
tud June-August. Therefore, it can be assumed that for these months there
ts a well-expressed and constant influence of local factors on the condi-
tions for the formation of precipitation in the territo*y of the EMP. A
33
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Komr..whnt more unr.errnin problem is l�hut of the existence nf such an influ-
"Ice iii Mny, sittr.e c:he P11-p2 intcrvnl:i Eor ttic Z+ und Z_ region5 overlap.
I t!.y possi.ble tlint the reution f.or this uncertainty is the extremely sma11
iiumUer nf dbservationy o!' cenl�crs of precipitaCion for the X+ region,
w}iiC}i is cnused, as menCioned above, Uy the relaCively sma11 "breakdown"
a� Clie precipitatinn field itt Mny. Thus, the daCa in Table 5 make it pos-
sible to assume Cliat the 1oca1 Lactors exert a constanC effect on the con-
(litions for formation of prer.ipitACion in the CerriCory of the EhtP during
ttie eneire period of modification of convective clouds (Mny-AugusC).
Tab le 5
Values of p I'arameter and il�s Confidence Intervals pl and p2 by MonChs for
Total I'recipitation Regions for 1966-1970
2
3

5
I:ey :
hlecAU 1
s,
'

n I
m I P I
P, I
P: ~
n I
ni I
P I
Pi I
P,
Ma1
S
6
0,75
0,35 )
0,97
18
6
0,33
0,13
0,53
Lltoub
IG
13
0,8I
0, :6
0.96
21
7
0,33
0,14
0,57
btwnb
12
11
0,92
O,G'l
0,94)
22
d
0,14
0,0:3
0,36
Anrycr
15
12
0.80
Q,5'l
0,96
20
I
0,05
I 0,01
0,29
Manth
2. May
3. June
4. July
5. August
Now we will makE an attempt at a qualitative examination of where the sources
of modification for the formation of precipitation should be situated. in
the territiory of the EMP.
'l'lie regions I+ and II+ are adjacent to the territory of Krivoy Rog and it
is natural to assume that specifically the peculiarities of a large indus-
- trial city exert an influence on the formation of precipitation. The influ-
cnce of sucti cities on clouds involves, primarily, first the initiating
effect of the heat island over them with ascending currents in the limits
10-40 cm/sec, and second the effect of an increased content of condensa-
tion nuclei in the air [7, 11]. Therefore, it can be assumed that the rea-
son for the formation of precipitation regions I+, II+ and IILE. is the in-
Fluence of Krivoy Rog.
'('he existence of extremely large gradients of the quantity of precipitation
for a montii and for a season and the small values of the mean monthly sums
(aUoiit 30 mm) in the regions of an increased quantity of precipitation is
- the basis for raising the question: is there a redistribution of precipita-
tion over the territory of the EMP during the warm season o� the year?
34
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r
.
FoK UPF'tC t A1. U5N oNLY
Iq the increane in preripitation near l.drge cities not accampanied by a
decreuve in precipitatiott at nome distance from thege cities? If there
;ire reasons f.or ttie more frequcrnt and more inten4ive re.olution df cumiilo- _
ntmbuy rloudg ncnr ritirs, tliiy tn rrnponsible for .1 decreaye ln khe iiumi
I,er of r.ases af their resolution at some diatance frdm the Cirieg. If this
hypothesig is true, then prior to artifirinl modification durittg the warm ~
veuson of ttie year ttie following problem drinegs aceomplistt modtficatidn
tn such, a w.zy to eliminate, ittnofnr as pogxible, the unfavorable influ- _
ence of a clty on ttie diFitribution of precipitation near it.
In conclusion, I wish to expresa appreciation to M. V. lluykov, A. V. Levin
ind B. Ye. Ntshman for uHeful discuggion oE ttie work.
llIE3LI0GEW'liY
npy.ilyamava, Z. G., 7vorykina, 0. Il., Sokolova, N. G., "5ome i'eculiar-
itiex of t1ie 5patial-Temporal Uigtribution of Considerable I'recipita-
tion Over the Territciry of Moscow and Moskovskaya Oblast," TaUbY TsVGMO
('1'rrinsartians of the Central Volga 1lydrometeorological Observatory),
No 2, pi) 83-94, 1973.
IioKatyr', L. F., Rnmov, A. I., "Ttie Influence of Mesoscale Temper.hture
Intiomogeneity of ttie Underlyittg 5urface on 5ummer ConvecCive precipit-
ation," TRUDY UkrNIC,MI (Transactions of ttie Ukrai7ian Scientific Ete-
search Nydrometeorological Institute). No 61, pp 106-113, 1966.
J. KI,IMA'I' Mc)SKVY (Climate of Moscow), edited by A. A. ihniCriyev and N. p.
13essonov, I.eningrad, Cidrometeoizdat, 1968, 323 pages.
4. Korniyenko, Ye. Ye., "Evaluation of the Possible Quantity of Additional
Precipitation Under the Infl.uence of Solid Cancon bioxide on Cumulus
- Clouds," TRUbY UkrNIGMI (Transactions of ttie Ukrainian 5cientific Ite-
search Hydrome[corological Institute), No 92, pp 72-94, 1970.
5. Korntyenko, Ye. Ye., "Artificial Regulation o� Precipitation," TRUDY
UkrNIGMI, No 131, pp 3-24, 1975.
0. i,eonov, M. P., Perelet, r. I., AKTIVNYYE VOZDEYSTVIYA NA OBLAKA V KHOLOD-
NOYF: POI,UGODIYE (ArtiEicial Modification on Clouds 'in the Cold Half-Year),
i,eningrad, Cidrometeoizdat, 1967, 152 pages.
7. N1:11Riil)NAhtER1:NNYYE VOZDFYST'VIYA NA KLIM/1T (Inadvertent Fffect on Cli-
m:;te), Leningrad, Cidrometeoizdat, 1914, 260 pages.
8. I'riklit'ko, C. F., ISKUS5TVENNYYE OSAbKI IZ KONVEKTIVNYKH OBLAKOV (Arti-
ficial. Precipitation from Convective Clouds), Leningrad, Gidrometeoiz-
drit, 1968, 173 paRes.
35
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9. Kliari, G. , Sh1p i ro, 5. , 5'f,`7'I5TICli1:5KIYC MUI)I:LI V IN'LNI.NEEtNYKH zAUACII-
Af:N (5tntt4tical Mddel:i in Enp,ineering 1'roblemg), MoHcoc+, "tiir," 1969,
395 pFiges.
10. Iluff, F. A., Cliatlgnon, S. A., "Climatnlogical A�nes4metit of Urban Ef-
fecte ott I'rer.ipttation at 5t. Louis," J. AI'PL, Mi;'I'L�'OitOL., Vol 11,
6, rp 823 P42, 1972.
11. LandraherR, 4., "tnadvertent Atmoepheric Modificcition Through Urbaniz-
atton," WEATIi};k ANU CLIM11T1: MObIFICATION, New York, pp 726-763, 1974.
36
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A
UbC 551.509.615:535.361.1
INCItLA5E IN TNE VI5II3ILI'I'Y ItANGE 0F LA5EK I3CACON5 IN AFOG
Moscow METEdROLOGIYA I CIUKOLOGIYA in Rusgian No 12, Uec 1978 pp 31-42
(Article by Candidate of Physical and Mathematical 5ciences 0. A. Vo1ko--
vitgkiy and V. i'. 5nykov, Institute of Experimental Meteorology, aubmitted
for publication 20 March 19781
Abgtract: Ttiis paper gives the regults of an inves-
tigation of t}ie intengity of scattered radiation of
a NeNe laser propagating itt a droplet �og with its
evaporation by tlie coaxial beam of a C02 laser. Dur-
ing observation toward C'~--. :ay it is noted that the
evaporation of droplets itt Ctie af fecCed zone leads
to movement of the znn( of maximum inCensi.Cy of scaC-
tercd visible radiatinn in the direction of the ob-
server. T}ie results of the experiments and computa-
tions were in good agreement. Expressions are deriv-
ed which make it possible to establish the correla-
tion between the intensity of a C02 laser and the
range of movement of the zone of maximum intensity
of scattered radiation of a 1{eNe la:;er. It is sliocrn
that for a substantial (by several times) increase in
the range of detection of a laser beacon under the -
conditions prevailing in a real fog it is necessary
that the radiation power of the C02 laser be several
tens of kilowatts.
[Text] At the present time there has been extensive development of optical -
~ystemh for KIgnating, transmission of information and navigation based on
lise of laser radiation. A serious limitation for Che use of optical systems
operating throug}i the atmosphere is the presence of fog and clouds. The de-
tection of signal lights and orientation by ray in fogs and clouds are made
(Iuite difficult or become impossible since over a quite extended path the
radiation energy can be virtually completely scattered by cloud elements.
[n order to increase the range of detection of a light ray in fogs and
i�louds the authors of [21 proposed a method based on the fact that beams of
visible and infrared radiations (sucii as that of HeNe and C02 lasers) are
37
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~ u;ixl;t l ly dlrrr.tvii towiiYcl thv ohyoYVrY. 11y a rrsult (iC the rffrrt tif 112
I ,itIfiil Itiu ;i i ighl ruy lN yl lKlit ly Hrnttereil 1tt a I't- lrarocl" zonv ,incl Ur-
cnne,-t viqiblc, a;a ;t reyult of aeersol scatterf�g at a diql-anCe where the
ovaporation of C1oud ClE1f1F'ntg decreaqes.
Wv will examine ttie 1awq of change in the intensity nf sounding radiation
tiratcered in ttie zcme of effect nf a be.7m of COZ laser and we will evaluate
the pogyibility of a substatttini increage in the visibility range for laser
beacons in a fog nn ttie basig oC gCaCtered light.
