JPRS ID: 8374 STUDY OF THE SEISMIC CHARACTERISTICS OF LARGE INDUSTRIAL CENTERS

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4 APRIL 1979 ~ . i OF 3
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JpRs L/ea7a
4 Apxil. 1979
STUDY OF THE SEISMIC CHARACTERISTICS
OF LARGE INDUSTRIAL CENTERS
U. S. JOINT PUBLICAfIONS RESEARCH SERVICE
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JPRS L/8374
4 April. 1979
STUDY OF THE SEISMIC CHARACTERISTICS
- OF LARGE INDUSTtiiAL CENTERS
Moscow IZUCHENIYE SEI5MIC,HESKOGO REZHIMA KRUPNYIQi PROMYSHLENNYKH
TSENTROV in Russian 1978 siqned to press 5 Jun 78 pp 1-188
(Book by Ye. I. Gal'perin, I.L. Nersesov, et al.., lzdatel'stvo
"Nauka," 900 copies]
CONTENTS PAGE
Abstract I
Foreword 2
PART I. DEEP-WELL SEISMOLOGY 5
Chapter I. Equipment for Borehole Observationa 5
5 l. Deep-Well Seismametera 6
5 2. Preamplifiers 10
5 3. Amplifying and Recording Unit 13
Chapter H. Sensitivity of Deep-Well Observations aad Structure
of the Seismograme
16
5
1.
State of the Art with Respect to Seismological
Obaervations in Boreholes (Brief Survey of
Published Data)
17
3
2.
Laws of Variation of Noise Level with Depth
25
4
3.
Background Stability at Different Depths
32
4
4.
Useful Signal and Seneitivity of Well Observations
42
4
5.
Noise Background in the Case of Stationary
Noise Sourcea
58
4
6.
Observations in Shallow Wells Opening Up the
Crys:.lline Basement
67
- a - II - USSR - EFOUO)
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CONTENTS (Continued)
Page
PAttT IY. RADIOTELIIMET1tIC RECORDINC
ChapCer III. ,\lma-Ata Seiemological Radiotelemetric Test Area
77
S
1.
Ceological-Geophysical ChargcterieCice of the
Itegion
77
5
2.
Strncture and Technical Indexee of Che Test Area
83
5
3.
Radiotelemetric Channel
87
4
4.
Equipment of the Central Recording SCation
94
5
S.
Equipment for Controlling the Tayga Recorder
Dur3ng Tricomponent ltecording of Earthquakea
in the Slaved Mode
103
S
6.
Means of Smpxoving Radiotelemetric Equipment
108
Chapter tV. Field
Data and Procebsing Procedure
112
S
1.
Operation of the Test Area and Characteristice
of the Data Obtained
112
S
2.
Processing Procedure
119
S
3.
Er.ergy Classification
133
4
4.
Recording of Explosions
138
4
S.
Effect of Observation Conditions on Structure
of the Seiamograma
150
Chapter V. Observation Results
182
6
1.
Seismicity of Zailiyakiy AZatau
182
5
2.
Seismic Characterietics of Alma-Ata
194
S
3.
Azimuthal Deviaeions of the Seiamic Beams of
Diatant Earthquakea
218
�
4.
Directione of Future Re$earch
228
Conclusiona 231
Bibliography 233
Appendix I. Bulletin of Local Earthquakes Recorded by Radioteleme[ric
System from 1 June 1972 to t. July 1976 for idhich Epicenters
Are Constructed 240
Appendix II. Bulletin of Nearby Industrial Exploeions Recorded by
the Radiotelemetric System fram 1 June 1972 to
1 July 1976 247
- b -
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a
PUBLICATION DATA
Engliah title ; STUDY OF THB SBISMIC CHARACTSRISTICS
OF LARGB INDUST1tIAL CSNTSR5
ituseian title ; IZUCHBNIYB SEISMICHESKOGO REZHIMA
KRUPNYIQH PROMY3ffi,ffiNNYKH T5BNTROV
~
Author (s) ; Ye. I. Gal'perin, I. L. Nereesov,
et al.
Editor (s) .
Pub:iahing Houae ' Izdatel'stvo "Nauka"
Place of Publication ; Noecow
Date of Publication ; 1978
Signed to preas : 5 Jun 78
Copiea : 900
COPYRIGHT . Izdatel'etvo "Y:auka," 1978
- c -
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~tr
ABSTRACT
- Tnia book inveatigatea the development of the procedure$ and equipment for
- studying the seismic conditions of large industrial centers in agiemically -
iiazardous regiona. Stationary observationa in deep boreholes permitting
a sharp increase in senaitivity of the equipment and :entralized radio-
telemetric recording which incresaea the accuracy of determining the ~
coordinates of the centera in space were ueed se the baeis fur the atudy.
A description ie presented of the seiemic characteriatics of Alma-Ata
studied by the mater'als of 4 yeara of nbaervations.
_ The book ia deaigned for geophyaicista, aeiemologiats, geologieta, design
engineera and builders.
There are 17 tables, 92 illuatratiuna and a? referencea.
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rOREWORD
The SovieC tinion has many large industrial centers locaCed in seismically
dgngerous areae. In particular, theae include the capitals of union
republice such ae Alma-Ata, Frunze, Tashkent, Dushanbe, Ashkhabad, and so
on, and tene of oblaet centers and cities aith developed induatry.
The development and construction of citiea located in theae regiona require
seismic regionalization, the statement of the problema of predicting earth-
quakes. They are unthinkable without further etudy of the seiemicity of
the territory and improvement of the instrument obaervation network. With
an increase in construction intenaity the requirementa on the detailed
study of the seismicity grow. However, the succesaful aolution of the prob-
lem is connected with consideration of certain specific peculiaritiea. The
~ basic one of them is the high level of seismic interference caused by the
vital'activity of large centere which limite the seneitivity of the equip-
ment and makes it impossible to record weak local earthquakes which are of
special interest during perioda of "quiet" in the seismic regime. The
stations located at sufficiently greAt distancns from a city stop "noticing"
weak local earthquakea even before the city ha$ "felt" them. In addition,
for all earthquakes which can be recorded, the accuracy of the constructions
falls off as a result of the dietance between stationa. At the same time
when studying the seismic characteristics of a local area it is neceasary
- to insure high prfciaion of all of the conatruction, including tracing of
the zones tnat are seismically active at the pcesent time.
These contradictions greatly complicate the study of the seiam;c characteris-
tics of large industrial centera in seip^ically hazardous regiona.
Accordingly, during t1:e laKt deraaea the Inatitute of Earth Physics of the -
USSR Academy of Sciences in cooperation with the lnstitu-te of Ceo:ogy and �
Geophysics of the Kazat:h SSR Academy of Sciences has performed research in the development of procedures and equipme-it to study the seiamic character-
iatics of large industrial centers. SCudiea have been performed in the
vicinity of Alma-Ata, which ie located in a fcrce 10 zone for which a -
"quiet period" in the seismic activity is now characteristic. The basic
areas were to increase the sensitivity of the equipm;:nt and improve the
accuracy of the constructions.
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It nppeared that it is pdssible to achieve incre$sed sensiCiviey of the
equipmene under the apecific conditiona of a large city by organizing
obaervstiona in deep boreholes. Let us note rhar there is no experience in
deep-well seiemology in the US5R.
_ In order to increase the accuracy of the consCructions, first of a11 it
was necessary eignificantly to increase the accuracy of the Cime service.l
This could be achieved by centr$lized multichannel recording of the signals
at all statione located in the reeearch area with a united time service.
The prospectiveneas of thia recording wae determined by one of the basic
trends in modern seismology realizing the transition from observationa by a
network of ecattered statious located at great dlsCances (hundreds and more
kildmeters) from each other to observatione by a large number of stations
located in a comparaCively emall area. The groupe formed in thie case permit
use ef the directional interference procedure, correlation analyeie of the
waves and improvement of the resolution of the seiemic methoda.
The principlea of this area of atudy were laid down by the worka of
G. A. Gamburtaev on the correlation method of studying earthquakes in
Northern Tyan'-Shan', Pamir and Turkmenia �n 1951-1953 (21, 23, 27-29).
_ In this book a etudy ie made of the problems connected with the nentioned
- problems and also the results of 4 years of study of the seiamic regime in
Alma-Ata.
The first part of the book is on deep-well seismology. Descriptione are pre-
sented of the equipment and the specific peculiarities of performing
stationary highly senaitive seiamologic observationa in deep wells
(Chapter I), the laws of decrease in level of aeismic noise with depth.
An estimate is made of the poasibility of increasing the aensitivity of the
borehole observations under various seismogeologic conditiona (Chapter II).
It is demonatrated here that in order to increase the aensitivity and
accuracy of the constructions it is aignificantly more advantageous to
go "under the city" than away from it to the side.
Th. second part of the book contains a description of the Alma-Ata test area
of automatic ground surface and deep-well atations and also the radiotelemetric
recording system (Chapter III). A detailed descr3peion is presented of all
elemPntR of the set of radiotelemetric recording equipment. 'The basis for
the radio channel was the system developed by V. G. Katrenko [37].
In spite of the fact that the studies were basically of a procedural nature,
the data obtained as a result of operation of the test area made it possi-
ble to study the seiamic conditions of Alma-Ata. These resulta not only
confirm the effectiveness of the developed procedure but also are of
independent interest (Chapter IV). A detailed description is presented of
the initial mate:ial and the procedure for processing the multichannel
seismogrnms. Conaidering the novelty of the operatione, we have conaidered
it expadient to present a yuite large nwaber of primary seismograms in
the description.
1 [accurate hour's service] g
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tn thn cnncluding Chnpter V n descriptinn ig preaentect of the baeic
rer.ulinritiem aC the nriamtc conditions. A etudy wne madQ rhere of the
~ eEfect af the nbservation conditione on conetruction of 8eiamograma and
the nzimuthnl deviations of the seiemic beams.
'Chc nccumulnted experience has shown that the developed procedures and equip-
ment: can be recommended for studying the seiamic conditions of large indus-
trial cenl�erb ]ocated in seiamically dangerous zonea and also Co solve other
problems of seismology. Therefore the procedure and equipment are described
with a degree of deCail which is sufficient for organizatian of analogous
atudies in other areas.
This is nll the more aignificant in that the study of the weak local earth-
quakes la acquiring greater and greater interest in the rtioblem of earth-
quake prediction. Thus, in the second phase of the national program of
Japan for predicting eartriquakea whicli was atarted in 1976, in order to
record the weak local earthquakes in the vicinity of Tokyo provision was
madN for the creation of a Cest area of xhree highly sensitive stations,
the seismographe in which will be located at deptha of 2500 and 5500 meters
[76).
The book was written on the basis of reporta fromtfie coworkera of the
Laboratory of Deep-well Seismology Ye. I. Gal'perin, L. M. Vorovskiy,
R. M. Gal'perina, P. A. Troitskiy, A. K. Trofimov, A. I. Chesnokov. The
muterial was prepared by L. M. Vorovskiy (Chapters I, II, Chapter III,
91, 2), A. I. Chesnokov (Chapter*III, �3-5), R. M. Gal'perin: (Chapter IV,
Chapter 17, 52, 3), 51 of Chapter V was written by I. L. Nersesov, the fore-
word was written by Ye. I. Gal'perin and the conclusion by Ye. I. Gal'Perin
and I. L. Nersesov.
In addition to the authors, the reaearch was participated in by
V. P. Kharin and M. I. Moshul, and in individual phases also by
P. A. Troitskiy (1970) and A. K. Trofimov (1972-1973). V. G. Katrenko was
of significant assistance :.n organizing the radiotelemetric recording (1971).
A. P. Vorovskaya, C. L. Suzdorf, L. A. Ditler and A. V. Frolova basically
participated in the processing and interpretation of the materials and the
formatting oE the monograph.
All of the s[udies were performed under the direction of Ye. I. Gal'perin.
The authors express their appreciation to all of the coworkers participating
in the 8tudies and the preparation di the monograph.
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PART I. DEEP-WELL SEISMOLOGY
When solving many of the problems of seismology, highly sensitive operatione
are the basie determining the level of inveetigation. This pertaina, in
particular, to the study of the seiamic characteriatics of large induaCrial -
centers. One of the possible means of increasing the senaiCivizy of the
equipment is observation in wells or boreholea.l The new area is develop-
ing as deep-well seismology, and with each year it is finding broader and
broader application.
The seismic noise formed basically by aurface waves decreases with depths.
~ Nowcver, even the useful signal at internal pointa of the medium ie
weaker than on thE surface. This is explained by the fact that on the day ~
surface the wave ampli.tude is doubled as a result of reflection from the
earth-ai.r interface. The posaible gain in sensitivity of the equipment on
burying the seismograph is determined by how much fabter the noise 1eve1 -
decreF;ses with depth than the uaeful aignal.
- For ti;:: .ievetopment of deep-well aeismola>y it was firat of all necessary to
build equipment which could be uaed for observations in the wells, to atudy
the laws of variation with depth of the seismic noise background under
various seismogeological conditiona and to eatitaate the poasibilitiea of "
increasing senaitivity of the equipmenx,for o'oservations in boreholea. The -
resolvability of the seismic recording is determined not only by the signal/
noise ratio, but also by the complexity of the shape of the useful signals.
Therefore, along with the wave-noise distribution with reapect to depth it
is necessary t9 study the laws of variation of the shape of thp useful wsves.
These probleme are the subject of this part of the book. `
CHAPTER I. EQUIPMENT FOR BOREHOLE OBSERVATIONS
Observations in deep wells are connected with a number of specific peculiar-
ities of both a technical and theoretical nature. On the one hand, the
ltlere and hereafter we shall use the word sensitivity to mean useful
Rensicivicy, that is, maximum amplification that can be xealized with an
admissible noise level.
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decreaAe in seismic noiae level;with depth makea it possible to increase
thc, Hr.nHltivity nf nce r.quipmenr. On the other hnnd, nH n result of high
c:cmpartiturc ;tnd preeHUre, long length of the cable and other reaeons, the
equipment noise increases. In addition, the per�ormance of the observa-
tions in rhe boreholes is connecCed with ecological difficulties. The
basic meana of increasing the signal/noiae ratio under these conditiona
is the low-noiae equipment which has been developed and used for ehorC-
term (vertical seismic profile) and atationary observations.
- 91. Deep-Well Seismometers
Before the beginning of the described reaearch in the Soviet Union there
were no low-frequency seismometers for stationary seismological observa-
tions in deep wells. Comparatively few observations of a reconnaissance
nattre were performed in 1961-1962 using ground seiamometers designed for -
regl,onal studies (NS'3 with a natural freyuency of 2-4 hertz). However,
during the first years after the beginning of studies (1966-1967) low-
frequency seismometers were developed for seismological observations in
deep wel.ls. For deep well observationa of both short-term, prof ile and
stntionary type, aeismometers of two types were used which were developed
at the Inetitute of Earth Phyeics of the USSR Academy of Sciences the
SBU-V (deaigned by G. L. Shnirman) and SD-1F (designed by N. Ye. Fedoaeyenko).
The SBU-V seismometer. The deep-well vertical magnetoelectric SBU-V
seismometer (a high-gain, vertical seismometer) is designed for recording
the vertical component of the seismic oscillations in deep, specially
equipped wells [59J. The general view of the seismometer without the pro-
r.ective case is shown in Fig 1, a. In the upper part of the device there
is an automation compartment which provides for performance of the
instructions transmitted over the lagging cable from the control panel
located on the surface. In the lower part of the device there is a
pendulum compartment. The pendulum system (Fig 1, b) is in the form of
the mass M and the extensir,n arms P1 and P2 on which the operat3ng coils
K1 and K2 are fastened. The entire system is suspended on a cylindrical
coil spring ii with zero length so that the axis of rotation of the pendulum
and its center of gravity are in the same horizontal plane. On oacillation
of the pendulum, the operating coils are shifted in the annular radial
gaps of the two magnetic systems rigidly connected to the base of the
instrument (not shown in the di.agram).
The bnsic parameters of the seismometer ar.e as follows: coil resistance ;
about 300 ohms, the oscillation period is regulated from 0.8 to 1.2 seconds, ,
the reduced length is 11+2 cm, the electromechanical constant is no less
than 11 Webera/rad, the moment of inertia of the pendulum is 7�10'3 kg-m2,
the sensitivity on a frequency of 2 hertz is 0.5 mv/micron, the damping is ~
0.4, and the operating temperature range is from 0 to +80�C. The container
insures a seal at a pressure to 20 MPa. The seismometer set includes the
Eollowing: the seismometer itself, the grcund control panel, the feed
unit and the connecting cable. The ground control p:inel permits remote
realization of the following operations: locking and unloc:king of the
F
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aeismomeCer; awitching the ayatem on and off regulating the poeition of
equllibrium of the pendulum; measurement of the natural oscillation period
of the pendulum; feeding of the calibration pulae to the coils. The panel
feed can be realized either from the 24 volt sCorage batteries or the
220 volt AC networic.
Q