'ormulns for Computtng 5ounding Itadiation Scattered in AffecCed zone
The tntentitty of ttie radiatinn nf n NeNe layer scnttered by an elemeneary
volume 4 Vof .i homoReneoua cloud medium with an attenuation coefficient
CtAn sIt tlle angle 0� to the dirertion of propagation of radiation, regis-
tcred by a receiver situated nt ttie diStanCe t from the boundary of ttie
medium (F'ig. 1), in the single scattering approximation can be evaluated
ii:3ing the datn in studieg [6, 8, 121.
'I'lie expression for thc intensity of scattered radiation I;k (A normaliz-
ed to I;\(), taking into account attenuation along Che ray path to the scat-
trring volumc A V and from Q V to t}te obgervation point can be writCen in
t tie form o y
~ ,

i, _ (00) xx J(00) e`- ~ x* sln ric ) sin~ 4' x z
~ o a _ tl ~ d~ }
, o
where f(0 �)/4ri is the normalized scattering function for rndiaCion in a
homogeneous cloud medium;
CPX ~ r 1
is the angle of divergence of the ray of a HeNe laser.
z,
I
/
9
- i'iK. 1. Schematic representation of arrangement of sounding ray and radiation
detector.
In the affecCed znnr the microstructure of the cloud medium is inhomogen-
cous. In order tn determine the fiel.d of scattered radiation in the neiRh-
borhood oE the beam nf a C02 l-iser it is necessary to take into account the
taws of change of microstructure caused by the exposure.
38
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,1n approximate exprewyion for determining the radiati()n intettgity nF n }IeNe
1aser, `qcattvred lt' tlie "clearing" znne fcirmed in a Itdmogeneous Jroplet
rloud rneditim by tile cdtitinuoug radiation df a COz lager I;1vis (o Can be
written uging an nnalytical desCriptidn di the lager action proCeSg examtned
in (31 witli ttie fnllowing assumptions. We wi11 aggume that the t'atio of the
trangverse dimengionn of ttie clearing zone dp and the diameter of the sound-
ing riiy d a o ig guch that the rnicrogtructure of the medium within the limits
oE the transverge section of the goundtng ray is uniform and we wi11 aggume
that the optical gcattering gection under Che influence of the C02 laser
radiation changes due to a decrease in the size of the droplets althdugh
their concentration remains the yame. 'Chen the expresgion for I;x vi'q(8
I a o will tiave the following form:
A
ak W. s) dx' o =1
~~'"re 1 I 0~
r~A_.~. ~ QA~x~ Z~~ ~ Q ~ x
" ( 1 ~"o sin o� sin~ 9�
o :
1 (z)
x �v
C, + p,x
(ii = vis, �X a
.ind fvi.4(D �)4m is ttie normalized scattering function of radiation itt the
affected zone; z is .n coordinate determining the positiott of Che sounding
ray in cfle beam of a C02 laser (with coincidence of the axes of the heams
i - 0).
On ttie
ratio
After
wliere
basis of (1) and (2) it is possible to write an expression for the
of intensities of the radiation scattered by this elementary volume
and before the action of radiation by a C02 laser.
s011 i c. :l I. Itl
(9� r ~xo f 109
AsJ (Z) = t;o - t,. = aya x--- I a, (x', z) dx'.
(3)
Tlie values �`a (x, z), ta(z), AtA(z) entering into (2) and (3) can be deter-
niined using Eormulas 13, 41
r �o
ta(z)= 1 2 \e 3 +3
In
Tp ~ l, (e9(s)--1) e tA�T~J'/J--1 + (4)
- + V3 arctg ~ - arct 1~'3 �
g
I Z[i -3-(te(z)--1) e- --A� (5)
r~,r 1+2e 3
aa (x. z)
l~ + - I ) e �ao *10.c
J
39
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wliere the thermal efEect functinn iq
Cp, t -
~(t) = 2 `,_roV ~ ~..~ff
~
- lo R�t + 3)
1 f~(N+I11N+21
lle re C r 3 A~ ~T ~r ,
q p7--,
(T = hEat; p- gcatJ i, ig ttie heat of evaporation; I'o is Che itttenotity of
the COZ lnver; ro in the radius of the beam di thc COZ lagcr at tlie inten-
sity level I- io�e-1; 2�lU3 cm-1; v is wind veloeity; /~t' ,
iire coefficients taking ntd ecCOUnC the energy loages di the c6~tlager sCat
in heating of ttie gurrounding medium and scattering of radiation by a drop-
let roedium; itpZ is ttie mean square radius; � is the parameter of gamma dis-
trtbutidn of droplets by gi.zes. For Tp = 293 K, I= 100 IJ/cmZ, itaZ = 5�10'4
cro, A hent ^ 0. 75, Q gCgt A~ 0.6.
The normalized scat[ering functions f(B 0)/4rr and fver~~ Att for the in- -
itial microstructure of ttie droplet medium and the droplet medium in ttie
:iffected zone r.an be found from tableg or graphs with known droplet dis-
trihutton parameters itg and f.t . The Rz values in the affected zone can be
- r.omputed uqing the formula _
- Rz (x,
, ~ ~---TpoA ~.t FI/ (s)
C .
derived from (S) with the asstirnptions made concerning the optical section
on the basis of obuious considerations.
Table 1
fl' I A I Rs NKAf
~ �m
2,0 64 2,0
2.5 4U 1,6
:f,U 2!) 1.4
4,0 li 1,2
5,(1 12 1.1
In carrytng out the computations it is not entirely convenient to use a
grarlitc or tabular representation af f( 9�)/4rr as a function of micro-
structure. In this connection it is desirable to find an approximation of
ttie depetidence of f( 8�)/4,n on R2. A satisfactory approximaCion of this
(ici>enderice Eor small observation angles With RZ < 7�,m is the function
R=
I(G� - const ) R, z-
R, (9)
� '4 (K. ~ e '
4 n
40
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in whieh the conxtants A and R* can be geleCted in dependence on the nb-
gervation angle and the parameter Fdr b the Aand it* valueA nre
;;iven in Table 1.
Ttie error in computing ehe function using formula (9) in comparigon with
the precige value in the range of change of radii 1.5 >loyed. The direct radiation was registered using a Fb-24K photodiode
(point C). The photocurrent from the radiation detectors, after amplif-
_ ication by logarithmic amplifiers, was registered by a multichannel auto-
matic recorder. The angular aperture of the deeectors did nor exceed 6';
_ this made it possible to measure the coefficient of radiation attenuation
witlt a sufficient accuracy [7]. The total error in determining ~Ao did not
exceed 97 when cXa 0 = 0.1 and 12 when x;x0 - 0.8 m'1. Measurements of scat-
_ tercd radi.ytion were made in a broad range of change in the aCtenuation co-
efficiettt, whose value attained a ao = 0.7-0.8 m`1. As demnnstraCed by
investigations of scattering of radiation in an optically dense medium (9,
101, with values aAp > 0.4 m 1 the contribution of multiple scatCering to
the tot.71 r~ndiation flux could become substantial. In addition, an inter-
Ference in the registry of low levels of scattered radiation was the back-
};round caused by "outside" illumination of components of different measur-
tnA apparatus. The contribution of multiply scattered radiation to the
total flux of registered radiation, generally speaking, can be computed,
l,ut, as experience has shown, one variant of computations of the field
of multiply scattered light by the Monte Garlo method takes about 100 hours
tin an M-220 electronic computer [11). This makes such computations undesir-
. :ible in routine work.
In our experiments allowance for t1ie influence of multiply scattered light
and the background from sources of extraneous irradiation was made by di-
rect measurements of the scattered irradiation by the receiving system,
41
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- on whir.h the flux df singly qcattered lager lighe was noe inCidettt. In the
computationq we a5gtlnted a ratid of Che light Eluxeg -
y..._P" ,y ....P~ . f'A
~
i I
(ld)
( NJ Pt = meag; ~P = baCk(grouncl) I where i' a m~ ( 8�) is the radinCion flux
registered by ttre detectdr ~~e the paint g; ~A baCk ig Che flux di the
background of mulei.ply scaetered lighe and "outside" irradiation; I'a O
Iq ehc light flux ot a iieNe laser, useO in the experiment (p a0 = 5�10"'2
W) .
'I'lir rontr�ibution of the aback/PAp value to the ratio nf the fluxes
I' m~,� y((~ �)/Y a p began to he manifested aignifiranrly when I' A back/~' k 0
- t 10" (with vnlueg aaO >0.4 m`1). 'Che baCkground value wag PT back y
(2.2-3) -10-11 W.
I`or r.nmparing the experimentally measured fluxes of scattered radiation
with the romputed intensity values it is possible to use the expression [61
eh :t ~o
pr, (0�) 0
~ ~a Sii 1 + dk ~ stn N,
/
f' (11)

~ o S~ a I 1-F J, sin 0' )
~
where
4 Aw, d;
~
is clie field-of-view angle for the receiving objective; dtjn is the solid
;ingle of the field of view receiving objective; f is its focal lengttl;
d{ is the diameter of the field dinphragm;
z
da = d)� (1 + r
Is thv dtame[er of the sounding ray at the distance x with a divergence
;inglr
- _ ~ 41_,. ~
:ind tlte init ial diameter dAO; dtJA is ttie solid angle of the sounding ray;
Is the rrn;;s-sectional area of the sounding ray at the distance x; Siy is
ncc area of the projection (a[ the angle 5Pn) of the field diaphragm onto
the rav.
'1he sr;lttcrtng volume 6 V, entering into (1) and (2), formed by intersection
of the two conc~s, has a complex configuration. However, under the condition
tliat the effective dtameter of the receiving objective dnZl exceeds the ray
42
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d tnmvter dA X nnd rni Chr asqumptinn thnt d,,,X ~~nd dnr v,nry lieele wit}iin
tl~r !NV L1mItN, tht, ;-~rrittrr.tn}; v~~lumr c~rui hr rc~m~~utrci 1
t'~~rmu 1 r~ npprnximatrly u.atnk,
I -A V,~ r da s dnr1 (12)
~ 4~ SIt10� ' -
where '
sln~Uo -
d"r~ V d" C1 _t. d� m t
dn is the dinmeter of the receiving ob3ective. -
ide note thar Che 6iV value, computed using formula (12) wiCh 90� in
the moet unfavorable case, when dAX= dnzl, will exceed the A V value =
found uyink thc more precise formula A V= 2/3 dJ*% X by less than 1$%. When -
d"'Ll -
s~n U~ ~ 2 da x
the error in computing G1 V will not exceed 5%.
PA fe7, paI (e1
~ ~ ~ v{ q
Q ooa ~ o 0 0 0~
101 e~
0
0
0
JO** F \ �
0 0, 4
6)
~
RB a 42 44 46 IrAp
Fig. 2. bependence o� flux of radiation scattered at an angle e� = 5� on
:Ittenuation coeffioient aa0. 1, 2) results of ineasurements of p~ (e o)/
lox 0`'~nd P a vis ( ~ )/P ,\0 respectively; 3, 4) computations under conditions
I,o ig aetenuated in accdrdance
with nouguer'g 1aw, in the affecCed xone Co some -`~ko values there is a de-
c:rense itt the flux of gcatCered radiatibn cauged by a decrease in the np-
tica1 seceion under the influence of the radiaCion of a C02 laser, arid '
then witli an increase in 01;kd Chere ix a greater, in comparison without
such an effect, flux of scatCeYed radintiott.
'I'he dependence of the rario of fluxes p),vi ( 9�)/p ( 0") on the attenua-
tion coefficienC aA0 for Chrep positiong o~ the scattering volume on Che
beain axis (x = 12.0, 7.4 and 5 m) ig shown in Fig. 3. The figure shows
- that the flux of scattered radigtion from the affected zone increages by
'L or 3 orderg oE magnitude with the a Ao values, power of the COZ laser and
geometry of the mea3uring sygCem used in the experiments. It fnllows from
the cited data that by means of the effecC of the radiation of the COZ
taser on Ctic c.inud medium there can be a substnntial improvemenC in the
visibility of signal lights in a fog at consideruble distances from the
radiation source.
- Cstimating Radiation power of C02 Lasers for Improving Visibility of Laser
- Be.iCUt19
.1n analysis of equation (2) shows that the inCensity of sounding radiaeinn
scaCCered in the affected zone at the nngle 0� attaine a maximum value at
- some distance xmax from the beginning of the patti. The interrelationship -
between ttie distance xmax and the power of the affecting radiation can be
established from an expression derived after the differentiation of (2),
equating it to zero. Thi.s expression will have the form
2 (Cn (s) - I) P--a~~rllXmix~f (X~ 1l-}-
~ k~ r J (13)
fs (0�. .rmI110 -
~ Ia ( 0�. -imax ) = 0.
Using an approximation of the scattering function in the form (9), (13) can
he transformed to the form
3 tl +Q.1' 13 R,r; 1 (14)
where i a .o,Q, 4 R. (1 + QI)113 =0.
Qt = ~e0 ( ) - ~ ~ B a ,o r'*xmrR~
(1$~
45
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ISy means oC replar.inf; (1 + Q1) = y3 (t4) iy reduced eo a fourth-dep,ree
V qun t tnn
y ~1 -
,
y' y 4+ .4 a. ' - 0' (16)
Table 2
141.11~ Y III In Q,
3 1, 795 4.689 1,545
- I,G2S 3,28i I1In)
i 1,liU;) 3,I39 1,144
An annlysis of thi.E; equation shdws that it has two fiCtitious and two real
roots, only one of which saeisEieg ttie condition of tlie problem. The values
of this ront with e� - 2� are given in T'able 2.
_ Ninding ttie roots oE equation (16), from (15) we obtain a simple expregs ton
rclatin}; xmax 1nd ttie thermal ef fect fuitctioct e(z)
5~~ Ie~ ~ t~-- I (17)
'Xrno~ = 4 yp fl Ql ,
where 5M is the meteorological range of vigibility (5M:z:4/�CA 0), correct
for D(z)> 0.7.
in a case when e(z) 1, iC is possible to write
sN
amsx = 4 y^, [0 (Z) - Ifl Qll. (18)
Graphs oE the dependence of B(z) on xmax are given in Fig. 4. The distance
:it wllicti Chere will be registry of the radiation scaCtered in the affected
zone, iE ta vis(O exceeds some Chreshold inCensity Ithr, exceeds the
%mnx value. 1'his distance xreg can be evaluared using the formula (if zl =
~t)
xreg'-- x4nax + Xthr,
(19) -
where
xthr - S"-- in f; (�C = 0, 6')
- 4 rp /nop
ls found from the consideration that at ttie distance xthr from the source
tlte inteiisity oE ttie radiation scattered in the fog wiCfiouC an effecC is
.ittenuated to Ithr� As an illustration we have given the results of com-
ilutntions oE several specific examples of a change in scattered visible
rndiation propagating in the fog along an extended path in the zone of
- :irCion of the C02 laser.
46
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B(Z~r
70
0 1i 0 (mCx AfN
rig� 4. bependenct! oE ttiermal effect function on xmax for different fog
microstructureq for 5M = 200 m. 1, 2, 3) RpZ = 3, 5 and 71Am respectively
6).
Table 3 -
~ b U ~ 31 d _
k t~i tl 1 ~
4 v C I~~ ~
I 5 2 0 2,5 1593
2 25 J O J (2]4
3 32,5 13 10-1 2.5 24:i
4 65 I 13 10"4 5 490
Key :
a ) kW
b ) rad
c) kW/cm
d) W/cm2
Vow we will examine tlle change in the patterns of scattered radiation
Erom the beam of a HeNe laser caused by the effect of C02 laser radia-
tion on a fog, whose optical density is characterized by a meteorological
range of visibility SM = 200 m( a a o = 0.02 m 1) on a path with the
47
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l.engrh = 2 lcm wiL-h a wind velocity 1 m/sec at a CemperaCure 'I'� = 20�C.
We w.tl.l assume that ttie microseructure o� the fog is characterized by a
gnmma disCribut3on o� droplet sizes with ttie parameters R02 = 5�m,
- 6. 'Clie compuCaCions are made For a case whett the observer moves parallel
to ttie ruy nt ttie disrance zt (see Fig. 1) and registers the intensity of
:icaetered radiarioti at the angle e� at rtie distance x+ zl/tg 8�. We
5elect ttie angle of ray observation quire small, sucti as B�= 2�, since
in the case of small observation angles the increase in rhe intensity of
scatrered radiation as a resulC of'an increase in the function f(0 �)/4rr
exceeds Che attenuation of scarCered radiat�ion at the distiance AB = zl/
sin 0� from the scattering volume to the observer. The specific Po and dp
_ values for the nondiverging (cp= 0) and diverging beams (the divergence is
iissumed to be rlose to the diffracrion value), used in the compuCations,
are cited 3.n Table 3.
'I'he paramet;ers of the sounding beam are selected in such a way that the
, diameter d a 0 is miich less rhan d0, divergence does not exceed the dif-
Fraction level and the intensity I a is equal to 1 W/cm2. Under these
c:onditions in the first example P a = 0.1 W and d a p= 0.36 cm; in the re-
niaining cases P 1 W and d \ 0= 1.13 cm.
A laser ray can be detected from sirgly scattered radiation if its inten-
5ity at tlie observation point exceeds the background level caused by out-
side irradiation and multiply scattered radiation, and also exceeds some
threstiold illumination whicti can already be discovered visually or using
_ zin instrument. In compuCations of the intensity of scattered light, in
(1) and (2) we assume ~Pn= 61, which corresponds to the mean angular
resolution of the eye. We will not take into account the background irra-
diation, wliicli in principle can be eliminated using interference (constant
background) and polarization (multiple scattering background) filters,and
we note that ttie threshold illumination for a red color, clearly distinguish-
- able to the eye, applicable to the conditions for nighttime signaling in
aviation and navigation, is Ithr = 6�10-14 W/cm2, and the absolute light
threshold is Ithr = 3�10'16W/cm2 [5].
?dow we will examine the conditions under which the ray of a HeNe laser will
be observed in the neighborhood of the affected zone. We will assume that
Che observer is situated at the distance zl = 10 m from the laser ray. The
results of computations of the ratios of intensities of the scattered radi-
arion
I'kver(A �)/IN (x = O.e 0), I;~ (x, 0 �)/I 7,(x = 0, 6'0)
_ [B = vis] (left scale) and the intensities of scattered radiation I T vis
(k, 9�) and I;,( j , 0�) (right scale) are presented in Fig. 5. It can be
:,een from tlie graphs that with the selected geometry at a distance ,Q ;:Z;~ 600
_ in f.rom the radiation source the observer ceases to distinguish the ray of
:i HeNe laser with the intensity I T 0 = 1 jd/cm2 in a fop with a stipulated
_ rittenuation coefficient (aa o = 0.02 m'1). The effect exerted on a fog
as
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la e') e�~ t f c, e~), lts (t, e~emlcr,t W/cm"
s
10'~t
r
d
f0'1$
fo70
a,s 7,0 1,5 1 KH
Fig. 5. Uependence of functions I a(x,9
IT (x '0, e*) , I\ ver(x� 0 ')/I a(x = 0, 00)
(left scale) and intensity of scattered radia-
tion I;k ( 1, , 00), I,Aver(i, e�) for zl - 10
ei (right scale) on x,respectively. 1-4) saroe
as in Table 3; 5) Pp = 0. I) threshold inCensity
for red light applicable to nignrtime signaling
conditions in aviation and nuvigation; II) abso-
lute light threshold.