Po
n
PL
L.-
Figure 1. SBU-V Seismometer -
a-- General view with sutomation (1) and pendulum (2)
compartnents; b-- schematic of the pendulum.
Althoug}i the SBU-V seismometer is designed for stationary observations it
is necessary to note that it has been used successfully for profiling,
withstanding more than 500 cycles of unlocking, swinging and locking with-
out any siEnificant failures. During the stationary observations the
SBU-V seismometer can operate for years. In practice all of the station- -
ary observations were performed by the SBU-V seismometer.
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0-11~ Suigmometer. mhia seigmompter [571 is n dpvice with a magnetie
cushion nnd zero redured lengCh. The eesting of the geiemometer and the
dpvelopment of the rnntrol gystem for it Werp carripd out aieh the partici-
pation of the authors of thfe paper. The serueeurp and the opergtittg
princinle of the seigmometer are obvidug in Fig 2, e. Twn magneCg
(stationary 6 and moving 3 distrit,itted on aprings of the membrene type il)
are turned with the 1fke po1es c.vward each other. Thp moving magnet ig
the pendulum of the neigmdgraph. In the gaps of the twn mxgnetir oyetmmg
there are opergting coile: a eeationarp coi1 12 rigidiy connected to the
housing nf the devir.e and located in the gap of the moving magnet, gnd the
moving cdil 14 which ig fagtened tn the moving magnee and in the gap of
the scationary magnet.
The pendulum di the instrument (the moving magnet) is adjugted and euspended
by using additinnal mngnets: asegsing 1 and suppnrting 2. T'hp insCrumenC
is locked by pressing the pendulum into the exCreme loWer pnsttion Which ig
realized resnotely uging a reversible electric r.wtor 15 fed a direct current
from the day aurface.
The basic parameters of the aeiateometer are a$ follas,ts: amplitude range
of osCillations of the inner masg +S mm; damping 0.4; reaietance to the
operacing coil 600, damping coil 400 ahms; the period of the latural
vibrations is 1 second; the coefficient of elpctromechanical coupling of
the nperacing coil is 1.2 volt-seeonds/cm.
_ Fnr remote control of the epiemograph (the seiamometer) a control panel vae
used ahich has been developed and manufactured by V. G. Katrenko. The
panel is made up of four basic units: the pulse generator, stabilizer,
pre-amplifier and switching devi:es (Fig 2, b). _
By using the panel it is posgible to feed a voltage to the electric mocor
of the seismograph and tesc pulaes to the calibration coil of the pendulum,
to switc}i the inpuc of the pre-amplifier and the operating coils of the
pendulum, and to monitor the feed conditions. The pendulum is unlocked by
(eeding a voltage to the electric motor 15 (Fig 2, a) Which drive$ the
locking mechanism. When swinging the pendulura, its position is controlled
by heteropolar adjugtable pulses generated by the pulae generator.
'1'he pcriod of the seismogruph ia determined and regulated directly in the
Well using a panel specially manuEactured for thia purpose. The electric ~
response oE the pendulum sys[em to the test pulse is amplified by the
high-resistance DC amplifier and is fed to the nointing indicator. Afcer
swinginR the pendulum and establishing the required period, the seismograph
is saitched to the operating amplifier, and the control pulses are fed to
the recorder tape. The amplitudes of the pulses of opoosite polarity taust
be striccly the same in this case.
The SD-lF device Which is structurally simple and easily controlled can be
used successfully for deep-wellobserv,tions of the profiling type When
multiple repetitions of the unlocking-Lvinging-locking cycle are required.
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d
nt
/IJO
/!!d'
(2) dUI Ft 2T
~ /I!A
t
~
f /Jlt
irM e~
~
4/M
'ION