48a
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FUIt 11F1-ACIAL 118I? ONI,Y
wlvit tltc wind vrl OVt ty iH l m/yuC f ii t IiE' ,"i," ,If the heilm o C" COl 1nKvr
wl tlt ,z puwer oC32.5 KIJ, dC~ = 13 cm, y' = 10"1 ' rnd makev t tpossib Ie tu move
ChiH ltvel of the intengity of wr_attered radiation to the digCunce f z: 1,100
m(Fig.' 1). A better effect in ar.tained uging the benm of a C02 l.hner with
a power of 65 kW with the same divergence or using n nondivergent benm with
.i power of 25 kW (.Q ft 1,500 nnd 1,900 m respectively). The computationy
show t}iat nt e}tc digtance wtiere scnCtered radiativn begins to be di8Crimin-
7ted the intensiry of the direct ei'fece of sounding radiation is reducEd
to gafe limitg.
'fhe time in which a st.ntionury sCate of fog clearing is establistied, lead-
Ing to an improvement in the visibility of laser tieaCOtlB, can be cytimated
using the expregqion t- do/v. In our exampley it will not exceed 0.13. It
therefore follows tftat a considerable (by upproxitrtately an order of magni-
tude) decrease in the metin intensity of ehe effecCive radiation Can be
attained by the use of pulged sources c,iCh a pulse lengClt t-0.15 sec and
with a pu.1Ke duty Eactor of nbouC 1.5 sec. `
t,hanKes in the distance zl from the .laser ray, observation angle nnd geo-
metric,1t narameters of the receiving syytem, attenuation coefficienC aA
~
nnd other partimeterK le~nd tc~ different quantiCative estimates. It must be
uoted that a decrease in the temperature of the medium and an increasc
In wind velocity, all other conditions being equal, cause a decrease in
the effect Erom the radiarion. An increase in Che intensity of the radia-
tion neceswary for compensnting the influence of these factors is easily
estimated �rom an analysis of the expression for the thermal effect func-
tion, from which it follows that with D(z) = const the effect will be
tdentical.
'l'he results of computations of the intensity of scattered radiation in the
- iteigtiborhood of the zone affected by the beam of a C02 laser, cited here,
indicated the fundamental possibility of increasing the range of detection
of laser beacons in a fog on the basig of scattered radiation by the method
proposed in [2]. The formulas derived in tltis etudy make it possible to
niake the necessary evaluations of the intensity of scattered radiation
For o[Iier me[eorological situations and for the parameters of beams of C02
l:isers, whicti can be used for increasing the effectiveness of specific laser
uavigation systems.
The auttiors express deep appreciation to A. F. Nerushev for useful discus-
sions and A. C. Petrushin for computations of the scattering function.
BIBLIOGRAPHY
1. Borovskiy, N. V., Volkovitskiy, 0. A., "Large Aerosol Chamber," TRUDY
IPC (Transactions of the Institute of Applied Geophysics), No 7, pp
5-12, 1967.
49
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Vo1kovl.rskiy, 0. A., Mamonov, V. K,, 5edunov, Yu. 5., Semenov, L. p.,
5krlpkin, A. Dt., "Mr.thod for Optt.cal Stgnali�f; in a Fog," AUTHOR'5
Cl:lt'I'1V1CA'1'I; U551t Nn 5277299 dated 71 Fehruary 1975.
l. Volkovitskty, 0. A., "Approximate Annlyticat nescription of tfie E:tfect
of ` COZ i,,iser on a nroplct Cloud Medium," TRUnY ICM ('I'rangaCCintts oE
the InvCitute of Experimentxl Meteorol4gy), No 18(71), pp 23-33, 1978.
4. Volkovitslciy, c). A., "C}intige in 'Crnnsparency of att Aqueous Acrosol
iit the Wave.tength oE 5otmding Rndiation in the 7.one of its Clearing
by a I1eam oC a COZ Laser," ItAnIOT[:KHNtKA I i;LI:KTItONIKA (Etadio Lngineer-
inK aid Llectronics), Vol 22, No 7, pp 1379-1383, 1977.
:i. Cavrilov, V. A., VIDIMOS'I'' V A'I'M45FI;itI; (Atmospheric Visibility), i.en-
lngrad, Gidrometeoizdat, 1968, 324 pages.
b. Cershun, A. A., "YhoComeCry of Turbid Media," I7.IlI2ANNYYC 7'EtUDY YO r0'TO-
ML�"I'ItI2 I 5V[:TOTi,K}{NIKf, (5elecCed SCudies in the Field of Yhotometry and
Ligtit I,ngineeri.ng), Moscow, Izd-vo Fiz.-Mat. Literatury, pp 85-113,
1958. -
7. %uyev, V. Ye., I'ItOZRACHNOST' ATMOSFCRY bLYA VIUIMYKH I INFKt1KRASNYKH
1.UCHCsY (Atmosptieric Transparency for Vlsible and IR Rays), Moscow,
"Sovetwknye Radio," 1966, 317 pages.
8. 1vanov, A. P., OE'TIfG1 EtASSEIVAYUSHC1iIKH 5RED (Optics of Scattering Med-
ia), Minsk, "Naukn i Tekhnikn," 1969, 542 pages.
9. Ivanov, A. P., "131urring of a Narrow Light Beam in a Scattering Medium,"
'JZAIMODLY5TVIYE NERAVNOVESNOGO IZLUCHENIYA S VESHCHESTVOM (Interaction
tietween Nonequilibrium Radiation with MaCter), M.tnsk, pp 84-94, 1965.
10. Kabanov, M. V., "Optical Transfer Function for Scattering Media," IZ-
VCSTIYA AN S5SR, FI7.I1G1 ATMOSFERY I OKEANA (News of the USSR Academy
of 5ciences, Physics of the Atmosphere and Ocean), Vol 4, No 8, pp
835-843, 1968.
,
11. Ozerenskiy, A. P., Romanova, L. M., Snykov, V. P., "Light Field in an
Aqueous FoY Outside the Ceometric Zone of Propagation of a Collimaeed
l.riser Ray," TRUDY IT:M, No 13(58), pp 147-161, 1976.
12. PROZHCKTORNYY LUCH V ATMOSFERE (Searchlight Beam in the Atmosphere),
Moscow, Izd-vo AN S5SR, 1960, 244 pages.
SO
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' FUIt c111'VtClAl, ISL r1NI,Y
UbC 551.(513.2:510.534)(215-13)
5F'ItING at;5T[tUCTURING OF TNL TEMPCItATUItr ANb I'[tL55UKL FICLb IN TEir
50UTHERN F1LMI5PNCKE _
Moscow MI:'Cf:OEtOLOGIYA I CIbROLOGIYA in [tussian No 12, bec 1978 pp 43-49
(Article hy Candidate of Ceographical Sciences L. A. Uranova, US5It liydro-
vieteorciloKicol 5cientific Researc}i Center, submiteed for publication 17
I11rch 19781
Abstract: A study way made of restructuring _
of winter cyclonic circulation to summer
anticyclonic circulation in the southern
- Iiemisphere seratosphere. On tlie basis of an
analysis of pressure paCtern charts for tlie
30, 30, 20 and 10 mb surfaces and spatial-
temporal aections constructed using data
from aerological and rockeC soundings it
was possible to determinc the date of the
restructuring. The results of tlie analysis
icidicated that for the most part the restruc-
turing of the temperature and pressure field
tn the southern hemisptiere stratosptiere oc-
curs the same as in the northern hemisphere.
[Text] buring the last decade a rattier great number of studies have been
(ievoted to an investigation of the processes of restructuring of circula-
tion in tlic norttiern hemisphere stratosphere [1-111. In these studies the
;iuthors Eor the most part proposed qualitative characteristics for deter-
r,iining tlie dates of restructurings of the temperature and pressure field
_ tn tlie stratosphere. As the date of the restructuring it is customary to -
use the day when the spring stratospheric anticyclone was to the north of
the cyclone and vice versa, when the anticyclone was to the south of the
cyclone in autumn. In addition, the author determined the dependence of
the seasonal restructurings of ttie stratospheric temperature and pressure
ftcld on difEerent factors.
1n [8] the author found the dependence between restructuring of the tem-
i)erature and pressure field in the atmosphe:e and restructuring of the
field of total ozone content. The gradient J',qp_p, obtained by D. A.
51
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['ed' (ti1, wa� used aq a rharacteristiC of ttie restructuring. Under the
influence of nn intensive influx df golar rtidiation, ifCer ehe winter
molstice Lhere iy a reKtructuritig of ttie field of Chc total ozone con-
tent, acid then the gtrntoqpttcrir Cemperature and presgure field begins
to be rcsCrucCured.
As is well known, after ttie winter 301qCiCE an intengive flux of UV radi-
,tinn is incidenC dn ttie upper boundary of ttie stratogpherc in the south-
- ern part dE the temrerate latieudeg (30-40"N); under its influence, as a
regult of photorhemicnl reactions, a marked increase in the quantiCy of
oznne begtns. Firvt Che ozone increases in Che stratopause reginn, and
then lower. Naturally, tliis leads to a temperaeure increase in the serat-
osphere. This, in turn, changes the geopoCential field nnd firsC causes a
weakeiiing of the westerly winds prevgiling before ehis nnd Chen their re-
placemcnt by easterly winds.
- An analysis of churrs of aeraCospheric levels (50-10 mb) for a 20-year per- -
tod indicnted that usunlly the spring resCructuring begins with the ap-
; pearance of nsmall hent region at 30-40�N along the shores of North Amer-
ica in the AClantic Ocean or along the shores of Jripan in the Pgcific
Ucean or at the center of Eurnsia at the isobaric surfnce 10 mb. Then
this cocus begins to be displaced almost stricCly Ca Lhe north and afeer
several days enters the polar basin. This is followed by pressure field
_ transformation. inciden[ally, Che relationship between the movement of
lieat foci and foci of grnwth of the tatal ozone conCenC was already noCed
tn an .7nalysis of stratospheric winter warmings in [7]. It was noCed
there that Eirst a region of increase in the total. ozone content is formed _
and Ctien a region of a temperature increase.
Unfortunately, for altitudes greater than 30 km there are still no suffic-
iently good temperature data for the hemisphere that would make it possible
to trace ttie movement of heat foci.