� ( 3)
,41 (6) ~ L
Figure 2. SD-1F Seiamomecer
a general view: 1-- astaeing magnet, remotely controlled
electric snotor, 2- aupporting magnet, 3-- principal magnet,
4-- magnetic circuit of the upper converter. S calibration coil,
6-- principal magnet of che los,rer converter, 7-- magnetic circuit
of the las+er converter, 8-- houaing, 9-- guide rad, 10 eplit
buehing for regulating the position of the supporting magnet,
11 diaphragm type springs, 12 operating coil, 13 nut for
regulacing the position of the mag;-t and the magnetic circuit of
the lower converter, 14 moving operating coil, 15 -!KH or
MSV electric motor;
b-- control panel electric circuit: 1-- pulee geaerator, 2--
stabilizer. 3 preamplifier.
Key:
1. output; 2. Shl; 3. P3a, P3b; 4. IP1; S. Pr; 6. Knl.
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It must be nneed Chae, nn the experience df 5 yeara of nbservaCinns has
indicated, the sensieiviCy uf the exigCing eeismographs cannoe be cnnsidered ~
aufficient. For ground obsetwgtiong in the differenC-phaees of the
resparch profile, semigCationary and etgtionary series geigmometerg
di the SM-2M, N5p-2 end VEGIK type were ueed. Inasmuch ge all of them are
manufgCtured in seriee, they gre deecribed in the literature (5), and
they have long bpen widely ueed in seismic reaearch, their characCerieCica
and parameeers are nat pre$ented.
prdtective Housings and Clamping Deviceg. The protective houaing of the
deep-well insCrument is deeigned to prnrect the elementg of the inetrument
from the exCreme pnvironmenC. For boCh of the deep-well eeismomeCere
the SBU-V and the SD-1F field protecCive housings were ueed which were
rovered by plugg dn bnth ends. The upper plug or head of the protective
- housing ig degigned td seal the hnueing, connect the ineCrument to the
cable and place the electric leada connecCing the cable atrgnds Co the
fngtrument circuitry in it. A specially developed standardized head wae
used itt which conical insulatora with internal electric leada were inserted
in the plug bridge. The inside volume of the head (just ae in the series
SBU-V) wag filled with chemically neutral cagtor oil which preventg accees
of water or drilling mud to the electric lead. The seal of the sciam(,graph
housing was realized using rubber aealing rings. The lower plug of tlte
preteceive houaing is deaigned only for aealing the housing. The protective
housinge vith a universal head that Were uaed demonatrated good reliahility
and dperation not only in the case of short-term but al8o long-tsrm atation-
ary observations lasting several yeare.
For the observations at any given depth and "disconnection" oE the device
from the day surface (when it is necessaxy to slack the cable), a clamping
device was used which serves simultaneously for rigid fastening of the
seismometer to the well Walls. Out of the many types of existing clamping
devices, a mechanical type unit vas selected as the simplest one, not
requiring additional cable stranda. The basic part of the dc:vice is the
spring (one or two springs, depending on the Weight of the Well unit)
mechanically released on raising the device and holding it at the required
depth. The displacement of the inetrument in the aell is from bottom to
top in the closed position. Nith proper adjustment the unit opErates quite
stably and reliably.
52. Preamplifiers
In connection With the difficulty of improving the sensitivity of neei-well [
seismometers, it appeared expedient to amplify the electric signal directly
at the point of installation of it for ahich a preamplifier Was installed.
Thc folloWing basic requirements are imposed on the preamplifiere operating
in drep aells and combined vith seismometers (the deep-s+ell preamplifier):
a) minimum dimensions; b) low natural noiae level at operating tempereture;
c) operating stability; d) feed econaay.
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It ig necessary to note that the difficulties in using the exieting
ampltfiere during etaCionary obeervatione at depthe of about 3000 metera
and Cempergturee of nare ehan 100�C are determined primarily b y tihe
temperature characterietice of the amplifiere and the natural noiee 1eve1.
Severgl types of amplifipre were teeted in Che varioua gtggee of Che
nbservations, in particuler, the K5E and Che RV3-T. Por obeervatione
at low temperaturee (Co 50�C) correspoading to depthe of 1000 to 1300 metere,
n preemplifier with negative feedback wae uepd ahich aae developed at the
Earth Physice inetitute of the USSR Acgdemyr of Sciencee (Fig 3, a). The
amnlifier hes the follmwing parametere:
Input imppdance, kilohma about
Noiee reduced to the input, microvolte no more than 0.5
T'rengmiesion coefficient with reepect Co
voltage, Kn 200
Feed voltage, vo1Ce . 1.5
Intake current, mi111amps 0.5
Operating temperature range, �C from -15 Cn +45
Operating frequency range from 0.6 he;rtz to
several kilohertz
The circuit diagram of the preamplifier combined with the SBU-V
aeiamometer is ehosm in Fig 3o b. Although the preamplifier itself itas
small dimensiona, placement of it in the houeing of the seiemometer
simultaneouely With the two Mare or Saturn type power aupplq elements has
involved some structural changes. It aae inetalled in the lightnitig
protection compartment, removing the diechargere.
The duration of the continuoue etationary observatione by the deep-well
seismometer with the praamplifier ie basically limited by the discharge
time of the feed elemente and amounte to about 1 year. Then the iastrument
must be lifted out of the aell and the power pack replaced. In order to
avoid exceaeive lifting and loWering operations, a power pack has been
developed which is placed in the eeiemometer and is fed from the gurface.
The achematic diagram of the power pack is depicted in Fig 3, c. It ie
a square-pulse generator assembled from txo traneistora. A 6-volt DC volt-
age is fed frmn the surface, it ia converted by the generator to the high
frequency equare voltage. On being picked up from the secondary aindinge
of the Tr-1 tranaformer, it is rectified, filtered and fed to the pre-
amplifier power supply circuit. The current intake by the unit is 10-13
milliampe.
In order to avoid feeding high voltage to the power pack and preamplifier
Erom the control panel of the SBU-V seismograph (as a result of which they
_ can be put out of order), the RPS-20 type PO relay ie introduced into the
c i r c u i t d ia g ram (Fig 3, b). Thia relay diaconnecte the power pack
nnd the preamplifier input from the control lines during the operations
of locking (unlocking) and sainging the pendulian of the aeismograph.
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c~
~1~ f~JA~~/
~
b-
~
FOtt O"ICIAL USB ONLY
. (3)
-~se
~r,,.~
K6 A 166 (5)
ftyd
(14)
xy /roK
~NM ~'Ilti,1 (7)
i~ss
t ! f t t~""'' (8)
' c
,
(1
3)
6
AM!
i
Af
mme
pi/t q,.ro.r~.nna /s,ner,re
'
(12)
xi'
~
~
( lOs ~+iw~r~tr
j
~/~YAr ~iAONOIA~/~Af~ 11 ~
.
Figure 3.
Preamplifier
a Rchematic
diagram; b
circuit diagram with
SBU-V
selemometer; c
circuit
diagram of the power pack
Key:
1.
input
7. cable atranda
2.
output
8. armor
3.
-1.5 volts
9. amplifier pover pack
4.
+1.5 volts
10. P4 is located in the
automation
S.
P416B
compartment
6.
C1500x6V
11. to thn automation compartment
12. 1.Dr2, kDr3, common
13. -1.5 volta
14. conmon
15. +1.5 volts
12
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~
~
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The pincpment of the preampiifier directly at the observgtion point permitg
the ereneroteeion of a sufficiently ampiified signal over thd cable Co Che
Aurface nnd eC Che same time makee iC poaeible to decreaee the electrical
inductione significnntly and increaee Che eena3Civity of the equipment.
93. Amplifying and Itecording Unit
The elpctric signal of the seimometQr amp,l3fied at the obaervaCion point by
g preamplifier is fed over the KBG-6 or KSB-6 logging cable from the
borehole eo the dmplifying a.ad recording equipment.
beviceg develdped at the Earth Physics Inetitute of the US5R Academy of
Sciences were used gs the power emplifiere in the different observation
etagea. The recording was done by the RV3-T type visible recorders [1].
Standard pen recordera were connected aC the output of the device.
.
In pgrallel With the visible recording by the pen recordera at some of the
obaervaCion points a recording was made by a ChISS frequency eelection
seiemic station with octave filtere (the reaonance frequenciee of the
filtere Were 1.4, 2.8, 5.6, end 11 hertz). The recording Was made on
photographic paper using tha RS-II recorder. The block diagram of the
seismic recording channel and frequency characterieCice are ehown in Fig 4.
At the automation etatione included in the teet area, the recording wae
made by a radiotelemetric unit which is deacribed in Chapter III.
The control of the amplificat~!on and etability of the characteriatice of
the deep-well seismic channels Waa carried out ueing the calibration
aignal of the constant amplitude magnetic generator (MGPA).
Thus, the situation with inatrument aupport of deep-Well aeismology is r,s
folloWg:
1. The exieting seta of equipment for thq aeismic obsetvations in deep
' wella normally operate at temperaturea to 50�C Which in the vicinity of
Alma-Ata correeponde to deptha of 1200-1300 meters.
2. The uae of a preamplifier directly at the point of inerallation of the
eeiamometer in the well easentially increasee the uaeful seneitivity of the
equipment.
3. The eensitivity of the deep-Well eeismometer is inaufficient for
observation in deep wells. For profile well observations it is expedt.ent
to uge the SD-1F seismometera diatinguiehed by simplicxty of control,-and
for prolonged atationary meaeurementa, the SBU-8 aeiemometers ahich are
atable and reliable in operation.
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xi I ~y UAivNy /.'ep0n0- ~
(c)` i
~
, - -Y ParutmAamo' (d) ~
Nu,v
.
4
N,..,~ (1)
0
~
~
j
~
( f )
!
(k)
~
~LMO ~
lhlA
Nllti
,vp
l
,
~u~ntA~
~
a
,
'
b
!
~
~
r
t
0
~
i
.
;
i
V
~
!
^_7 -
( n.aoNO~eM,ow
I BAOK ~i~ ~
~ ~an~mPad
~ (h)
4j /,0 r 0 IO f,rq (m)
Figure 4. Seismic Channel
a-- block diagrani; b-- frequency characteristics of the
seismometer (1), the amplifying and recording channel (2),
the entire channel (3) and the reproduction fitters of the
ChISS [frequency seIection eeismic atationj (4)
Key:
a. Chronometer h. Filter unit
b. Terminal amplifier i. Galvanometere
c. Pen recorder J. ChISS (frequency selection seismic
d. P.ecorder atation)
e. Contrul panel k. Seismograph
f. Borehole or Well 1. Preamplifier
g. F.lectric power supply m. f, hertz
14
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4. For the further development of deep-well aeiamology it ie necasaary to
improve the deep-well equipment. The basic aregs here are the following
_ devplopmente: a) eingle component and tripie component deep-we11
aeismometere with a naCural oscillation period of 5 seconde, the seneitivity
of which ie 20-40 timee greeter than the pxiating ane; b) amplifiers with
1ow noiee 1eve1 and Channel multiplexing equipmenC for Crangmiee3on of
informatinn from rhe well over the small-core cabiej c) vers3ons of the
deep-well equipment with thermal etability to 120�C.
15
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CHAPTER II. SENSITIVITY OF DEEP-!1ELL OBSERVATIONS AND STRUCTURL OF THE
SEISMOGRAMS
At ehe presenC time the operations with respect to increaeing the seneitivity
of geiemic operatione are developing in two areae.
The firet of them ie connected with wave selection by ~jrtain parametera
characterizing the wave field. Here, in addition to ::he traditional wave
seleceion with respect to frequeacy, the weve selection with respect to the
direction of propagation and velocity ie acquiring more and mnre eignifi-
a cance in recent timea. In procedural reapecta it ie connected aith groupa
uf aeiemographe located along the line or on the observation plane. In
addition, wave eelection with respect to the polarization attribute (the
polar�zation filtration) has developed which is based on wave eeparetion
at the point with respect to the direction of motion or with respect to the
- nature of the trajectory of motion of the particlea of the medium. The
sensitivity increases aignificantly on combination of both types of wave
aelection with respect to direction of propagation and polarization of the
waves [16].
The aecond area is based on the remnval from the eurface, that is, ehe
observatione in the welle [17). In each apecific eituation, depending on
the goals of the reaearch, the nature of the wave interference end obeerva-
tion conditiona, different methoda of improving the ueeful aenaitivi!y or
- combinatione of them can be selected.
When atudying the eeiamic characterietica of large industrial centera, the
- epecific obeervation conditions greatly coniplicate and aometimes exclude
the poasibilitiea of uaing the methods based on wave selection With respect
to direction of propagation. At the same time, the wave interference
primarily made up of surface wavea gives rise to effectivenese of the
second area. Therefore when atudying the seismic characteristics of local
sectiona of large induatriAl centere the aeismic observations in boreholes
acquire special interest. 'i'his chapter diacusaea thie area.
Let us characterize the state of the art with respect to the available
published data and thus describe the experimental studies performed by the
Earth Phyaice Inatitute of the USSR Academy of Sciences in velle drilled
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.A
to a dcpth of 3000 mntera baeically in terrigenic depogita and located in
nrnna with fiigh (Almn-Atn, 'Cnahkent) nnd low (rhe viiinge oF Chi11k) noiee
levele and also in ahallow (to 100 meters) we11s revealing the cryeta111nf
fnundetion.
When egkimating Che aensitiviCy of the equipment ir is neceesary firet of
a11 to diecover the laws of variation with dppth of the level of aeiemic
noise end useful signal.
The variation in noiae level with depth was inveatigaCed by Che meChod of
verrical seismic profiling (VSP) (15). Kowever, the background interference
not only changea with depeh, but it is also characterized by great variabil-
iCy in time. in order to etudy Che time igwa, long-Cerm gemietationary
and stationary observations were performed in the wells. buring these
observations a large number of differenC earthquakes Were recorded in a
number of we11s at different depthe.
The performed observations made it poseible to eatimate the poasible gain
in sensitivity during the deep-well observations and also to comgare the
shape of the recording of individual wells and the atructure of seiemograme
obtained at different depths and on the day aurface.
41. State of the Art with Respect to Seismological Observatione in Boreholea
(Brief Survey of Published Data)
In the last 20 to 25 years studte$ were made abroad (especially in the
United Statea and Japan) with reepect to the development of seismologic
observations in wells. Sets of deep-well equipment were developed, and
studies were made in areag of different structure in the depths range from
several tens to 6000 meters. It is necessary to note that in the publiahed
materials the data on poseible gain in aensitivity of the equipment are
presented only in some of the firat papers; primary attention in the majority
of the papera has been given to the Wave interference characteriatics and
a discussion of their nature.
One of the firat papers on estimating the poasibility of increasing the
sensitivity of the equipment during recordinga in wells muat be considered
to be the experiment of (80) performed to isolate wavea reflected from the
Mohorovichich surface. The observations performed in three boreholea at
depttia oE 1000 meters demonstrated that the natural noise background at
the surface is appreciably greater than at depth. Thus, whereae on the
surface the noiae level reached 40 microvolts, at a depth of 1000 meters
it was about 4 microvolts, and in one of the wells it was 1 microvolt and
did not differ from the natural noise of the amplifier. The fact of a
decreased noise level With depth indicated the important role of the
Rayleigh wavea in surface noiae. The resulta of theae observations have
conEirmed the theoretical propoaition of the posaibility of increasing the
sensitivity of the equipment by b uryiag the aeismograph.
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The seigmological observatione in wella began to develop quickly at the
end of the 1950's. This wae promoted to a;raat extent by the epecial
studies to compare the recording additi.ona tn cased and uncased wella,
which demonetrated that undel the condition of a we11-cemented well and a
reliably clamped seiemograph the recordinge in' the frequency range of
15-70 hertz were not diatorted by the effece of the casing (71). The
compleCe identicelness of the recordings 3n the cased and uncased wells
wag also proved and, at the eame time it wae demonetrated that the cased
we11s cemented to the head did not dietort the recordinga in the frequency
range from 1 to 10 hertz. Theee resulte greatly aimplified further studies,
for the recording in an open well ie always fraught with the danger of
losing the aeismogreph and failure of the well iteelf.
Eor convenience of inveetigation, all of the borehole obaervatione can be
prnvisionally divided into three groups: observations in shgllow welle
(to 100 meters) (66, 77, and ao on], medium-deep welle (to 600 metere)
[77, 78, and so on), and deep wells (more than 600 metera) [64, 70, 72-75,
and so on]. The drilling of ahallow we11s ie appreciably cheaper and
observntiori eimpler in connection with which the evaluation of the feasi-
bility of increa8ing the sensitivity here is of special interesC. The
observaGions in deep welle aLe coupled with great technical difficulties
caused by increased presaure and temperature.
Let us present the basic observation results.
bbservationa in Shallow and Medium-Deep Wells. The moet cotaplete atudies
of noise in shallow wells are preeented in reference (66), which permitted
its authora to formulate certain concluaiona.
Apache Well (Oklahoma). This area is one of the "quietest" placea in the
continental United States. The depth of the borehole is 18.3 metera. The
weatttering zone ia very thin, and the ground seismometers were inatalled
directly on limeatone. The background in the period range of 0.3-1.4 aeconds
is made up almost completely of oscillations with a neriod of 0.5 aeconds;
the 0.5-second apectral peak ha8 a mean amplitude of about 0.2 nm2/hertz.
On a still day no signiEicant difference was observed between the noise
level on the surface and in the well. The probability of the occurrence
of a bnckground of the given or smaller amplitude is illuatrated in Fig 5, a
t)y which the decrease in noise level connected with wind at a depth of
18.3 metere is obvious. From the histograms of noise of different
periods on a still day with a aind velocity of 20-40 km/hr it followa that
the noise is repreaen[ed basically by oscillations With a period of
0.5 seconds; the insigniEicant predominance of the long-period component
in the borehole by comparison with the surface is noticeable. The depth of
the borehole is insufficient for complete disappearance of the aind noiae.
Wichimo Mountain Well. The surface and deep-aell seismographs Were installed
on bedrock (granite). On a still day the background interference level on
the surface differe little from the background interference level in the
borehole. During windy weather with a wind velocity of 30 km/hr at depths
18
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i
I D M 04 0410
e+1
~ v ~ g O Q pa ~ O 4C p;
� s} M 3 ~ ~
or
J a ~
w

' u
tl

. S
v
~r.r1
~
1
~ o
~s--�
~ N ~
~

v
. s
��S
.
e ~

'+,''0
4 Z
N
~
c
^
!
~
a
~
V

~
YM 1
~1
b
~
.
v V
~ Z
M
14
a
~~a
O
z
.~L
~
.
v1
R)
Cl
~
L
14
~
ti
-w
W
'I"1
~1,
W
r4
1
~
~
w
N
O
~
w
19
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r
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. [Legend and key �or Fig 5, pxeceding page]
a-- probability of occurrence and percenCage content of noiae in the
period range of 0.3-1.4 seconds at the surface and at a depth of 18.3 m
(Apaahe, Oklahoma): 1-- etiill day, aurfaae and a depth of 18.3 metera,
2-- wind velocity 20-40 km/hour, depth 18.3 meters, 3-- wind velocity
20-40 lc.m/hr, surface;
b-- energy epectra of the noise in the Pinedale well (Wyoming) on the
surface (1) and at a depth of 32 meCere (2) and in the Winner well
(South Dakota) aC night (3) and in the daytime (4);
c-- amplitude ratios of the noise shifts in the we11 at different depChs
and on the aurface (Japan) for different frequency intervals (1, 2--
horizontal componenta, 3-- vertical component).
Key:
1. nm2/hertz
2. 1`, sec
- 3. X, nm
4. f, hertz
~ of 61-36 meters, no wind interference wae detected; at a depth of 18 m
only an inaignificant part of the background is connected with wind.
Pinedale Well (Wyoming). A well 61 meters deep waa drilled in shaly clay
having a longitudinal wave velocity on the bottom of Vpl3.0 km/eec. On
a still day the background level with respect to SOX probability level
decreased with depth and at the bottom was 0.7 of the aurface value. The
amplitude of the useful aignal at the same depth decreased to 0.9 of the
surface amplitude. Table 1 shows the results obtained when analyzing the
recording at different deptha. At a depth of 61 metera the noise connected
with wind is not obaerved in practice.
The peak in the borehole noise epectrum (Fig 5, b) between 0.7 And 0.4
seconds is caused by the fact that the noise connected with wind doea not
diminish at this shallow depth.
Table 1
V~