1'here are very few sttidies devoted to an investigation of the seasonal re-
::tructurings of the stratospheric field in the southern hemisphere. E. Far-
I;as (lO], in an analysis of variation in the total ozone content in the
course oE ttie year ae diEferent latitudes,relates these data to the similar
temperature variation at the isobaric surfaces 100 and 50 mb. These data
were used Ln computing the S?40-85 values for 03 for each month over a
period of 10 years and were used in this study for determining the mean
times of resCructuring the field of the total ozone content. The mean
monthly ~`Z40_p values for the isobaric surface 10 mb in the southern hemi-
sphere were taken from charts constructed by L. A. Zhdanov for a four-year
period.
joint analysis of the monthly distribution of J~40_p values for ozone and
geopotential Hlp for the sout}iern hemisphere with the .�Z 40- values for
the northern hemisphere (Fig. 1), plotted on the graph from T11], indicat-
ed ttiat restructuring of the field of total ozone content in the southern
52
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liI-Iml41010rc, the yame ay tn the northr.rn hemiqphere, occurq aooner than
tlir reytructurinK oE thu gcoPntentinl fteld nt the isdbartr surE.1CC ld
111l. 'flie snme aq in tho norlhern hemlqpherr, t}ir ch.7nge in circulntton ilt
llit! 11Ip Hurfact-, heglns when thr resCructuring oF thc ozone field h.7s ala
ready occurred, thnt ts, when S~4d..pO3 = 0.
J?
FiR. 1. Mean long-term S~40_p values and geopotential E110 for the south-
crn }iemisphere (1)9 southern hemisphere (2), total ozone content in the
nc,rthern (3) and southern (4) hemisnheres.
It mLitit be noted that the time interval between restructurings of the ozone
I'tel.d and geapotential H10 (Qt) in the southern hemisphere (Table 1) in
hoth spring and in autumn is greater than in the northern hemisphere. The
tipring restructuring of the geopotential field occurs more rapidly (22
(lays) than the autumn restructuring (56 days), whereas in the northern hemi-
tiphere, on the other hand, the spring restructuring is considerably longer
(46 days) t}iati the autumn res[ructuring (18 days). It is also interesting -
to nute that the spring restructuring in the northern }iemisphere (Table 1)
and the autumn restructuring in the southern hemisphere occur almost at
t}ie szme time (February-March).
Tlie autumn restructuring in the northern hemtsphere occurs two months earl-
fer t}ian in the southern hemisphere. The fact that the spring restructuring -
of the temperature and pressure field in the southern hemisphere stratosphere
53
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FUk OFt'tCtAL USL 11N1,Y
�eCur4 Ot the nvorago twtvr a:; Ea9t aq in thv nnrtherii Ilc'tT1LH(1I1Cre r..1n evi-
tIriitly br attributeJ an.ly ta the influence oE the underlying yurface. Thig
- is Incticated by the data in Table 2, which showy the duratidn (in months)
clf ryclotlic (.fZ40_p > 0) attd nntiCyclonir circulaCion (5240_r 1 0) in the
strcitospherc of both tiemispheres. The duration of cyclonic circulation in
the southern hemigphere is nnt mucti greaCer Chan in Che northern hemi- -
sphere, whereaq the dlfferences in the lifetime of the fl.eld of the tota1
content aE nzone of the saine sign are very greae. I'or example, whereag the
minimum iti the northern hemispliere polar bagin 0140_1)> 0) pergists for
6.5 months, in the youtliern hemisphere iC is obgerved over a period of 9
months. As ig we.il known, Che amplitude oE the variations betweett the maxi-
mum and the minimum in the eotal ozone conr.enC in the annual course is less
than in the northern hemisphere.
Table :l -
11ean Times of Unset of Seasonal ItesCructurings
L CcnepHOC no.iyuiapiic 10;~cttae no~ywapnc
_ z
'x�a Hio ~3 -1 o, ~Hto a 3
.18 D piS II IS I V 46 Z XI 24 XII 22 -
30 15 VIII 2 1~( 13 II 1 IVI ;~6
b ut
Note: Dspr and Da t. are the dates of the spring and auttunn restructurings,
t~p3 ts tlie date 0 ~ restructuring of the ozone field, bNlO is the date of
restructuring of the geopotent.i.71 field ae the isobaric surface 10 mb,
~'C is the time interval between restructurings of the ozone and geopoten-
tia] Eields. 1) Norttiern hemisphere; 2) Southern hemisphere; 3) days
1111 t}iis taken together ts evidently the reason for the rapid spring and
_ cletriyed autumn restructurings of the geopotential field in the southern
liemisphere.
tiow having an idea cvncerning the mean Cimes of seasonal restructurings
of the temperature and pressure field in the strarnsphere in both hemi- _
:;plieres, we will proceed to an analysis of the spring restructuring in
etie southern hemisptiere in 1977. For this purpose, during the period of
the 19th voyage of the "Akademik Shirshov" scientific researcti vessel we
c-onstructed pressure pattern charts for the 50-, 30-, 20- and 10-mb sur-
faces for the southern hemisphere for November and in part for December,
charts of the trajectories of movement of the centers of cyclones and
anticyclones at these levels and the spatial-temporal sections for both
temperatures and winds from S�N to 50�S along 95�E and from 20 to 50�S
iilong 65�E.
The spztial-temporal section along 95�E from 30 to 50�S for the period 11-
19 November 1977 indicated that in the entire thickness of the strato-
tiphere, from 22 to 45 km, where the stratopause was situated at this time,
34
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FOIt OFFICIAL USl. UNLY
therr. were engterly windy. This indicates thae the reytructurittg of thc
str,itoypheric tvmpernture ,7nd pressure Eield aC these latitudes over thc
[ndirttt Ocean hny already nccurred. Abnve ttie 4tr.atopauye, .t.n the meso-
spherc, ht an altiCude nf 50-56 km 7t 40�S westerly windg with a velodty
uf ZO m/sec: were ;il.re7dy obscrved on 13 November. On 16 November westerly
and southwesterly wl.nds with velocities up to 15 ro/sec were observed at
45"S nlrefidy at an altitude from 56 to 59 km, whereas at 50�S weseerly
toindg or_curred only above 65 km. Thus, the boundary of ttie westerly winde
rose aC ttie rate of 2 km/day. It can algo be seen in this secCion Chat ~~t
nn altitude of 30 km it 40�S From ehe beginning of November Chere was a
cemprr,7ture -40 --45�C, wherens during winter ttie temnerature at this nl-
titude here drope to -60�C. The spatial-tempora1 xection along 65�C from
30 to 50�S and b7ck frnm 75 November through 3 becember a15o indicated
that [n the entire stratdypheCe and mesnsphere there were easterly winds
tit th[v region and accordingly a spring restrucCuring had already occurred.
Table 2
Uuration (in MonChs) of Positive and Negntive
S~40-p Vnlues of Field of Total 03 Content and
Ceopotential Field 1110
Cenepnoc
no.lywapnc
10 "oc 2
nanywapne
o o
0
0
n v
n
V
~ c
r
a
~ g
~
o
a a
u
a
Hio 7.5 4,5 8 4
O3 6,5 ti,5 9 3
Key:
1. Northern hemisphere
2. Southern hemisphere
3. surf
l;nEortun:itely, a small delay in departure on ttie voyage did not make it pos-
5ib]e to trace ttie entire restructuring process because it began at the very
beglnning of November, as is indicated by the pressure pattern charts 50-10
nb for the southern hemisphere, constructed and analyzed during the 19th
voyage of t}ie "Akademik Shirshov" scientific researcti vessel.
As Ln tfie northern hemisphere, the spring restructuring in the southern hem-
isphere began with the formation of heat foci in the subtropical zone (Table
3). The data in the table do not give a complete picture of movement of he3t
foci toward the pole, but on the basis of these data it is pcssible to ob-
tain a reneral idea concerning this. For example, during the period 6-9
55
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Novembcr f.ucl wl.th h tcinperarurr --40 --44�C nppeared in different rcgicms
uf tiie Nubcropics (23-25�S) at the iyobaric yUXEF1CC 10 mU, and nlready dn
1 l November ct forug witli r tempr.rature -31�C wns observr.d along the atloreg
uC MntarrtiCtt. On 27 Nnvember, at thr. III�>lIU lfL'>IJ)hllllll\111':!
.
~
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-
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~ LL ~ t=~ C, . ry~:~ c~ r; r T= a 3 4-
O H i",B M q 4 Cr�~ yi3ts C V n 4
Cx~ La -*_:[t-l:.C~z ri,
O r-1 Nfn ~tu'1%0 f-000N 0-4 N M.7 wt-p f-00
N N NN N N N NlVC-1 c"1rn cl1 mc''1 mm cnc'1
108
FOR OFFICIl,I. U5E ONLY
APPROVED FOR RELEASE: 2007/02/08: CIA-RDP82-00850R000100020020-6

APPROVED FOR RELEASE: 2007102/08: CIA-RDP82-00850R000100020020-6
P.-I
~J
r-1
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1-40R nrrtcrni, ust. oNt,Y
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109
FOR OFFICIE.L USE ONLY
l_
1
APPROVED FOR RELEASE: 2007/02/08: CIA-RDP82-00850R000100020020-6

APPROVED FOR RELEASE: 2007102/08: CIA-RDP82-00850R000100020020-6
FOk UFFIC1AL USL c)NLY
- Key Co Ttible 1
1.
[Zcg.lon
2.
Cv;iluatl.dn or Climutic conditions
Cvalucition of. soil r.anditionq
4,
beprh of: soil. wetting
5.
Overa11 eva].uaeiun of ytaCe of winter
crops
0.
Sum of neguCive temperarures during w
inCer
7.
Sum of active temperatures by periods
- 8.
Sum of precipitatinn by periods
9.
Soil boniter
10.
% o E mean fnr obins t
11.
Depth of so:Ll wetting, cm
12.
% o f inezn fnr oblast
- 13.
Cvrocesyltig syqCem of tlte Ye5 electronic computer, and the devel.dpmettt of
y.imllnr mar.rodcterminarionx by oneyel� is qutte time-rnnguming. Therefore,
thc Uasic 4tructures were realizcd with uge of cdmmandg of cottditioia1 and
unconditiona1 cdntrol tranamisyidns. Althougli thig in a vin.tneinn of struc-
tural progrnmming In lts pure form, the t+ery fact of congtruCticsn of ttte
pCpgrtlttl EYtlitt t11CCC banio stCUCtUYe3 15 VGry i1gefUli aitlCe it 1@ndS t0 a
roityiderable nidering of the logl.c or the program and faCilitateA uttder-
~+tandtng of Che rrogrnms
'l'he result of Che firyt gtep in the program for rnmbinittg two data masses is
recorded on magnetiC tape in ehe FGGL format with the excluyion of dupliC-
.ited communications and regigtry di the Combined magy inCo magtteCic tape
vnlumeg in the FGCE format, thiie ig, the actual program itself has the fol-
InwinY form:
11 5ECOND
I3EGiN
21
CLEARANG
;3) bM1'I1ILG
EQU *
11
F'OREOV
5)
ANAL1515 SIGN
6)
IF 51GN =Qj TI-IEN MEaGE
7)
Ir SIGN= 1'r;IFN F1LE bNE
g)
1F SiGN= 2 THEN FILE TWO
9)
ENUWFIILC DOWHILE
10)
F NDWOR1C SECONd
11) E:01'OUT
UNLOAd dUT
121
SE'1'NEW OUT
13)
SETINPUT
14)
I3 DOWHILE
Proposirions 1-10 correspond to segments which determine:
l) standard heading ("cap") of any program in assembler language;
2) ini[.tal farming of the volumes of magnetic tapesy printiug of Che
headin9 of the processing Eormand obtaining the first record-headings
l
fil
and f1 2 ~~C the files Fi1 and Fi
(il = 12 = 1);
1) cummancement of cycle of com9ining of data masses;
4) stor;ige nE the numbers of the input and output files from which the
new
slx-hour data blocks begin;
output of tlie processing forms and analysis of rhe lieadings f
an
j
f~ of the two input files Fii and Fi
. The parameters t}1 and t di
9
1
2
2

l
2
'"'d `li~, Si and Si are compared; a coincidence of all three parameters
i,ie,~ns thiie ~he two ~nput files must be combined into one file;
0) tlte combitiing (in the case of coincidence of the parameters C, d and
S)
(if the two fLles Fil and F12 into a single file with the exclusion of
dupltcnted communications;
7)-8) regLstry oE t}ie file Fi1 or Fi2 on the output tape;
118
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Vc)li C1VVI (I AL U:+I. r1Nt,Y
9)-10) analywiy at tle end oE the cyr.le of combining of the data masy atid
termlnation oC prcyr.cyyirrg fina1 forming of the magnetic tape outpUtlowol-
Me.
Propugitiony 11-13 are for prdCessing n qituntion when fdr regigCry of a
combite(i data tnagq it is noC suff.icient to hnve one magneeic tape vdl.ume
Alone cind iC Ly ner_essary Co employ an aclclitional volume fUr rtie ouepur
data myyq.
A11 thc segmetiCs whoqe ttameq were used itt rhe maitt segment of the program,
i'ited above, orher than e}ie segmenC degignaeed rtEitGC, tinve 1-2 more levelg
tn depCh and are quite simple. The rtrKr,L segment, which is for Che Combitt-
ing nC the two dat.n Eiley into one, is mdre romplex and ies depth ig meas-
tire(i wttli y.tx lcwrlw. We w111 eite cin example of thc D1LftGL segment:
1) MACaO
2) ,`.1E (~G r.
3) I-(C:r1hCiZ
4) DOWt-I1LER I;QU #
5) SOLU'TIOti PR15
5) IF pR15t-0 TUIEN QUr1LIC0N
7) iV PRt5= t'1'I-iEN REPOn�f ONE
8) IF PCt15= 2 TIiEN nEpOaT TWO
9) f'INISFf DOWHILER
10) OFORti1i'C
11) NEYTFILE
12) MEND
Ilere proposition 1 is the heading of Che macrodetermination; proposirion 2
a prototype of a macrocommand deCermines the symbolic name of Che par-
t Lcular segment.
I'ropostt(on 3 r.orresponds to a segment which creates the heading of the file
oUtalned witli tlic combining of two input files and introduces the headings
I�}1 kt ;ind rt k�I' the Eirst (kl = k2 = 1) communications Ri kl and
jZ k_,. rroro9ition 4 serves ag the commencement of the cycle 1-f combin-
ing uf two Files into one. After one passage of the part of the program cor-
respcmcling to rhis cycle (propositions 4-9) there is n changeover to the
itext communication in one of the combisied files or in both.
t'ropostttnn S corresponds to the segment for carrying out n comparative an-
:Ily:~is of the headines rit kl and ri2 k2 of the communications RI1 kl and
KiZ k.,. An .inalysls is made of the parameters aIk, ot lk' A lk' bK+ Present
ii the iirading of each communication. Depending on which of the two commun-
ications nil kl and Rf2 k2 is preferable Co be registered first, the pCtI5
c�rtterion ts assigned the value 1 or 2. If the above-mentioned criteria are
i nadequate for r, solution (this means tllat the communications are duplicat-
vd), the P[tI5 criterion is assigned the value 0 .
119
FOR OFFICIAL U5E ONLY
,
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Fdit Ot:FLCIAL tSE: ONLY
TaU te z
Wrl~;lit;i f~r 14, 11nh111ty Critrrin
V;tluo cC rellrtbllity 0rHe riptlcin lJe i};ht
crieerinn
0 Nn checking 3
1 Correet va].ue 5
2 QuegCionable value 2 _
3 grranedus vnlup 0 -
4 Vnlue changed in
checking prdceaM 1
Proposieion 6 correqponds Co tite gegmenC which wiCh a value of tite t'Itt5 cri-
terion equal Cn 0 n comparneive analygis ig made of thh c;dmmuuica tions
ItI .hnd it2 k2. ''he analysig is made on tlte Uasis of ehe qualiCy con-
tro.lkc~riteriaZfdr tite principal el.ementg in the cotnmtinication gupplied
hy the territorial vubcenterg. Eacli quality contrdl criterion is agsigned
some weiglir. (muhle 2).
!ytnf; +t rer.udlng Commund ('Ttt) each contro1 criterion cncnuntered in Fi par-
t.trular communication is converted inCo Che r_orreyponding weight and the l
Lotal weight di tite parCicular commuttiCaLion Pik is deCermined (segment
QUALICON). In ehis same segment there is a cnmparison of tlie COCa1 weights
P ~1 kt and P12 k, of ehe commun~.cuCions itIl kl and Et~2 kZ.
[f I'~1 kl < I~~ k2, rhen ehe pRIS criterion is nssigned the vglue 2 und
ihere is a reaiing of the hending rl k nE tite next (kl - kl + 1) com-
munication Itil kl (that is, the Worst of the duplicated communications is
timitted). }lowever, if Pl1 kt> Pi2 kZ, tite PE~IS criterion is assigned tite
value 1 and we reud the heading r~2 k2 of the nexC (k2 = k2 + t) communica-
tion R12 k2.
I'roposition 7 corresponds to a segmene which (if tite value of Che PRI5 cri-
Lerion fs equal to 1) accomplishes registry of the communicaCion Itl1 kl
into tite combined file and then the input of the heading rl1 kl of the
iiext (ki = kl + 1)-th communication Ril kl�
I'roposttioti 8 corresponds to a segment whicl (if Che I'RIS criterion value
is equal to 2) perfnrms the same operations ns the segment in proposition
y, but witti respect to the communictttion R12 k2.
I'rnpnsittons 9-11 correspond to the segments which perform an analysis at
tlie end of the cycle of combining of files, finalize the combined file
fn accordance with the requirements of the FGGE formaC, and accomplistt
the inptrt oE the headinfis of the next files in boCh input data raasses.
i'roposition 12 is the end of the macrodetermination, determining the seg-
tlleIl t .
120
FOR OFFICIl.L U5E ONLY
APPROVED FOR RELEASE: 2007/02/08: CIA-RDP82-00850R000100020020-6

APPROVED FOR RELEASE: 2007102/08: CIA-RDP82-00850R000100020020-6
FOtt hVt'tCIAL U5L ONLY
'I'iiull, ri1thoug1i the uye of iirayemblar langurif;r l.n thiy ptokr,lm ciid tiet make
_ Il~ IM~4r1ll1lr Cil rrr(itt, a I'ully Hl-rurturecl Prngriam, the cippllc;ition or the
!+tructuriicl prngrAmml�g prineipLc ln org;znixtng the pra};r.am way extrf-imely�
iiyeCul tn the ctebugging stapc in ttie program and the introductinn of
changes (cautied primaril.y by changev itt thc FGGC format) 1nd made iC pog-
~Iible ea reducc� ehLi titne required fnr debugkitig oC the prdgram and making
_ preparatinnq for the FGGt; tent period.
'1'he progrnm wav uged for cnmbining the mayses di test d7ta received from
the United 5tates, 5weden, Grent Uritain and Japan attd prepared in 5oviee
PCGC centers.
'I'he time for nperaeidn di the program with the merging of two magnetic tapes
with ld-d.ny data. magges ig about 30 minuteg.
I3IBLIOCEUII'l1Y
l. Akyartn, N. N., MyaCh, L. T., "bata Collection itt the First Globa1 Cx-
periment CAItP," MrTCOROLOGIYA I GIbROLOGIYA (Ateteorology and Nydroldgy),
- No t, rh 94-t030 1978.
C3i.lkuti, S. N., Maylyuk, G. F., "Structural I'rogrnmming," I'itOGE2AMAtIRO-
VANtYt: (programming), No 60 pp 123-131, 1976.
l. Cer.iviroenko, V. A., "[3asic principles of SCructural Programming,"
7.ARUtIi:ZtWAYA ItAUIOEi.LKTRONIKA (Foreign andioelecCronicg), No 11, pp
3-]0, 1976.