noe
(3) C~cea~cNNe
a~,
~
I
( y' 0)
A cKe I 'xM
H, u
A /A
cKS noe
2
-
(4)
ks)
(6)
0-8
2,5 '
2.0
32 '
0'8
35-50
6,5 �
2,8 .
32
0.43
0-8
2.7
2,0
48
0074 .
30-35
4,0
2,3
81
' 0.58
50-80
8,8
2,3
81
0,34
Key: 1. V, km/hr; 2. Aaurfa , nD; 3. borehole; 4. Aborehole'
- 5. H, m; 6. Aborehole~~surface
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Winner Well (Soueh Dakota). The level of microseiemic background in thia
area is very high 26 nm; Chexefore the "wind" background is not isolated
on the surface recordinga. The decrease in background wtth depth takee
place on the average from 20 rnn at the eurface to 16 nm at a depth of
56 metera and 5 nm at a depCh of 302 meterr,. The mean amplitude of the
signal at a depth of 302 meCera was 0.33 nf the eurface amplitude, and
therefore the aignal/background ratio increased by only 1.9 timea. The
peak at 0.35 aeconda at night (Ffg 5, b) ia appreciably leas than'in the
dayl:ime, and thts indicates the "cultural" origin of the background.
In the opinion of the author of reference [66], a reduction in background
level with removal from the surface is explained by a decrease in intensity
of both aurface wavea and volumetric waves. Ttke decrease in amplltudes of
the surface wavea in the presence of a low velocity zone takes placea
eapecially rarely. The decrease in the noise with depths, which is
especially faet in the upper part of the section, is also cauaed by a
decrease in the noiae of "wind" origin.
Tolcyo Meteorological Institute [78]. When studying noise at depths of
10, 20, 50, 100, 150, and 200 metera the following resulta are obtained,
1. The decrease in noise level is more significant for nigh frequencies,
which is obvious from Fig 5, c. The noise amplitude ratios in the well
and at the aurface for different frequency intervals are indicated. For
example, for a depth of 50 meters (vertical component) the noiae amplitude
ratio in the well and at the aurface is about 0.05 in the frequency range
of 6.3-10 hertz.
2. The low-frequency noise amplitudes (less than 0.5 hertz) decrease
weakly with depth.
3. Significant improvement of the signal-noise ratio is achieved at a
~ depth of 50 meters. In general the optimal depth depends on the geological
structure,andfor each area it must be determined experimentally.
4. The noise connected with a passing series of transport vehicles or
with falling of heavy weighta ia not sensed by the borehole instrument
even at a depth of 50 meters.
In reference [17) a description is presented of the observations in bore-
holes 64 meters deep (Nokogiriyama) and 380 meters deep (Hongo) performed
to increase the signal/noise ratio when recording microearthquakes in a
frequency range of 5-100 hertz. The noise ratio at the surface to the
noise in the well 64 meters deep is equal to two, and in a well 380 m deep,
10. The signal/noise ratio at a depth of 64 meters is only somewhat
greater than on the surface, and at a depth oE 380 neters, three times
greater. The useful signr,ls are recorded more clearly in the boreholes;
therefore it is expediem. to obaerve microearthquakes in the we11 even if
it is not very deep.
21
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nbservations in neep We11s. A detailed gnalyeis of Che observgtion materinls
in Chree deep wplla is pregented in reference 165j.
Grapevine Weil (T'pxae). Thp Clrapevinp iie11 is 3040 neeers dpep, iC is
cased, and the cement ie raieed 304 meCers from the bottom. '1'he noiee
characteristic in the weil is ehovn in Fig 6, a. The curve for the
decregse in nnise amplitudp dppth ig constructed aith reepect to the
502 probability level. The greater pare of the noire in itt the period
range of 0.3-0.6 eeconds. The noige decreaspe rapidly With depth and
approgches a coneCant value of 1.5 nm; thie is caused, in the opinion nf
thp author, by the volumetric wavee, ehe noige 1eve1 from which, in
cuntrast to the surfgce waveg, doeg not change vith depth.
The Hobnrt Well (Oklshona) is about 3000 metere deep, it is caeed. and the
rement ia reieed 304 matore fran the bottom. With respect to the noiae
variation curve With depth (Fig 6, b) it is obvious that to a depth of
2130 meters the iaw of vgriation of the noiee amplitude is the same ae in
thp Grapevine We11, which indicaCee the eame type cf wsve. Lcnier down,
the noise level again begine to increase. This depth corregponde to the
low-velocity layer, and tfie increage in noiae lavel can be connectpd With
kave guide phenomena.
Orlnndn Well (Florida). The Orlando tiell (Florida) is 2080 meters deep, it
- is cased and cemented 945 meters from rhe bottom. The surEgce noise is
- highly unetable ee a reeult of law-f requency interference (0.3-0.5 eec)
comiected with the tictivity of tnan. At depth the long-period noiee pre-
dominates (0.8-1.5 eeconds). Along the curve (Pig 6, b) the noise varia- ~
tlons aith depth coristructed by the 50% probability level it is obvioue
that the noise decrease corresponda to the damping of primary mode of th8
?tayleigh Waves. A aharp improvement of the eignal/noise ratio for high-
frequency signals is a characteristic feature; the high-frequencynoiee
almoat completely disappeare at a depth of 1975 meters.
In the opinion of the author of (65], obeervations in three welle demon-
strated the following:
1) The noise level decreases vith depth; the degree of the decrease depende
on the frequency and the eeiamogeological charecterietic of the section;
7) The amplitudes of the useful aignal decrease aith depth aed reach a
minimum at a depth equal to half the aavelength reflected from che surface;
3) The Rayleigh vaves predominate in the noise;
4) The recording divisions in each aell are different, and the estimation
of the gain in sensitivicy for each of thera must be especielly determined.
In general, the submersion of the seismographa will perroit us to obtain a
signal/noiae ratio of the same order as in the "quietest" continental
areas.
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Figure 6. ttoiAe in Deep Nellg
a-- probability of oecurrpnce of noiae gnd vdridtivn nf it vith
dhpth in the Grapevine Well (rexae) in the period rgngp of ,
0.3-1.3 seconds: 0-- eurface, 1-- 0.2, 2-- 0.5, 3-- 0.6,
4-- 1.3, 5-- 1.80 6-- 2.4, 7-- 3.0 km. Curvp I age conetructed for a predominant period of 0.3 eeconds;
b-- the abeolute and relative noiep amplitudpe in the Nobart
Weli (Oklahoma) (rurve 1) and the Orlando Nell (Floride)
(curve 2). The numbera at the dote are the predominant periodg.
Key:
1. X, nm
2. Arelative
Nature of the Noise. If the lave of variation of the noige level in the
aell accnrding to the data of vArious euthorg agree among egch other, then
the opinions of the authors diverge in the problem of the nature nf the
noise. In eome papera (64, 74, 751 the noise is interpreted as a combina-
tion of different modea of the Rayleigh wave, in (691 and other papere the
basic propertiee of noise are explained from the point of vies+ of the
stationary compresaion vaves. In reference (67) uhere the results of many
years of etudying the noise background in the vells with different geological
atructure are suoaaed up, the nature af the seismic noise is explained as a
mixcure oE volumetric and surface vaves. Defined combinations of different
typea of Wavee correspond to different period ranges. Thus, the ratiog
of the noiae epectra at the gurface and at a depth of 5200 meters and also
the cheoretical curves of the firet three Rayleigh aades and P-wavee for
normal anglee of incidence for the Fort Stockton Well (Texas) permit the
author to coneider that the cauee of the noise in the aell can be the
23
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presence of different cypee of aavea in ehe adjacene period rgnges and aloo
the presence of Love aaves. 'Phe regultg obtatned in ehe pinedgle Nel1
(Wyoming) are expiained bese of ail by e combination of P-+wavee and the
basic ttnylRigh mode.
For the ApaChe Ne11 (Oklahoma) thc experimentel empiitude-depCh ratios in
the perind range of 2.0-0.8 seconde agree ae11 aith ehe theoretical eurves
and the P-Wavee in the Rayieigh tcode. '1'hp gutocorreiation analynir of the
reeordings after digitai fiitration performed to separate these t`o casrg
demonstrated thgt the noise ie made up of surfece aeveA. 'Phe noise in the
peridd renge of 0.8-0.3 eecond� ie uauaily connected vith regpect to its
nature to the cioseness of populgted placer and their greater "cultural" ,
gctivity. Thp noise spectra for the Qrapevine Wali located near the lgrge
indugtrial center of Daligs, Texas, are characterizpd by a vaet decreage in
noise vith depth ahich ie determinpd by the primry Etayleigh mode. At
depehe Where the ampiitudp of the primgry mode ia email, the aeplltude-
depeh ratio cgn be expiained either by a combination of higher mndes ar by
voluroetric aavpe gnd interference of tao typee of vaves.
Reference 1821 containe a degcription of the obgervatioris in the Crepevine
Nell perfonapd eimultaneously by four three-component devices loceced at
depthg of 139, 1062, 1951 and 2885 metere. The reeulta obtained confitm the
fact thet the selemic noise is mde up of a eet of Reyleigh aeve modee,
but, in addition, different Love vave modee are alao present. The volu-
metric vavee aere not dptected in the areA ahich is connected aith the
pre$ence of a high level of "cultural" noiee. It ie noted that ie the
areas Whpre thpre is no high 1eve1 of "cultural" noiee. the volumptric
Wevee make a eignificant contribution to the eeisraic noiee.
In eddition to thp above-noted baeic wotks, others [72, 73, 79] are knovn
in ahich atudies aere made of the seismic noise and its nature. A8 a
result of analyzing the-publiahed papere it ie possible to draw the
follnwing conclueiona.
The noise level decreasee aith deptha; at great deptha the differencee in
noise intensity for different areae and veriability of noise aith time
aithin the limita of one section are appreciebly lees than on the day
surface. The degree of decreaee in noise with depth for different areas is differpnt end depende on the frequency and the aeismogeological
characterietic of the section. The fastest decreaee in noise irith depth
!e obgerved in the areas With a high level of "cultural" noise. Por losr-
noise areas, the decrease in noise aith depth is observed only for the
high-frequeney cotoponenta of the epectrum. In the individual eectiona
of thp vell egainet a background of general decrease in noiee, local
buildup of che noise can be obeerved connected with the vaveguide phenonena.
The aignal level decreases With depth and reaches a minimum at a depth
equal co half the uave length.
1("Cultural" is ueed throu hout to refer to noise geaerated by
eepecially ae in ci[iea.#
24
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Usefui SQasietvity af ehp Bnrehole 3eaeidns. This indpx must be specially
pseimnted. Thp grhatest ggtn can be obteieed in areas with high graund
ndise levpl. In g11 cases the eubmergion of the seismograph makea it
poaaible eo obCain asignal/noise ratio of the eamp order ae for ground
observaeione under ehe moat fgvorable conditions.
The gignal/noige ratio at a depth of 100 meters increaeeg by 3-4 timee
for frequencieg of 2-10 herta. The number of igolated earehquakes in the
prpgpnce of borehole observacions increases by 2.2 timeg.
11
The appliaation af complex vereical oygtem ia effective only fdr arean -
with a high level of ground noise and ashgrp decreaee in them with depeh.
Here the signal/noiee ratio cen reach vgluea of 15-25 decibele.
42. tavs of Variation of Noiee tevel with Depth -
'Che obgervationg Were perfermed by the VSP Cverttcal eeiamic profiling]
methnd in Wells loCgted in different grege with respect to noige level.
"fhe Tdghkent and Alma-Ata Ne11e are located under cond!tione of high ground
noise lpvpl conneeted with the vital activity of large indugtrial centere.
In rhe Novo-A1ekseyevekaya Well the high noiee level ig connected with a
concentreted gdurce lOCdted nearby (the building mnterigle combine) gnd
the Chilik iJp11 ig located under high noise level conditione.
Obgervatfone in Largp induetrial Centere. Taehkent. Thie borehole is
designed epecially for geoprygicaY measurements and it was drilled in 1968.
It revealed Quaternary, Neogenic, Paleogenic, Cretaceous and Triaseic-
Juragaic deposit8 and WQnt into the Peleoaoic at a dQpth of about 2400 m.
The bagic obaprvations aere performed in June and October of 1970. The
reaultg of the observationa of different eeries egree with p8Cf1 other.
According to the grephs of the variation of maximum noise amplitudes with
depths (Fig 7, a) it le obvious that on che day eurface che noise level is
very high and fluctuaceg at different timee of day with brnsd limits.
Nheress in the daytimp (the dntted eurvee) at night ~
(the solid curves) it ig a total of 80 cm.
Nith an increase in depth, the intprferpnce background diminieheg. The
sherpest decrease in noiee level is observed in the upper part of the
gection. At a depth of 350-400 meterg the noiee level already decreasee
by approximately 1-1/2 ordere. At greater deptti the decrease in noiae
takes place appreciably more elowly. In the depth rangh of 400-1000 metere
the incerference background diminiahes on the average anty by 2 timea.
tn the depth range from 1000 to 1800-1900 meters, a total oE tvo series of
observations Were made at different timea. The inteti-ference level
decreases still more slovly here, and at maximum depths nt night it is
2.5-3.0 and 9-10 nm.
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A gtab1e differencp ig obeerted in the noise backgrdund ieve1 gti nfght and
in the dgytimp.. On the day suxfece the noiee baekgraund 1eve1 in the
daytime can be an order higher rhan at night. Wirh an inereaee in depth
this difterence diminiehee, gnd in the depth range of 300-1000 metera the
ratio of the background noiee 1eve1 on the average in two.
'Che minim:.ai noise beckground both on the day eurfgce and at interngl
pointa of the medium aas obgerved ae night on a holiday. For thie aeries
gignificantly amaller decregge in noise ampiicude aith depth in character-
istic ttian for the nthpr nighttime obgervation gprien.
For cdmpariaon with the background amplitudee on the eurface and 3n depthg
synchronoug recordinge were mede of the borehole and ground seiemographg.
The varigtione in background ratio on the surface and at depth ere pre-
apnted in Fig 7, b. Por the day geriee the raeio in the upper part of the
seceion incrpagee sharply at first. Thua, in the depeh renge of 0-200 m
it varieg by morp than an order. Nith a further increaee in depth it greag
aignifiCantly mnre gloWly, and in the 200-1000 meter rgnge it triplee in
n11.
At night the ratio of the noige amplitude in the aell end on the surfece
in the upper part of the sectiori increaaes more elowly, end the velue of
ten ig regched only at a depth of about 400 metere. At greater depths
the "night" and "day" graphA coincide. The Sunday obgervatinn series for
Which minimum noiee amplitude ratioa are characteristic constituteg en
exCeption. At a depth of 1000 meters this ratio is 14, at the eamp time
as for the remaining series it ie 50.
A comparigon of the graphs constructed with reappct to the maximum ampli-
tude level and With respect to the avetege maximmn amplitudeg indicatee
that the average values are smaller than the maximum values for approx-
imately 20-302.
The predominent interference aave periods on the day aurface amount to
abouc 0.2 seconde. At the internal points of the medium g]ready beginning
at SO meters, the perioda are equal to 0.3 eecondg, and they vary very
slowly Wi[h depth. At night the predominant noise period is eomewhat
greater than in the daytitae.
Alma-Ata. A aell 2000 meters deep Wan drilled in the terrigenic coaraely
claecic depeeits for ahich continuoue increeae in velocity aith depth ia
chnracteristic. In the upper pert thia groath tAkea plece nwre eharply,
and with depth, the velocity buildup gradient decreaees. The curves for
the amplitude variation in the depth range of 0-950 meters for three day-
time observation aeries and four nighttime aeries (Fig 8, a) indicate
that the obaervationa of the different eeriea egree aell with each other,
grouping quite narroar bands into tRro: day and night. The interference
backgreund in the daytime and at night differe on the everage by two timee,
nnd the neture of the aaiplitude decreaee aith depth is approximately the
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gamh. Zn the upper pare of the seeeion (50-250 meeera) a sharp decreage
in noiae wirh depeh in nbnervedt the noise gmplieude decreaees at night
in praeeice by en order (frdm 270 to 25 nm), and in the daytime by g
haiforder (from 220 to 40 nm). in thp depth range of 250-950 meCere the
noise ampiitude decreaaee a totai o! 3-3.5 timQe (from 40 to 13 nm in thp
daytime and from 25 to 7 mn at eight).
The staeiaeical processing of the 10-eecond noiae recording ineerval of
_ the daytime serieg made it pasaible to coneCrueti the prabability curves
for ehe occurrence of noise of given or loapr ampiirude (Pig 80 b). By
rhe Gurvea it i8 obvieug thae, for example, at a depth of 150 metera the
probability of occurrence of noise aith en amplitude of 40 nm and 1esa
ie 60%. At a depth of 850 meters it ie pooeible to expecC Q ehift of
8 nm or laeg with the eame probability of 602. For the aame dapth the
= probability that the background amplitude aili not exceed 17-18 nm wili
bp pqual to 100X.
For compgrison, in the same figure the dara ate part of the curve obtainpd
in the f;repevine We11 (Texas, U3A) in ahich a very large volume of aork
wes done to study noige. Comparieon ehowe that on the rurface the noise
ievel in Almg-Atg in eeAentially higher t1tan in the Grapevine Well. Thue,
+ahereae the probability of the occurrence of noise with an amplitude of
100 nm .,r legs in Alma-Ata at a depth af SO metere ia 15%, nn Che eurface
of thp Grapevine Well it is more than 90%. At the eame time at a depth
of 650 metere the probability curvee ditfer ie practice 1itt1e. The
difference in intarference levels nbviouely ie explained by the fact that
the Crapevine Well, in contraet to the Alma-Ata Well, ie a distance of
abaut 50 km from a large city (Dallae). The curve for the noise amplitude
as a function of depth for the day eeriea of obeervatior.s in the Crgpevine
We11 congtructed aith reapect to the SOX probgbillty level (the heavy
line atth circles in Pig 8, a) lies in the regioe of the "night eerieg"
of observationa in the Alma-Ata i1e11.
From che graphs of the noise apectra at different depths (Pig 8, c) it is
obvioug that maximwa noise amplitude both at the day eurface and at
greater depthe correepond to the long-period caoponenta of the spectrum.
In the frequency band from 0.2 to 0.8 hertz the nature of the decrease
in noise aith an increaee in frequency at the day surface and at depth ig
identicnl. At a frequency of 0.8 herez the noise level at the day eurfece
aill be 0.08 nm. The noise level at a depth of SSO meters in this frequency
range is approximately an order loWer than on the daq eurface. Beginning
aith 1 and up to 4 hertz, the neture of the decrease in noise variee
shnrply. At the day surface ngeinet a background of sharp peaks, aome
increase in noise level fs observed at the eame time ae at a depth of
H=SSO meters.the noise level decreasee, but this decreaBe takes place
eppreciably more eloWly than in the low-frequency range. In the 5-7 hertz
band, the noise amplitude at a depth of 550 metera is 40 times lees than
at the day aurface. Por the entire imreatigated frequency range the retio
of the apectra at a depth of N-950 meters and at the eurface (Fig 8, c)
. M
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io 1ean than one. "Che raeid becomea minimal in the 1*7-2.7 hertz band.
'Che neture of the decreaso in noise on frequencipe in the range of
0.2 Cn 1.0 hertz permite tfip coneideration thae the basic moden of the
Rayieigh waves predaminat@ here. In the higher frequency band the noiae
can be reprenented by a combieation of baeic, firat and gomet3mes second _
Rayleigh moden and tfie volumetric waves. Inaemuch an the well in
lacnted directly an the edge of euch a large indugera.al eity as Alma-ACa,
the nuige ean be expiained primarily by the "culturgl" activity of the .
ciey.
Observationg in Arpag with Loot Level Nttgp gt UepChs of 300 and 600 Meters.
7'he observations in we11s severel hundreds of metera deep are of grpat
interest. Thie ie explained by the fact that the we11e gre aleo compara-
tively cheaper and can be driiled by portable drilling rigs. In gddition, i
frdm the technical point of viea the obeervatione at thpge depths gre
appreciabiy eagier and equipment is appreciably eimpler. At the eame time,
ng xae demoneeratpd, the eharpeet decreaee in beckground occure in the -
upper pgrt nf the eection.
The pnggibilities ot the observatione ere eetimated by the materialg
obtained in the Chilik borehole. In contreat to the Tashkent and the
Alma-Ata We11s, the Chilik We11 is located at a gignificant distarce Erom
the large citieg which cauees apprpciably emaller background of the above-
ground interference and permitn synchronoim observgtione on the day surface
and in the well.
The Chilik Flell, the depth of Which ig 600 metera, is located on the edge
of the rayon center of Alma-Ata Oblagt aith the same name approximately
100 km east of Alica-Ata. in geological reapects this area differs from the
previougly investigaeed onee by leee thicknees of the gedimentary depogite
Which reach a total of 1350 metera here and are represented, just as in
Almn-Ata, by terrigenic coarsely claetic rock. The vertical seismic pro-
filing by individual eeriee in the day and night with a step of SO meters
over the entire depth interval uade it possible te obtain the curves for
the vnriation of the noiae amplitudee for tao night and txo day seriea
(see Fig 8, a). In the daytime the noiee level quickly decreasee aitli
depth, nnd at 100 meters it is en order loaer than on the surface, gnd at
300 mptera, 20 times loo+er. In the range from 300 co 600 metera the noise
amplitudes are cut approximately in half. At night the noiee background on
the day surface is essencially 1oWer than in the daytime, and it decreases
aich depth more slovly than in the daytime. Thus, at a depth of 300 metera
the noiAe background 18 3 to 4 times less than on the day 9urface.
The predominant-noi9e frequency on the recordinge obtained on the surface
is abouc 3 hertz; at a depth of 600 meters it decreaaes to 2.5 hertz.
The apectral analyeis shoWS (Fig 8, c) thac the nature of the epectral curveg
for the Chilik Nell is analogous to the same curves for the Alma-Ata iJell.
29
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~A .
1AV (3)
1N X, NM
l/y ~Owt~~
1V1/
'ay
Figure 8. Noise background at night (solid line) and in the
daytime (dotted line) in the Welle of Alma-Ata
and Chilik
g-- noiae amplitude ag a function of depth for the Alaia-Ata and
Chilik Wells; b-- probebility curves of the occurrfnce of noise
of the given or lower amplitude at depths of 1-- 850 metera,
2-- 750 metere, 3-- 650 metere, 4-- 500 metera, S-- 450 m,
6-- 300 metere, 7-- 150 metere and 8-- SO meters in the
Alma-Ata upll. The dotted curves are the data on the Crapevine
Well (Texas) for a depth of 650 metere (the circle) and the
surface (croegea);
Key:
1. Alma-Ate
2. Chilik
3. X. nm
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c ` .

1i
0
0
A


Figure 8 (continued)
c apectra and spectral ratio at depths of 1-- 50, 2-- SSO,
3-- 950 meters for the Alma-Ata Well and 4-- surface,
S, 6-- 600 metera for the Chilik SJell.
Key:
1. f, hertz
2� Avell/Agurface
31
POR OFFICIAI. USE ONLY
~

TIM
K
1
,
~

~
~
+ 1
(

r
f ~
. {
~
T;
;
M
~
~
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A
The maximum noise umpli,tudea are oboerved in the lowrfrequency part of
the epectrum, and rhe dilferencee in levele on the eurface and at depth
are minimat hera. With nn increase in �raquency by approximately up to
1 hertz the noise level decreaees eharply. Ai frequeaci@e of more Chan
1 hertz, the decreaee becomea leaa eharp. On the day surface the noise
1eve1 decreaeee very little with lrequency, and e relative maximum of
ehe noise ie observed at a frequency of 2.5-3 hertz. At a depth of 600 m
the noise level.reaches valuee of 4-6 nm on a frequency of 6-7 hertz.
For the Chilik Wpll, the minimum ratio of the epectra at a depth of 600 m
and on the eurface ie 0.02 on frequencies of 3.5-4.5 hertz (Fig 8, c).
Lawa of Variatiun of Noise Background in Three We118. For the day serieg,
the background level in the Chilik Well ie gpproximately half the back-
ground level in the Alma-Ata We11 and four timee lese ehan the background
level in the Tsshkpnt We11. Let ue remember that the general background
level in the Taehkent We11 is gr8ater than in the Alma-Ata Well by
approximately two timea 121. Ae a depth of 900 metere, the noise amplitude
in ehe Alma-Ata Well ie 12-13 nm in the daytime and it is close taith reapect
to value to the noise level in the Taehkent We11 at night. The different
noise levels in the wells can be explained by the fact thaC the Taehkent
Well is in the center of the city, near lerge induetrial enterpriees and
other aources of noise, and the Aima-Ata Well is on the edge of the city
and ie comparatively remote from the baeic explicit eources of interference.
At a depth of 600 metere in t'hedaytime che noise amplitudee in the three
wells reach 10 (Chilik), 20 (Alma-Ata) and 40 nm (Tashkent).
The nature of variation of the background in the Chilik Kell for the day
aeries coincides with che variation of the day background in the other
tWO Wells.
At night the decrease in background in the Chilik Well is appreciably
weaker than in the Alma-Ata and the Taehkent Welle. Whereas for the last
tao We11s the ratio of the background on the eurface to the background at
a depth of 600 meters is 30-40, for Chilik it ie 4 to 6.
Some increaee in amplitude of the background on the surface in the frequency
band from 2 to 4 hertz ia observed for the Alma-Ata Well. It is poasible
to think that thia increase is eonnected with the "cultural" activity.
The nature of the peak in the apectrum of the aurface noise in Chilik at
3.7 hertz is atill unclear. Poseibly, it ie riused by a local eource
Which has ite effect only when recording on the eurface.
43. Background Stability at Different Depths
The noise stability hae important significance in eetimating the eensitivity.
The noise stability hae been apecially inveatigated. Stationary end aemi-
stationary obaervations have been aet up in tWO ae118 Alma-Ata Which
is characterized by a high level of ground noise, and Chilik, where the
ground noiee level is la+.
. 32
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ObnervnCinne in an Aren w3Ch High Gxound Noiee Level, The noise background
in the praeence oE ACnCionary obeervaeions 3r Che Aimn-Ata Well was
invuntignted aC depthA of 1950, 954, 700, 500 and 300 metera.
Noise Leve1 at a UepCh of 1950 metera. StaCionary observations at a depth
of 1950 meCers were performed in the firae phase of ehe operation, and they
were recorded by the aeismograph without a borehole preamplifier. Under
theae conditions the baaic source of the noise limiting the uaeful aensitiv-
iry of the equipment wae elecGrical interference. The microseiemic oscilla-
tiona caused by atorms on Lake Ieayk-Kul' constiCuCe an except3on.
Electrlcal interference ie unetable with respect to intenaity and frequency,
and it varieg both during the courae of the day and on different days and
in different months. Frequently this type of interference ig asaociated
with one time nf day. Among thP electrical interference it is poseible to
isolate geveral types which are noCed during vsrious time periods. If we
do not coasider the individual pulses, then the low frequency intenee
irregular oscillatione with a frequency of 0.4-0.8 hertz were observed for
the longest titoe. For noise of this type a stricC time coordination is
characterietic. This type of noise appeara in the evening from 2100 hours
eo 0200 hours local time. Sometimes comparatively high frequency (2-4-
hertz) oecillationa are rucorded which form long arce on the seiamographs.
Observation experience hae demonetrated that the baeic electrical inter-
Eerence ia connected with leaka, Usually after atarCing the seisenograph
for the firat time the interference level is comparaeively low. However,
later leake appear in the linea and the intensity of the inducCions
increases aignificantly. The following law has been noCed. In the day-
time there is basically cennparatively weak and high-frequency noiae. In
the evening and at the bef;inning of night, the long-period noise predom-
inates. At night, as a rule, the noise atops, and thid time is character-
izpd by a comparatively qtiiet background.
Seismic interference has been investigated only in the perioda when the
electrical interference level was comparatively low, which has made it
possible to raiae the gain of the channel. However, it has noC been posai-
ble to determine the quantitative amplitude of the aeismic interference.
With respect tc+ nature of variation of the amplitude with depth which is
typical of the majority of wells (including in Tashkent), it ie posaible
to consider that the amplitudea of the background are included in the
range of valuea from 2 to S nm. Even at depths of about 2000 meters the
"cultural" noise is felt. In the daytime the interference background
usually is one or two times higher than at night. Thia increase in ampli-
tude of the day background is characteristic approximately for 65-70X of the
total observation time with the exception of the night hours and holidays
when the industry of the city is not operating and the noise level is the
same in the daytime and at night.
33
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Oue of the seiamic inCerference duri,ng obeervationa at a depth o� 1950 m,
- the mose inrsnse is the 3nterference caused by aeorme on Lake Iesyk-Ku1',
but the level of Chie inter�erence ie appreciably lower than on the day
surface. Frequently even intense etorm microae3sme recorded at the -
Talgar stae3on by the KSE channels (To1 hertx) and the Stai channale
(Tp-0.6 herrz) wieh a r-ecording amplitude of 5-10 nm'have not been noted
in the well or at a11, or were very weak although the uaeful aignals (the
earthquake recordinge) in thie case were comnensurate with respect to
intenaity (Fig 9, a). In these cases the eignal/noise raCio in the well
_ Curns ouG tu be almoet an order higher than at the Talgar etation. Thia
difference in interference amplitude is explained not only by the depth
of the observation point but obviously by the fact that at the Talgar
etation the frequency characterietice of the KSE channel and, especially,
the SKM channelo are eomewhat ehifted in the low-frequettcy direction
(Fig 9, c). The storms are obeerved on Lake Ieaqk-Kul' most frequently in
the winter when there can be 15 Co 16 atormy days per month.
Noise Level at a Depth of 950 Metera. At a depth of 950 meeera the
stationary obaervatione are performed with a well type preamplifier placed
directly in the seiamograph. This has made it poaeible aignificantly to
- reduce the noiae background of electrical origin. The electric inkerf erence
remains only in the form of individual, comparatively rare pulses. As a
result, the useful senaitivity is limited only to the aeiamtc interference,
the amplitudea of which amount to from 4 to 15 mn. However, for the greater
part of the recording time (75-80X) the valuea of the amplitudea are 7-14 run.
These daCa agree with the results of atudying the interferenee background
by the method of vertical profiling. At a depth of 950 meters the eff ect of
the vital activity of the city is felt to a higher degree than at a depth
of 1950 metera in the daytime the noiae background increasea by
approximately 2-2.5 times by comparieon with night, reaching valuea of
12-15 nm.
Noise Level at Depths of 700, 500, and 300 Metera. The increase id noise
amplitude with a decrease in depth in this interval is comparatively small.
The values of the minimum and maximum background amplitudea of depths of
700y 560 and 300 metera amount to 5-20, 6-30 and 7-50 nm respectively, but in
the greater part of the recording time theae intervals are appreciably leas
broad.
The changes in the noise with depth in the range of 950-300 metera were
_ estimated by the variation in amplitude of the atorm microseisms of
Issyk-Kul'. For this purpose, the amplitude ratio of the microaeiams was
determined at each depth on the SKM channel located in a drift and acting
both as the standard and as the well channel. The magnitude of this ratio
varies within the limits of 3 to 5, that is, no clear dependence of the
ratio on depth was obaerved in a range of 950--300 meters. An example of
recording the storm microseisma in the well at a depth of 700 metera and
on the S(QK channel in the drift is preaented in rig 9, b. On the SIQH
_ channet the useful signal cannot be isolated against the noise background
in general. A comparison of the recordings of the storm microseiams at
depths of 700 and 1950 m indicates that their level has increased aignificantly
at 700 meters.
34
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a
b
i
VON (1) '
c
. .
0,4 O,i ~(0 r r si,i ~Ot;ra ~Z>
Figure 9. Recordings of storni microseisms and distant earth-
quakes at the Talgar station (SKM channel, upper
recordinga) and in the Alma-Ata borehole at depths
of 1950 meters (a) and 700 meters (b);
c-- frequency characteristics of the equipment:
1-- well channel, 1969 (H-1950 m), 2-- the same,
1971 (H-960 m), 3-- KSE channel of the Talgar station,
1969, 4-- the same, 1911, 5-- SKM channel of the
Talgar station
Key: 1. Vrem; 2� f, hertz; 3. 10 seconds; 4. 12 June 1969; 5. 0448 hours;
6. 0512 hours
:35..
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- Observatinns in an Axpa wl,th toi Crnund Noiae Level. The low noiae 1eve1
in elie vieinity of Chilik hea tmde ie poggible tn pprform dynchrenoue
obgcrvntiona uging identicel equipment in the wel1 Qt depthe of 606 and
300 meters and on the surEace. Unfortunacely, the resuleo of rtudying the
noiap in time do not ciaim to high eccuracy. Thie in explginad by thp
fact thgt the recording of loa amplitudes depends stroagiy nn thp ciamping
of ehe pen. dbnervation experipnce indicatee ehae quantitative procenning
in meaningful fnr amplitudee pxceeding 2.5�3 nm, and the escimaces obeained
for the veriation of the noise level arp, in our npinion, of defined
ineeregt.
brpth of 300 rieters. The total racording time at a depth af 300 mpcers
wae 50 dayg. During this time the noise levpi varied aith reeppct to
amplltude from 6 to SO nm. The noise amplitude disCribution vith reepeee
, to the recording time ie illuatrated beirn+s
A, nm 4.0 8.3 12.5 17.0 33.0
t, X 1.0 40.4 5.5 52.7 0.5
Thus, during 98% of the total recording time the noise level at a depth
of 300 meter8 aas included in the range of amplitudee from 8 to 17 nm,
and it varied by no more than 2 timea.
Depth 600 Mete,rs. iihen making the tranbition from a depth of 300 to 600 m
the noise amplitudes decrease by approximately 2 timee. Thp aaiplitudes
and the range of their variationa (see Fig 8, a) agree qualitatively aith
the vertical profiling data. At bnth depths (300 and 600 m) a atable
difference in noise level ie observed between night and day. At night time
(from 2100 houra�to 0600 houre local time) the noise level decreases by
almost 2 times, vhich confirma the "cultural" nature of the noise. On
holidays (Saturday and Sunday) the noise level in the Chilik Wall, in
contrast to Tashkent and Alma-Ata, does not decrease, ahich is obvioualy
connected with the absence of induatrial enterprises in the vicinity vhich
are the basic sources of interference.
The noise level on the day surface varies vith time Within significantly
greater limits than in the well from 15 to 500 nm, that i8, by more
thpn 30 timee. Since the obaervations Were performed during the quieteat
summer months, it ie possible to consider that this range aill increase
significnntly in the fall and winter as a result of aind interference which
is not recordcd in general at a depth of 300 and 600 meterg.
For illustration of the variation of the noise level from the day surface
and in the well let us pr.esent several aeiemograms. Nith equal cha-nnel
gains (k�2) the ground noise level is appreciably greater than at a depth
of 300 meters, but on increasing the ground channel, it ie half chat in
the well (k�1), the noise amplitudes are comparable (Fig 10, a, see the
insert). At a depth of 600 meters (Fig 10, b) f4r k=2 the noise level is
comparable to the ground channel the upper part of the seisnwgram
36
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PdP. oFFictati'UsE o
- ~ ^ � ' - - ~ 7~ . '