4. Ua}i1, bd. , Uykstra, Noor, C., 5TRUKTUftNOYE PROGItMihtIROVANIYF (Struc-
- Cural i'regramming), Moscow, "Mir," 1975, 245 pages. _
5. llills, N. D., "Top-Uown progranQning of Large Systems," SItEb5TVA OTLAD-
KI BOL'SHIKii 5ISTFM (Means for bebugging Large Systems), edited by
Rastin, Moscow, Statistika, 1977, 135 pages.
}{olton, Y., tiryan, B., "StrucroorPA Tnn-itow� xlow Charting," bATAMATION,
No 5, pp 80-84, 1975.
7. IN'TEItNATIONAL CLOUAL bATA PI20CE55ING 5Y5TEM PLAN `TO SUPPbR'T THE FGGE,
WriO, No 469, 1917, 73 pages.
;1. Rieks, C., "Structured Programning in Assembler Language," bATMtATION,
No 7, pp 79-82, 1976.
9. Yourdan, E., "Making the Move to 5CrucCured programming," bATAMHTI0N,
' Na 6, pp 52-56, 1975.
121
F0(t OFFICII.L U5E ONLY
APPROVED FOR RELEASE: 2007/02/08: CIA-RDP82-00850R000100020020-6

APPROVED FOR RELEASE: 2007102/08: CIA-RDP82-00850R000100020020-6
V'oK nVrtrr.nt, usE* ortLv
UUC 551.46:681.03.06
AU'TOril1'TIUN OF COLLEC'I'ION, PitOCESS2NG ANU ANALYSI5 ()F OCLANOGItApHIC -
INFODtATION nN TliC t3ASI5 0F 5MALL ELLCmitdNtC COMt'U'TEit5
Moyrow Mi:'I'GhR(lLdGtYA I GIUItOLOGtYA in Itugsian No 12, neC 1978 pp 95-98
(Artlr..ie by V. A. Volkdv, Yu. A. Grodetakiy and V. V. Lukitt, AYCtiC and
Antarr.ttc Sr.ientifir. itesearch InsCiCuCe, submitted for publication 6 Jan-
uary 1978]
nbscracr_: I'tie authorg examine e11e basic prin-
cipleq Eor the rouCine processing, syseematiz-
ing and analysis of information nn the besis
of yma11 etectronic compueers under expedieinn-
ary conditions corresponding to the prenent-dgy
nature of oceanoRraphic regearch and Chci modern
requirementv on dar.x prncessing. The irt-icle
gives tiie procedureg for use of sma11 programm-
able rlectronic keybnard cdmputers (pE:KC) ag
the bag.ts for computation centers for exped-
itions not having large electronic compttters.
There is 4mphasis on the desirabiliCy of using
PEKC for automating Che collection and primary
processing of data on scienCific resear(:h ves-
sels outfitted with large computers. Ttte ar-
ticle also gives nn analysis of experience in
operation of a compueer complex on the basis of
the "Iskra-125" I'IiKC an the high-latirude air
expeditions "Sevcr" di the Arctic and Antarctic
SctentiEic Itesearclt Institute of the Main Admin-
istration of the Hydrometeorological Service.
IText) OceanoRraphic investigations long ago ceased to have a purely geo-
graphical, descriptive charac[er. Now purposeful investigationq are being
_ mlde of the laws oE physicnl processes transpiring in the waters of the
worid ocean. Recently ttie investigations assumed excepCionally greater
scales, which is utcributable to the ever-increasing imporCance of the
ocean :ind its resources for man's economic: activity.
122
FOR OFFICI/,L USE ONLY
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APPROVED FOR RELEASE: 2007102/08: CIA-RDP82-00850R000100020020-6
FOlt OFFICIAt, U5l: dNLY ~
Uceaunokraphic expeditions are very diveraified in their OhjCCtiVCs, the
pcryonnel emplnyed and the equipment uyed. In addirion to purely scien-
tifir_ objectiveg, rroblems of a practical nature are bcing fdrmulated
ar.d go.lved, sur.h as the Collcction nf ttydrnmeeeorological information
Cor progndqCic purpose,s, planning and regearcli taork and the quesr fdr tis}i.
14.hjor experimentg at gen have ndw becdme commonplace; rtiey cover relative-
ly large buC 1oCa1izcd deean nreag (the5e expeditinns: Atlatttic HvaYnpt,ys-
tcal I'olygon-70, TitOYI:K5-74, pOLEK5-Spver-76, YULIMObC and oCliers). SuCh
inveqtigationq are nd longer being carried oue by individual gcieneific
resetirc:h sliips, but by detachmenCs of stiipg, frequently beldnging to dif-
t'erent departments or even differettt countries.
0r.eanologists are Curning more and more to investigationg of fine hydro-
logiccil Htructureg, sma11-scale itteeraceion between C}ie ocean and the at-
moyhhere, which requires the development and uge of self-conCained low-in-
orti,h menquring npparneus KivinK n considerably qreater flow of infdrma-
tinn tI17t1 ordinary inseruments.
Thus, the volume of infnrmation obtained un a modern oceanographic expedi-
cion iw wndcviatingly increaging and resetirchers are being ficed wiCh the
problem of itw hroceysing, tlte solution of whic}i is imposgible wittiout the
use oE computer.q. The processing of observational data must be carrted out
rnueinely, which is dictated, firgt of a11, by the neCessiCy of transmis-
sion of data for the forecasting yervices; second, by Che necessiCy in a
ilumber of c.ises to introduce correctionq into the research program ns re-
s:ults are obtained, that is, carry out so-Called "conerollable experi-
rients," which corregponds to a purposeful nature of present-day resenrch
in the ocean. r1t ttte game time, rouCine processing makes possible a con-
statit monitoring of the quality of observational data.
'11ie processing of the information collected on an expedition can be divid-
ed into three types: primary processing, systematization of observational
clat.i, analysLs.
'I'he primary processinK of observational data can be reduced essentially Co
r.omputationy and introduction into the instrument readings of all possible
rorrections with the use of traditional (nonautomaCic) measurement in-
truments and methads which at the output yield an electric signal and
:ilso a conversion oE coded data into the generally employed form. Tn the
-;ec:ond cave the problem also arises of compression of information aC a
real time scsile.
Until now the systematir.ing of data has involved the compilation of diEfer-
t-nt snecial.ized and composite tables. Now, when virtually all types of
ocennographic information are being subjected to analysis on electronic
4-cimruters, the collected inEormation must be incorporated on a computer
r..lrrier (punched tape, magnetic tape) and it would be natural, parallel
witli Corming these tables, to create archives of hydrometeorological data
tn a carrier suitable Eor input intn an electronic computer. The systemat-
izatton also includes the process of sorCing of data and preparation of all
possible intermediate and sample files.
123
FOR OFFICIE,L U5E ONLY
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APPROVED FOR RELEASE: 2007102/08: CIA-RDP82-00850R000100020020-6
roR oPrtrtAL usc: nNLY
'I'he flnril 1'orm uf d.ttci pror.eHyltlg iq at111YyIy. x'hc ypeCifiC form:i df ati-
aLyy,
lq ,ire determ.tnecl by ehe researcher li:lmgelf in aCCnrdnnr.e wirh the
purpufies nC Clie expatimeie. 'I'hiH clags rf problemq ig the mdst divergif-
Led.
`t'huy, the qygtematizing nf matcrihl in CIIe logicat ending nf primary
procesHing and is Che basig for analyCiccil CbmpuCatiott5. It is necessary
co be guicled by tltis thesis in fnrmulgting principles fdr the mathemar-
tcnl support of sygtems fdr ttie atiComaCed prncesging of nbaervaeidnal
clnta using electron compuCers.
'Chc }lydrometeorotogical 5ervicc gystem }�s a1ready acquired defittiCe ex-
rei�ience in the use of c.ler_tronic compueers under expediCionary cnndi-
ttoms on large Hcientiftc tesc:arch Vp8ge19 on which inCermediaee-CZggS
electronic CompuCerq of the "Minsk-32," Ye5-1022 and oCher type8 hnve
ber.n insealled. The upplication of e}iis experience to dceanographic ex-
pedit.inns bnHed on small nnd intermediate ships (gnd they nre Clle gre7t
imajority severul hundreds), drifCing sCations, etc. is not feasible
rind frcquently !.t iq simply impnssible due to unwieldiness, expenge gnd
cnmplexity in operation of the mentioned machineqe
As i:; well knowTi, Chere ure alao elecCronic computers of n smaller size.
'i'he first compuCprs, laCer given the name "minicomputerg," were the PDP-5
' nnd Pbp-8 computers produced by the American DEC cnmpnny, appearing in
1963 and 1965 respectively. The idea af a minicomputer is very simple:
in rtiese tnseruments ehere is a programmed performance of all elemenCary
rransEorm.7eions of dnta in ntt arithmetical-logic device, in the last anal-
ysis performing yume operation. 5uch an approach made possible a marked
reducCion ln the size and cosC of the electronic computers (alChough aC
the expense of some qualities speed, volume of the directly addressable
iiemory). In a wtiole series of cases it has proven justifiable to place such
an electronic computer at the disposal of an individual laboratory or
scientist. Minicomputers 1iave come into extensive use in scientific experi-
ments and in the control of production. The best known modern computers of
_ this cl;igs in the USSR are the M-6000 and M-400, and abroad the DEC
Eamily of computers PbP-11.
FurClier improvemenC in the technology of components and new ideas in the
architectural designing of elecrronic computers have led Co the appear-
ance oC minicomputers, with respect to their size being virtually personal
table-top mactiines for the researcher and having considerable functional
rnrabil ity.
' Amoig tliese computers we can mention those which can arbitrarily be called
program-controllable electronic keyboard computers (PEKC). Their characCer-
lstic peculiarities are the forra of storage of the progratns in the opera-
Lion.il memory unit (OMU).�
.\s ts well knawn, the usual sequence for carrying out a program involves
tts introduction into an electronic computer in some initial high-level
language, such as FORTRAN, its translation into an objective code
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the prdgram in n c:omputer code and work w3.th the reyuleing prdgrnm. Such
,i method mnkes iC poqgible eo obCnitt in effecrive progrnm, but rpquires
J Che avnilnbility of M lnrge-vdlume memory unit for holding the prografi-
- er.anqlnCdr. Additional mnehematicnl suppore is required Eor debugging e
program in computer codes.
A dif ferenr principle iy uyed in PCKC. In the I'EKC OMU Ctie program is sCor-
ed in t}ie initinl language and Ctte progrility scales, associated wiCh formation of ineanders and eddies.
A report presented by A. Gordon proposed a hypothesis concerning the form- ation oF a quasistationary polynia in the Weddell Sea and also the role
which the presence of such a polynia can play in the formation of Antarc-
tic bottom waters. As a result of the discussion, the hypothesis of a de-
- cisive role of the upwelling of deep waters in the formation and mainten-
ance of the polynia in the Weddell Sea was subjected to criticism. However,
the opinion was expressed that bottom waters can be formed in the polynia
reKton.
In the reports oE American researchers great attention was devoted to an
1nn.l.ysis of the }iorizontal and vertical correlation of the variability of
c�urrents in Drake Strait on the basis of instrumental observations (report
by F. Skiremammano). Tlie principal objective of these investigations was
obtaininR scientific.zlly sound criteria for the planning of a new major ex-
periment for s tudy of the structure and dynamics of the Antarctic Circum-
pol.nr Current in Dr.ake Strait in 1979-1980.
At the conference l-.here was also a discussion of the results of modeling
of water circulation in the Antarctic Ocean. For example, in a report by
V. V. Guretsk[y, V. 0. Ivchenko and E. I. Sarukhanyan the authors presented
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rin orlgtntil din};noetic model of circulution in the MtarcCic Oceun and
proposed meChodd for the pnrnmeCeriztCion of inesoscale eddies in problems
Involving description o� globAl circulation.
I:. Fendri gave An esCimate of barotropic waCer rrnnsfer ehrougii Drake SCrait.
In the field of study of energy exchange between the ocean and the atmosphere
and the energetica of the atmosphere, as before, the principal sCudies were
carried out by Soviet researchers. -
A review of the resulCs of instrumental observations of currents in Drake
Struit under a three-year program and a descript3.on of the srructure of
C1ie new "Drake-79" oceanic experiment were presented in a report by J. Mor-
rison. The experiment will be carried ouC in January 1979 and wi11 involve
the placement of about 20 buoy stations with submerged buoys wiCh current
iiieters and temperature meters over the entire area of Drake 5trait for the
purpose of a quantitative description of the spatial-temporal variability
of the field of currents in ttiis region at differenC scales.
_ A report by N. A. Kornilov and E. I. Sarukhanyan was devoted to an exposition
o� the results of long-term investigations on a section along 20�E and a
draft of a program for the oceanic experiment "POLEKS-Yug-79." The exper-
Lment will be carried out in the region between Africa and Antarctica dur-
ing the �irst special observation period of the FGGE and will include the
carrying out of a complex of aerometeorological observations on ships, place-
ment of FGGE drifting buoys, setting out of buoy stations with sumergible
buoys, a hydrological survey of the water area and work in the polar frontal
zone.
'ihus, in the course of the conference there was a presentation of the prin-
cipal xesulCs of Soviet and American investigations in the region of Drake
Strait and the Scotia Sea, carried out during recent years. The invesriga-
tions carried out within the framework of cooperation aiid represented in
the conference reports made it possible to advance considerably in an under- _
standing of hydrophysical processes in the Antarctic Ocean, to determine
in considerable detail the structure of the Antarctic Circumpolar Current
_ and the Antarctic polar front in the investigated regions, to obtain an
evaluation of water transport, and to evaluate the degree of influence of
the hydrological front on atmospheric processes. Thus, due to the joint
investigations there has been a marked increase in the effectiveness of -
scientific researcli work.
'1'tiis feelLng is shared by both Soviet and American specialists, who in ttie
c:ourse of the discussion expressed complete satisfaction with the results
uP the _juint three-year cooperation in the Antarctic Ocean and e:cpressed
the opinion that it must be continued and intensified for the longest pos-
sible period. In tlie opinion of both sides, the main efforts must be di-
rected to solution of the problems in large-scale energy interaction be-
tween the atmosphere and ocean, the structures and dynamics of the
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,
-
Ant;irctic Circumpolar Currenti and the Antarctic polar front, as we11 as
rhe formfxCion of Antarctic bottom waters.
LI� -
'I'he Sovier arid American specialists agreed on specific measures for the
excliange of :;pecfalists on ships and observational daCa. The opinion was
- :i1so expressed that it is desirable to exchange specialists in the field
of numerical modeling of circulaCion in the AnCarctic Ocean between the -
scientific research institutes of the USSR and the United States. The pro- `
posal of Amerl.can researchers that there should be organization of a joint
- oceanic experiment in the neighborhood of the Weddell Sea polynia was a.1so
r,iet with understanding.
- Thus, this contereiice once again confirmed the eff ectiveness of Soviet-
American cooperation in the field of investigations of the Antarctic Ocean
rind the desirability of its development in the future.
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N()'T1;5 FItOM AnkOAb
Moycow hiC'TEORULOCIYA I GIUltULOGIYA itt ltussian No 12, Uec 1978 p 121
[Arl-l.cle by B. I. 5ilkin]
['L'exe) Smog arises primarily �rom inCeraction between auComobile extiaust -
und citmospheric oxygen in the presence of solar rndiaCion forming an nde- ~(itiare quantity of ozone for this purpose. However, the prncesses of inl-er-
~ action between ozone and the remnining aCmospheric components, leading to
tlie appearance of such a phenomenon, have sCill been sCudied inadequately.
A recent discovery, made by Ctie physicistti R. Suenram and F. Lovas (US Bur-
eau of 5tandards), casta definite light on such processes. They established
the existence of a new class of organic substances dioxyrans, represent-
ed by a simple ttiree-rinb molecule cnnsisting o� carbon, hydrogen and oxy-
a;an atoms and ;erving as an "intermediary" in Che smog formation process.
- 'I'his discavery has led to a reexaminaeion of the formulated models of smog
which laid res )onsibility Eor this on the free radicals (unsCable chemical
substances) for.ming during the interaction of auComobile exhaust with ozone.
The investigations show that the reason iies in the appearance of less ac-
rive molecular compounds, such as dioxyran, created in the reaction between
ozone and ethylene, ejected by internal combustion engines.
Ttie existence of dioxyran was posrulated for the first time by the American -
r.}iemisrs W. R. Wodt nnd W. A. Doddard in 1975, but such a molecule could
not be discovered due to tfie fact thaC at the ordinary temperaCures at
wtiicli the reaction transpires the lifetime of dioxyran is extremely short.
5uenram and I.ovas succeeded in doing this due to t}ie use of low-temperature
inicrowave spectrogrlphy which stabilized matter for a time adequate for its
observntion.
'I'}ien they studied tlie reaction between ozone and other final olefins (the
f;imily of hydrocarbons to whicli, in particular, ethylene belongs). The next
stage in the inveGtigation will be to determine specifically what dioxyran
_ component plays what particular role in smog formation. This will probably
lielp in contending with smog, causing great damage to the health of the pop-
tilation in large cities.
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'1'lie cddylike currenrs rcceiLl.y discdvered in the world ocean are rinw being
[nveyCl.gaeed from gpace. r'or example, from aboard Che Americatt arCificial
enrth Mttel.lite "],andqat," qituaCed ar an altitude oE 915 km above Che
p:lcinetnry surfuce, it waq posgible eo rake a gpace phoeograpli nn whicll
,it lense cight individual CormaCiong of ehis rype could be distinguished.
'1'he procesyiiiK nf the photogruph, curried oue at the U5 Geological Service,
Itesentt, VirgLnia, under the direcCion of R. S. Willittms, made iC possible
eo deCecC Che existence of three well-developed double annular eddies aC-
taining a leitgrh df 70 km. Some nf rhese "rings" have a diameter of not
less rhan 30 km,
r1 study of Clie newly d3scovered phenomenon plays a ma;jor role in meteorol-
ogy ;ind oceiiiiology, including in Che investigaCion of inCerucCinn between
Lhe ocenn an(l ttie atmosptiere, in ttie Cracing of the processes of conCamin-
ation of the wuter medium, tn measuring p1ankCott productiviCy, erc.

Accnrding Co the concepts now prevailing among specialists, Che movements
of waCer masses, especially those associated with act:ion of the atmosphere,
:ire small ar great depths in the ocean and cannot exert an influence on
boetnm relief. However, recent inveseigations carried out in the Atlantic
Oce.m, in thi! region of the Gillis underwaCer volcano (to Che notheasC c:f
I3ermuda), have demonstrated ttiat very significanC movemenCs of sedimentar~
rocks are occurring on iCs slopes wliic}i it is difficult Co explain on th'a
basis of such concepts.
Around the Gillis submarine mountain, wliose peak is situated at an eleva-
- tion of approsimately 3 km above the ocean floor surrounding it, special-
ists placed a network of automatic current recorders on its slopes and at
Llepths aCtaining 5,000 m. The data registered by these instruments indicat-
ed that direcLly after the passage of hurricanes, which attain a great in-
tensity in the 13ermuda region, new currents appear in the bottom layer,
' even ar ri depth of 5 km. In three cases there was found to be a rather
- con5ider.ible rate of movement of the water masses, attayning 30 cm/sec;
thiti happened ench time after a hurricane.
:iuch 5poradically .irising and disappearing currents can fully explain the
reclistributton of sedimentary materials on the slopes of Gillis volcano
and the significant cliange in local relief which is observed there.
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