~ , ~s~ ~ t~. -~�s:"-^"---~------ ~Z't,F�;,.,~~^~'
tr!k+ll t
.'.....a.. ,Li-*'y^t~
. ~ i ,l i ..i~..~ . ~ ~a ~ ~~r
%tiA
~'.._?.~.�w~ ray~,'S'.f:r'.',t.i_L'~~~'r'j~�,i=_ ..,.�:++�..�.i4~~.-~� ~Y~i`s~:�r~~-,..~..
.~C"~~.w�~...'x...t,..+'"':~'> ~2:~�."'..~'~'i"..i.,.~'Y~~...,~`~.- .
_ : ~ ---~-.~....r....
~11~~ lul~it~ ~~i t ~'*`t~~_t~' ~''='a`-T,,,V,'..'.....~-""`_~''!~
. . ~ o _
.r,~ - ' - - -
"'~tlllhlm~ ~-t= ~ _
K~ - - -
~L~~:: i�}~. i'; �j`~~ S~Xy 1!~i ~.~~',~.,.`~.aaiG7~ Y~ ~xt~ ,,,t,.~~.~.~ =".~`1 w.�'
~Ny~Zy-i~~1~`F~:++ ~'y=~Ri~r,~~.. ,t�:~l'"-:�~
- - ~
. . . + ~ .
, ~ . - .
,
.
t . ~ .
~ w�~ .w ~
. . ~ ' �~~~r 1rA (4) .
?0~07'"S6f ~ 27. p,p 71A
N�60I~
~ 9n .
T
?3h J7ml~ 't
. 1~
ys blN
� ~ilMA~w.
/ . .
t . . . ,
~
~'~""'ri""' �
� . . : . + .

~06 ~ . .vM .1 N.�
1V w � ~ ~ ~\w~~4< ~ ti ti
t='~~~-"'~�-.,~ ~j"W"~IY'kyr~'~4t~r.st'r. , ~ 'I~~~~it
. . . ~~~~~'.x~Y.t
~ ~VI: ^r+ ~f�~u 'yF~ 1� ~.y ~'11~ r1, r'1~ ~VAN wa'
`~-~S ~w �M~.Mr ~w
` 'i ~w ~L~~'~: ` ; M' ~4' �r.~"i+~:.
#L �t'J J
~1.. ~ ~ ~ 'f~ ~~~.,tr/; ._'f 1~� `~1
. . . . . . .
_ . � ~g '
..r.
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Figure 10. [aQe preceding page] Noi,ee backgzound on the day gurface
and in the Chilik Neii at depeha of 300 (a) and 600 metere (b).
Keys
1. 4 August 1971
2. 0500 hourg and 39 seconde
3. 2317 hour# and 7 gerondg
4. 27 Juiy 1971
S. 2007 hours and 56 epconde
~ � lJ.d.6lt.~1~ ~
(2)
~is~rr
(4)
� j - . ' - '
.
~ = � ~ x . r _
i~ =
~ . r~1� r~�  � ~

a.
Figure 11. Recordings of earthquakes by the ground atation
(1) end deep-well atation at a depth of 1950 metere
(2) in the city of Alaa-Ata and the KSE channel (3)
of the Talger atetion. The errovs indicate the -
errival of the P and S aavea.
Key�
.1. 15 February 1969; 2. 1357 houra; 3. 23 July 1968; 4. 2012 hours
39
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FoR o"ictat, vsB oNt.Y
A�, (1) t
.
d

. ~
, . a

~a �~Ni~~~~~~
w
�
r~
a
~~a~a~� � ~~rr

~i
j
� ~
�J
/
j
l
~
V
:
~r~ �M L~r~� ~M~� ~~~~~~~Y~~~~~
~ ~
19, El
~lt~ 10 .+m ~0 .~Pf fy t~y�t (3)
Figure 12. Amplitudes and periods of near (a, b) and distant
(c) earthquake� by the deep etation (1950 meters)
and the Telgar station (ICSE chanael, drift,
June-July 1969)
Hiatograms of the valueg of Tp and TS in the vell and the drift
are aleo presented. The figuree at the points oa the graphs are
the number of coinciding valuea.
Key:
1. (Adrift/Awell)P. S 6. TD~~il)
2' (Tdrift/Taell)sp,g 7� T~p�S(vell)
3. tS-Po sec
8. Well
4. Tp.S(drift)' aec 9� TSt eec
5. Tp(drift)' sec 10. TPt eec
40
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. ~
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b
- C4 )
c
~
~ ~r ,t~ t/ r,,.,,�f (s~
t
1
v
/

lti~' ~ (7)
AL
(8) (4) ~ .
.
AV n r_~+ 8 j ~x
ii
l~ M
.
4i 10 rj 41 .fi lo~ ~ v 4f tr i/ T~, t
Figure 12 (End) [see key, preceding page)
41
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but ehen the noise ievpi on the aurfane in shnrpty amplified, and the
signni (2317 houre) en the ground aoiemogram became typical. At the same
time, at a 8ppth of 600 m+atexs no increaee ia noiee oacurrad, and ehe
nigflals were reliably epparated during the entire rQCOrding time.
Thus, for obeervations in aella not only doed the noise ieve1 dacreaee,
but ite stability in~:rea0ee sharply.
54. Uspful 5igna1 acid Seneitivity of We11 4beervatinng
The etudy of the ugeful signal in the we118 aae made in areas aith high
ground noiee level (Alma-Ata) end loa ground noiee level (Chi13k). In
order td egtimate the gain in eeeeitivity the obeervation materi8ls in the
' alma-Ata We11 vere compared with the recordings of the tao ground etatione,
' one of ahich (Alma-Ata) vae located within the city vith high ground noiae
~ 1pvp1, and the other (Talger), under f8vorable seimgeological conditione
aith low noiee level. The beismometere of the eecond station vere plared
in a deep drift [mine tunnpl].
Obeervationa under High Cround Noiee Level Conditions. Stationary obaerva-
tiong in the Alma-Ata Well were performed at different fixed depthe.
Uepth 1950 Meters. A comparieon of the obaervation materials of the vell
station with the ground station in Alma-Are demonatrated ttut the eeneitiv-
ity of the latter is 20 to 40 timee loaer. The recocdinge nf these gtations
are in praccice incompargble. Earthquakee (dietant (ir near) vhich are
isolated on the seigmngrams of the deep-We11 station either are not
recorded At all by the ground station equipped aith xtandard equipment or
they have a very loa amplitude (Fig 11, aee the inaert).
It is expedient to carry out the comparieon with the Talgar ground station
sepgrgtely by the recordinga of digtant (tS_P>1 minu be) and near (tSp]0 seconds) is approximately
6-8 timeq higher in the well than for Rround observations (Fig 219 b),
For distant earthqual:ea the gain in sensitiviCy of the well channel is
less than for near and locnl earthquakes, and it is 5-6 timea (Fig 21, c).
The 3Cfl3iCiVii} of the well channel when recording induatrial explosions
in the Atedeo (Fig 21, i) is,approximately tiie same as when recording near
earthquakes, thnt is. 6 to A times higher than the ground channel.
Thuw, iti spite of the high interference level caused by :!:e operation of
the combines, the sensitivity of the well observations in Novo-Alekseyevka
is essentially 1iigher thnn the ground observations botii in recordirig earth-
- qunkes and when recording industrial explosions.
.ib. Observations in 5hallow Wells Openinp, Up che Crystalline Basement
9'hc investiRated results indicate that under the conditions of great thick-
ne.ss of the sedimentary series, for a significan[ increase in useful
3et1giCiVity i[ is neceasary to b u ry the seismometers to significant
clepths.
It was possible to expect significantly bet[er results when submerging
seismographs in the wells opening up the crystalline bnsement at shallow
depcfis. In ordcr to estimate the gain in sensitivi[y for the well observa-
ti(ms tmder such conditions on the Ukrainian shield, studies were made
in shallow wells (several tens of ineters) opening up the crystalline base-
ment. Ttie observations were made in three wells located at distances of
about 20-25 km from each other.
67
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InasmuCh aa the rpgulCs of the obeervaeiong 3n gll of the wellg are
analdgdug,,we shall limie nurgelveB to e deacription of the resulee in
one of thpm 1ocaeed several kilometers from the rayon center nnd disCin-
guished by the highest leve1 of ground noise. The depth of the ae11 is
86 metere. The thiCkneas d� the epdimente repreeenCed by alluvium of
the Neogenic age (gand, clay, loam) is 54 meCers. From 54 tn 71 metere
ig wentihered granite, below 71 meters to the bnttom ig fresh, hard, massive,
fine-grgined granirp in which Che SBU^V deep-well seiemumeter was installed.
The ground seismometer was installpd in the alluvium directly at the head
of the well.
T'he gtudy nf the lnws of variarion of noi,ee with time nnd the ueeful nig-
nn1 wgs perfnrmpd by the semistationary dbservaCiona in the frequency
rnnge of 1-5 hcrtz. In order to obtain average statistical estimates of
the noige gt different times (the hours of the day, days, weeke), brief
recording sessions were held with large increasea of the equipment wi.th
8 pa8g bnnd of 1-20 hertz.
Noise 5ources. For observations in n well, the primary noiae source is
the crushers of several rocY, cruahing planr.a located approximately 4 km
- to the northeast of the well. tf we do not conaider the lunch breaks and
short-term preventive maintenance ghutdowns, the cruahers operate contin-
uously, in the steady state mode. The noise level is determined by the
_ number of rock cruahing planta operating simultnneously. Another source
. of interEerEnce is the industrial explosions in the open pit mines, but
they are very short-lived, they are produced in the majority of cases at
one and the same time (usually about 1800 hours local time), they are
easily recognized on the recordings and do not limit the senaitivity of
the observntions.
On the day surface the basic aourcea of interference are transportation
(automobilea, tractors, and so on), farm machinery operating in the
surrounding fielde and various machinery in the lumbering section in direct
proximity to the well (beginning with 200 meters and more). The rayon
center locxted at 6 km and several villages near the well ure also sources
of notse. In addition, interference can be connected with the regervoirs
located 200 meters from the well and the dam over which the water is
disc}iarged into the river flowing out of it.
Observation bata. The semistationary observations were performed in
April 1976. The amplification oE the Rround channel was given depending
on the noise level, 16,540 or 33,000, and the well channel, 140,000 or
280.000. The stabili[y of the equinment was controlled by sys[ematic
recording of the calibration siRnal. An example of seismograms from*a
visible recording is shaom in Fig 22, a. By the seismogram obtained in the
daytime (from 0900 to 2100 hours locnl time) it is obvious that on the
ground channel with amplification of 16,500, the recording was brokpn by
transport noiae with an amplitude of 25-30 rmn. At the same [ime at a depth
of 86 meters, with chAnnel ampllfication of 140,0()0, the amplitude of the
hackground noise does not exceed 1 mm, At night (from 2100 hours in the
68
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b
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~"'~Il~~'iid~Jl~fp~~'~~'~~I~~~~N~~'ar~ri~'li`lUl(~~~I~~~~i
Cigure 22. Seismogram of the noise and a distant earthquake recorded
by the welt and ground channels during semistationary recordings (a)
and photooscillogrAms of the noise with high amplification (b).
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evening to 0900 hour8 in ehe maxnirig leca1 time) the trAnaport noise makep
up 5n9; of the tatal obnetwat3,on time.
Uuring rnntinudus obaervatinna, the we11 ehannpl wae uaed to recoxd more
thnn 70 diffprent nignAle, including 15 d3etant parthquakee, but of the
SS nrnr signa1s the majdrity ere indueerial explosions from varioue
diaeancen. The grnund channel Wgg ueed ta reeord d tntal of nbout 20
gignnla, and of them none wae a digeant earthquake. This ig explained by
ingufficient sengitivity o# the ground obaervations 13mited by the high
intrrferenre lpvel.
`Che higfily aeflsicivp recarding of noige wae earried out i,n three minute
gepginng evpry 2 hours for 4 dAye ('Thursday, Friday# Saturdity and Sunday)
trnni 15 to 18 Apri1 1976. ExamplQe of eeiemograme are shown in Fig 229 b.
'Che neiqmegrnm at 1430 houra wAe obtained in the dayt3me, and at 0200 hours
at night, but the baeic interference in both cases wae the noise of the
crushprq recorded both by the well and by the ground channels. The noiae
Erom mntnr vehtcles was a18o auperimposed on the ground chennel recording
of the seismogram at 1430 houre, The seiamogram at 0203 houre i�uatraCes
noise under conditions wherh not all of the crushere of the rock cruehing
plants were in operation, and the seiemogrem at 1558 houre, When all oE the
crushcra were not in operation. On the recordings of the well channel, the
low-frequency interference ie quite vigible with a period oE about 3.5 sec
which is hardly neticeable on the ground channel rerordings in connection
Witli the gmall realized amplification~artd the high amplitude of the high-
frequency noise of the motor vehicles and the crushers.
_ Observation Results. Analysis of the materials showa that in the wella
three noise levels are observed which differ signiEicantly with respect to
amplitude and duration. The higheat level with displacement amplitudea of
. .tibout 10 nm occupies about 70% of the total observation time and ig
determined by the operation oE the cruehers of the rock crushing planta.
Tlie frequency of this interference is about 4 hertz.
The mintmum interfcrence level with diaplacement amplitudea of about 2.5 nm
occupies a total of 10% of the time ouc of the total duration of the
observationq, ancl it is tied to the periods whett the crushers of the
rock crushing plants are not in operation. The intermediate noiae level
oC about S nm is obviously associated with times when part of the crushers
are oper,7ting. Flith respect to duration, [his level takes up about 20% of
thc [otal observation time. The minimum background level corresponds pre-
dominantly to the period brtween 0200 and 0600 hours nt niglit locnl time,
occupyirig short intervals of 1-1.5 hours. The noise level of 5 rtm is
observecl hnsically from 1600-1700 to 2100-2200 hours in intervals lasting
1-2 to 4-5 hours.
The st.ltistical processing of the data was carried out to estimate the
nai.se Crom the various sources. The avernge noise level from the rock
r.rushing plants in the well is 6 nm (line 2 on Fig 23, a), it is constant
and does not depend on the time of day. The transport noise (region 3
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In F1g 23, a) daep nOt pxr.eed the plant ndipe with respeer rn level, ChnC
is, it -lg no more ehan h nm. 'Chey are observed on reearding only in the
Cane whr.re the eruahera are nnt in eperaeinn nnd the mntor tranaporeaeion
mavaa direcely nt the head nf the wpil (10r20 meters), When motor trana-
pnrtaeidn moven ae digtancpa closer than 20 meCern from the head, the
noisc frum it in noe igelated on the we11 channei reanrding.
In the we11 1ow-frequency nniae ia alqo reeorded with a period of about
3-4 geconds, the arithmetic mean levei of wh3ch fluctuates around a value
of 300 nm. During the observdtions in the well, the low-frequency inter-
ferenr.e was eoneinuougly obgprved. Tho interferenre 1evpl in Fig 23, a
ig prdvigidnally illustrated without a time arale. InngmuCh ag thia
noise fn ouCgidp the page bnnd di the equipmene, ite.amplitude doeg noe
exr.eed 2 mm on the reCOrding.
nn tlie day 3urfnce nt the head of the well, the noisp level reachps 2000 nm
_ (regton 3 on Fig 23, a), nnd it 3a determined bagirAlly by the transport
tnterEerence. With regpect td time it occupies 759; of the daytime recnrd-
iny;, attcnuating only at night, The transpdrt noise level on the gurface
ciepenctn on the distance ut which the moving transportation ie located, and
to a tesser degree on its form (nass). For example, during movement of
n motor trangport at a distance of about 150-200 metprs from the obaerva-
tion pnint the noige level reaehea 400-600 nm, and with a decrease in
distance to 15-20 m, this value increaseg to 2000 nm or more, that is,
300 times higher than in the well. In t}ie abaence of transport interference,
the noise amplitude on the surface reaches 50 nm in the daytime and 30 nm
at night (line 1 on Fig 23, a). The decrease in noise at night indicatea
Chat some part of the [otal noise level is determined by the "cultural"
noise connected with the vital activity of nearby populated places. On
the surface, just as in the well, a low-frequency interference is recorded
with a period of 3-4 characteristic in general for the given area. The
- interference levei on the surface is somewhat greater than in the well,
and it reaches about 400 nm (region 4 on Fiq 23, a).
As n result of the statis[ical processing of the data for the surface and
the well, curves wcre constructed for the probability oE occurrence of
noise oE the given or lowcr amplitude (Fig 23, b). In the absence of
transport intcrferencc tlie noise in the well is determined by the crushers
(curve 1), the menn amplitude of the noise with respect to SOX probability
level is 6 nm; the noise amplitude varies from 2.5-3 to 12 nm. On the
surCare under annlogous conditions the noise reaches values of 45 nm
(curve 2). The variation of the noise amplitudes on the surface is 15-90 nm.
1n the case wliere only part oE the criishers are in oreration, the probabil-
ity curves are shifted in the direction of smaller vAlues of the noise
amplitude (for example, curve 3 for the well and 4 for the surface). When
the crtishrrs are not in operation, the averaqe noise level in the well is
1.5 nm, varving within the limits of 0.7-4 nm (curve 5 in Fig 23, b). In
this case on the snrfare (curve 6) the amplitude varies from 8-10 to 50 nm,
and the mean valuc is 25 nm.
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,C, *+a~ " ~ � ~
!IO
iG
-
-
J
7
/O
!0
y0
t0
e
!04
!0
~
1
!,0
i
~
1
QJ0,1 0,1~Q6� 1,0 t ~ i~~~ .
- � ~1~
Cigure 23. Characteristica of noise during observationa in a
shailow well openinR up the basement.
n noiae level in the daytime And at night on the day aurface
and a depth of 36 meters; 1-- noise level on the surface without
cnnsidering trnnsnort interEerence, 2-- the same in the well,
3-- transport iioise on the stirface and in the well. 4-- low-
frequency noise on the surface. S-- the same in the well;
b-- probnbility curves for the occurrence of noise of given or
lower amplitude at a depth of 86 m(1,3,5) and on t}ie surface
(2,4,6,7) under various condicions;
c-- average noiae spectrum at a depth of 86 meters.
Key: 1. X, nm; 2. day; 3. night; 4. hertz
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Fdr abservacions on the sur�ace 35% of the time Ie characterixed by the
prpsence of trnnsnnrt i,nCerferancp. Curve 7(Fig 23t b) i,s conetructed
in lccordance with the noi,ge recording i,n the prpsence e� transpoxtaCi,on
mnving nt n dieeance of aboue 200 meters Exom the nhservntion point. A
lnrkc rnnpE oE vnriation of the nnise amplitudua (�rom 30 ro 500 nm) is
charnCterigtic, and the mpnn value w3th reapect to the SOX probgb3,lity
lpvel is 150-170 nm.
The specCrgl analysis of the noige in the well at a depth of 86 meters
indicgCes thae the maximum amplitudes correspond to the 1owMfreqvency
part nf the specCrum (Fig 23,c), With an increase in the frequency, the
nniae level derreases sharply. For example, with an increase 3n frequency
from 0.2 to 0.8 hertx the noise level decreases by more than two ordere,
With further increase in frequency, the noise ampllCudes decrease sisnif-
icuntly more slowly. In the 3-4 hprtz range, the relative maximum connected
with the operetion of the crushers is observed. The nature of decrease in
the naise with increase in frequency in the 0.2-1 hprtz range wi11 permit
us tn propoae that the basic mode of the Rayleigh wave predominates here.
Sensttivity of Well Observations, In connection with the presence of a
high level of ground noiae the recording on the surface under the condition
oC rrcording on the aeismonram of normal bacr.ground with an ampl3,tude of
morc than 1-2 mm is realizable only for amplificationa not exceedi.ng
500-1000. Inasmuch as the high level of ground interference is characteris-
tic far 75% of the observation time, the atationary high-frequency observa-
tions are in practice impossible.
The sensitivity of the well obaervations is more than 2 orders higher than
that of the ground observationa. Distant earthquakes considered as uaeful
signals which are clearly recorded by the well channel are not separated
in the ground channel under these conditions.
In the abflence of transport interference (about 25% of the total observation
time) the sensitivity of the well channel is approximately 5-6 tiries
higher than the ground channel. For example, if the earthquake at 1730
hours (see Fig 22, a) is recorded by the well channel with an amplitude
which exceeds by 10 times the background level, the araplitude of the signat
on the ground channel recording will only exceed the background level by
a s 1 igh t nmount.
A comp:irison witfi the ground seismic atation, the seismometers of which are
inst.zlled on outcrops af bedrock approximately 10 km from the well indicates
ttint the sensitivity of the two atations is comparable (Fig 24). The
higlier low-frequency noise (T-3-4 seconds) on the ground station is
explained by the fAct that the natural period of its seismometers is
1.5 seconds (the natural period of the well seismometer is 1 second).
Let us Identify the results of the well research.
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Fnr d high level of ground noise
1. Under the condiCiona of the large i,nduatxial ci,ti,ea the noise level on
ehe day surface ie very high and ungtable, The range of variaCion of the
nninp amniitudes:with time exceede 2 orders. Howeverp approximately to
300-400 metprs thp noiae 1eve1 ie etabilized and beeically varies from
dey Cd night by 2-3 timee.
2. The sharpesr variaeion of the backgxound takes place in the upper part
o[ the Hectinn (the Eirst hundreds of inetere). With lurther increaee in
depth the gradfent of the amplitude variation o.f the noise decreases rapidly. ~
Thus, whereas on going from the day aurfgce to a depth of 600 meters the
noise amplitudea decrease by 30-40 timesg on making the transition from
1000 to 2000 meters the noise amplitude decreases by a total of 2-3 timea.
3. The maximum noise ampl3tudes both on the day aurface and at great depthe
correspond to the low-period components of the apectrum. With an increase
in frequency the noise level decreasea aignificantly faster in the well
than on the day surface. `
4. The recordings of the ground and deep-well atations located in Alma-Ata
are in practice not comparable. The earthquakes, the recordings of which
are readable at the deep atationa are not recorded by the ground station
and, vice versa, the earthquakes recorded by the ground station are com^
pletely washed out on the recording by the deep station,
A compartson of the recordinQs of earthqusi:es obtained under city conditions
in a well at a depth of 2 km with the recordings of the Talgar station
located far from the city in a drift in crystalline rock indicatea approx-
imntely identical useful sensitivity of the etationa.
5. The results obtained make it poasible to recocunend the creation of
highly sensitive stations with seismographs buried in deep wella to study
the setsmic characteristics of large cities located in seismically active
zones.
F'or a low ground noise level
1. Ttie noise amplitudes decreage with depth significantly less sharply
than in areas witti a high noise level. The nature of variation in the
Chilik IJell for the day series coincides with the variation of the day
noise in the Tashkent and AIma-A[a Wells. At night the noise level in
the Chilik Well decreases significantly more weakly than in the daytime.
Wherels �or the TAShkent and A1ma-Ata Wells the ratio of the noise level
-it th(
- surface and at n depth of 600 meters is 30-40, for the Chilik Well
it i4 4-h.
2. On tlic- dny stirEnce the noise amplitudes can vary by several tens of
tlmes witli time. At a depth of several hundreds of ineters (300-600 meters)
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L-
tlir iiriiNv lrvrl vrtrl.ra, nA n ruir, hy nn morc+ ehrtn 2-3 Cimrs. Theer
clll'I't-rvii(-eH iirc, ulrilily conni--r,Led wJ,tli nn 1,ncreaHe .tn nnige in the dayCimp.
'Che gnin in useful sengieiviCy is appreciably lower Chan in the areas wieh
n liigh level nf grnund noiee. Nowever the high stnbillry of the noise even
at shallnw depehs increases the effpctiveness and the value of the well
dbservariane shnrpiy.
VlJ2000
V-1B0000
(1) !l.1R W a. Mb rjm
N-ON
.._A.an._.._ .;,...nA li , _
. U .
B6~
V�16J00
OM
Figure 24. Recordings of a distant earthquake by the well and
ground stations, the seismographs of which are
installed on outcrops of bedrock (upper trace)
and on sedimentary rock at the head of the weZl
(lower trace)
Key:
1. 11 April 1976
3. In tlie well the shape of the recording of each individual wave is
determined primarily by the superposition of the pulses of the incident
wave and the wave reflected Erom the day surface. In the section of the
well ad;3.lcent to the dAy surface, the shape of the recording of the
tnd[vidtinl wave can be more complex than on the day surface. The length
of tliis section depends on the shape of the pulse of the incident wave,
i[s predominant frequency and the high speed section. At depths where the
pulses of the incident and reflected wavea are resolved, the shape of the
individual wave is newly simplified, but in this case the number of waves
recorded on the seismogram increases, and the atructure of the seismogram
becomes significantly more complicated.
Por noisc Erom stationary sources
1. Uncler the conditions of the effect of stationary noise sources their
level at the surface can be very high. Nowever, the range of variation
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ciC nmplltuclaA wl.th timc� ip nppxQCinbly
'1'huH, whcreas i.n Alm1-ACa And Tashkent
orders, in Novo-Alel(3eyevka it ie less
lnwer thun �zom the etandaxd sourcea.
the ranga of variation exceeds two
than an order (7 timea).
2. 'I'here are two "noise" conditiona �or atationary eourcea differing
Htinrply between eacti oCher with respect to level and nature of variation
nf the noise "quiet" and "noisy." The former is characterized by a
low noise level and a monotonic decrease in naise with depth. For the
latter, a aharp decrease in ampliCude in the upper part of the section
(400-500 meters) and smooth increase in amplitudes with furrher increase
_ in depth are characterieCic. Thia decrease in noiae indicatea various
typag of waves predominant at different dapths; in the upper part the
surface waves predominate, and deeper than 500 meeers the volumetric waves
predominAte.
The higher frequencies decrease more aharply �rom Che surface to a depth
oE 500 metcra. Below 500 mptera the total increase in noise amplitudes
with depth takes place primarily as a result of the 5.1 and especially
the 2.6 hertz components.
4. The gain in useful senaitivity for well observations in Novo-A,lekseyevka
when recording at a depth o� 1200 meters for local e.lrthquakea is 8�,10,
for nearby earthquakes 6-8, and diatant earthquakes 5-6 and industrial
explosiona, 6-8 times.
With respect ta useful sensitivity the ;Jovo-Alekseyevakaya atation is
comparable with the other well stations of the test nrea (Alma-Ata, Ali).
For shallow wells which open up the crystalline basement
1. Even under conditions of high ground noise level, completely excluding
the possibility of high frequency ground observations, submersion of the
seismograoh in a well to the crystalline basement permits amplification of
about 300,000, that is, tt makes it possible to obtain the sensitivity
w}iicfi is commensurate with the useful aensitivity of the station located
on the day surface directly on outcropa of bedrock under unfavorable con-
d[rtons.
2. The gain in sensitivity obtained is connected primarily with the
transition to the crystalline basement. It is possihle to assume that
ttiis gain depends little on the thickness of the sedimentary series and
will be ohserved in ather regions of analogous structure.
3. Considering the high velocity gradient in the upper weathered zone of
the basement, it is expedient to bury the seismog,raph 10,45 meters
into stronger rock.
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PART II. RADIOTELF.METRIC RECORDING
The centralized radiotelemetric recording with a unit time service permitting
the accuracy of the constructions to be increased is one of the basic
Features of the developed procedure. A more detailed description is pre-
sented of the Alma-Ata radiotelemetric teat area and the equipment of the
nutomated well and ground stations and also the radiotelemetric recording
system. 5pecial attention has been given to a description of the experiment
and the observation results.
CHAPTI3R III. ALMA-ATA SEISMQLOGICAL RADIOTELQ4ETRIC TEST AREA
The observation conditions.in the vicinity of Alma-Ata are characterized
by the presence of a very high level of seismic noise caused by thP vital
, activity of the city and its h igh variability in time.
At the same time the seismogeological situation near Alma-Ata which is
located in a force-10 zone requires a detailed study of the seismic char-
acteristics of both the city itself and its environs. The necessity for
highly sensitive observations arises also from the fact that at the present
= time the basic characteristic of the seismic regime is "calmness" of seismic
activity. In order to discover and trace the'seismically active zones it
is necessary to increase the accuracy of determining the coordinates of the
earthquake centers.
Thus, the basic specific requirements on the observations in large indus--
trial centers are, first of all, high sensitivity of the equipment and,
sec:ondly, high accuracy of determining the coordinates of the earthquake
_ centers. The satisfaction of these requirements has led, on the onL hand,
to the creation of highly sensitive deep-well seismic stations and, on the
other hand, to the organization of centralized multichannel radiotelemetric
recording of the signals of all stationary observation points. Both of
these areas were basic to the creation of the Alma-Ata test area.
51. Ceological-Geophysical Characteristics of the Region
In adminlstrative respect4, the observation region belongs to Alma-Ata
Oblast .znd includes tkie city of Alma--Ata directly,
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'C1to rekinn includeg areng rhat are differene wirh respeCt to their geu-
mnrphntogical appearanrr from plaing and mildly Main y nrenn in thp north
to the mountainaus nrp~n in the south. The Tltyskayis locgted in
 the noreh, it runs in a subintitudinal di.rectidn along the 2ailiygkiy
Alatau Ridge which is located in the eouthern pare and ia eppareted from
the Kyungey Ala-'Tno ttidge locaCpd farther eouth by the Chon-Kemin itiver
valley. In the wegt, the Zuiliygkiy Alatau is ep1iC into Cwo branches the Kastekakiy nnd the Chon-Keminakiy Ridgee. The highest a1C3tude nf the
7.ailtygkiy Alaeau reachpa 5000 mpters. Strong dismemberment of the ridgpg
is a characteristic fpaCure.
Tecronics. On the regional level the district is in an area of joining
nf the Caledonian atructures of Northern Tyan'-Shant with the Hercinian
strucCureg of the Dzhungaro-Balkhaeh Province which is complicated by
.hlpine discnntinuous tectonicg. The Kungeyskiy, Zailiyskiy attd Chu-Iliyakiy
anticlinoriya and Iliyskiy synclinorium are large structures.
1'he Kungeyskiy anticlinorium ie made up of inetamorphic aerieg of the
PrnterozoiC with inclusions of large masses of intruaions of Silurian and
Ordovic:ian age. In the north the anticlinorium joins the 7.afliyekiy
anticlinorium along the deep Chilik-Keminskiy fault of nncient occurrence.
in the core of the Zai:iyakiy anticlinorium, on a modern scetion Proterizoic
deposits are noted which are highly intensely dislocated and form smttll -
isoclinal folds. The lower Paleozoic series are repreaented by a system
of narrow folds of the sublatitudinal direction. Together with the
Proterozoic, Chey are the only LoWer Paleozoir structnral Ftate.
- ;he surfnce effusive-sedimentary series of the Devonian and Lower Carbanifer-
ous occur unconformably on the Caledonian folded base in the form of a
number of comparatively gently sloping synclinal folds, forming the 2siddle
Paleozoic structural stage.
In the north the Zailiyskiy anticlinorium borders with the Iliyskiy
synclinorium througr the Zailiyskiy zone of faults of aublatitudinal atrike
which is a structural element of the Upper Paleozoic stage. There are no
Devonian deposits liere, and the Carboniferous and Upper Paleozoic deposits
of basically effusive-tufogenic origin occur unconformably on the dislocated =
rncks of the Silurian, forming gently sloping brachysynclinal and anticlinal
folcis. The t;ently R1oPing bell-shaped poles are made up of Mesozolc forma-
ti.ons, and the Iliyskiy intermontane trough with a flat bottom and several
upliftrJ limbg is made uP of Cenozoic deposits which maintain almost un-
disturhed horiZOntal bedding or their depth corresponds to the slope of the
Pa1roz4ic hase.
In Quaternary time the most intense vertical displacements of the blocks
tocik place hoth with respect to the renewed ancient tectonic futures and
wit}i respect to the newly occurri.ig faults which has created a stepped
relicE system so characteristic of the region. The systems of deep faults
are illustrated in FiR 25, a.
1 [Ili River Bssin]
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GenphygiGal 5tudy. The fireC lnrge�~~itle seiemic eCudien in NorChern
Tynn'-Shan' nre cdnneceed wiCh the names nf G. A# Ggmburtsev,
K. I, Satpeyev and D. I. Knzanli. They were starCpd immediately efter
thc disnstroun AahkhAbad enrthquake, The firAe etudipe were made of the
deep aeruCture uf thr rrgion by the deep seismi.r. sounding Cechnique in
1949 (22, 241, and the basia wao laid dnwn for the reginnal network of
seismnlogical sCntions (Alma-Ata, IIi, Chilik, Kurmeney, Itybach'yes
przheval'sk, Krasnogorka, Naryn). Theee sCgtions made it poasible to
record parChquakes beginning with the eighth energy class.
itere, in the vicinity of A1ma-Ata in 1951 G. A. Gamburtsev began the firet
highly apnsitive observationa to study the weak local earthquakes in the
high-frequency renge (5-30 hertz) by the correlation method of studying
eartliquakes (h?tIZ) [20, 211. 2t ia nec:paeary to noCe that the npplication
of Chie meChod at the present time ie the basic Crend in the development
of seismnlogy.
buring the period from 1965 to 1967, in connection with the deaigning of a
number of hydroengineering etructures in the I1i, Charyn and Chilik River
basina, a aet of operationa were performed to gtudy the degree of seismic
danger of this region. In addiCion to the regional network of atations
in the Chilik and Charyn interfluve, a group of four eemporary etations
were organized which made it poasible to record weak ahocks and more pre- -
cisely to define the parametera of the earthquake centers.
Since 1966, the complex regional geophysical studies, including seismologi-
cal studies with the zemlya [earth] stations have been performed by the
Kazakh Geophysical Trust and the regional network of seiamic stations of
the Institute of f:eological Sciencea of the Kazakh SSR Academy of Sciences.
Nowever, these observations have insufficient detail to study the seismic
characteristics of the city of Alma-Ata and its environs.
Deep Structure. The earth's crust in this area is�characterized by sub-
ho:�izontal layering ,and it is separated into individual blocks by vertical
or 9tCLPlY dippinR fractures [3). The thickness of the earth's crust is
from 40 to 60 km. According to the geophysical data, the roofs of the base-
ment, the Conrad and *tohorovichich boundaries are isolated (see Fig 25, b).
The Cnnrnd surface is submerged from west to east to e depth from 20 to
35 km and it is characterized by a complex structure. It is cut by the
Kurtinskiy, Altyn-Emel'skiy, Kemin-Ushkonurskiy and the Chilik-Keminskiy
cieep Ernctures in the northeasterly direction coinciding with the strike
oE the structures of the Kungey-Zniliyskiy anticlinorium. The Kemin-
llghkonurskiy and Altyn-Emel'akiy faults are traced in the entire series of
the earch's crust to the ttohorovichich interface.
Tlie "hasaltic" layer hounded hy the Conrad and rtohorovichich surfaces
Iias a thickness from 20 to 35 km, increasing toward the. east in the
direction of the submersion of the Mohorovichich surface.
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~
~
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~t
~
.
o /
zr
caur~A',9N (2)
u. ' b
0, Bt A~ a s
- cJ~ do
(3) -1,401' K~~ I,S
~ 4
~ ~
~ nvA.o ~ yu po~AO~+
t
p p ~ yU 1~R�~
' 6
( 7 )~I,n~"',~"~ ~
8 ~',ry ~ON ~K I
~ a1/rOM =
MPCrATO

_
(7) p'`'�H
Op~Kctrc ~ ;
,
,
(10) geo AAaa-AmQ 1
(9)
ff :sis
Figure 25. Schematic of deep faults (a) and structural diagrams
(b) with respect to the basement roof (on the left),
the Conrad boundaxy (on the right), the
Mohorovichich surface (at the bottom) and accorcling to
the data oE [3J.
[See following page for legend and keyJ
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[Lepend gnd key to I'3g 25, precedi,ng pngp];
n: 1-- epiCentprs nE deerrucCive garehquakea in the paat, 2-- deep
fnults (I Yuzhno-rizhungarekiy, II MAlay.Sarayekiy,.xTx
Knskelenskiy, IV Altyn-Emellskiy, V-� KarukasCekekiy, VI
Raragayly-8ulukekiy, VIi ~�-Kemin-Uehkonurekiy~ VIII Aktyuzekiyt
IX Severo-Keminakiy, X~- Chilik-Kemkiekiy, XI Severo-Kungeyekiy,
XII Tyupskiy); 3-- active deep laults;
b: 1-- isohypaes nf the interfaces, 2-- deep faulte.
Key:
1. Alma-Ata
2. Lake Issyk-Kul'
3. A1tyn-Emel'gkiy fault
4. Kemin-Ushkonurekiy fault
5. Alma-Ata
6. Chilik-Keminskiy fault
7. Altyn-Eme1'skiy fau1t
8. Kemin-Ushkonurskiy fault
9. Alma-ACa
10. Chilik-Keminakiy fault
'l'he "granite" lnyer which includes the seriea bnunded by the roofs of the
1.ower pnleoznic basement and the Conrad surface has a thicknesa of 14-22 km.
Thc PIIlE'.07.03C basement is distinguiahed by a block structure and it ia cut
by a qeries of differently oriented tectonic fractures with amplitudes
reaching 500 metera. The depth of occurrence of the basement ie different
in different parts of the area. In the aouth and aoutheast the Paleozoic
formations emerge at the surface. The Paleozoic seriea in the north a.nd
northwest are also close to the aur�aceo In the central part the depth of
occurrence of the basement is maximal. The series of tectonic ulslocations
with a brectk in continuity deep fractures roofs of the Pd?,iozoic base-
ment in the vicinity of Alma-Ata are broken down into three blocks:
southern, central and northwestern. The southern block is a monaclinal
which dips steeply to the north to a depth of up to 3000 meters. The central
block is separated from the southern and northwestern blocks by faults
complicated by a series of small discontinuities of latitudinal and north-
easterly direction, and it is the most submerged. The thickness of the
sedimentary deposits here fluctuates from 2.5 to 3 km in the west and to
4 km in the center. The northwestern block is also se-par.ated from the
adjacenC fractures and is characterized by uniEorm (quiet) bulging of the
basement in the northwesterly direction.
According to the data of geophysical research, the nropagation rates of the
longitudinal waves in the earth's crust have the following values:
the sedimentary layer is 2500-2700 m/sec, the "granite" 12yer ia 5700-6600
m/sec, the "basaltic" layer is 660n.-7300 m/sec, the subcrustal layer
(the riohorovichich surface) has a velocity discontinuity to $100 m/aec.
The velocity an the surface of the Paleozoic basement does not depend on
the depth of its occurrence within the limits of accuracy of the determina-
ttans.
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Seiem3Ciey of Che itegi,an.1 A chnracCPxieeic gepeure of NorChern Tyun',Shan'
iq ehv fnr.e thnr f.n n qhorr i,nter.val four diaustrous earthquakes have
orr.urred hera; Vc+xnrnnkaye (1887, 11-7-7.25), Chil.ik (18A91 Mtl7.54)'
Kehi nqlcoyr. (19110 M-H. 7) and Kemi.no-Chuyekoye (1938, Ma6. 5) . D, Gutenberg
anaigned a mnximum possible magni.tude of 8.7 to the etirongese of them, the
Kebingkoye eArthquake. 5rronger enrthqugkes did noC nccur 1gCer, and rhe
seismiciey ig connected with the appearance of weak and roed-twn earChquakes.
For Che gren nonuni�o rni disCribut3an of the earthquake epicenCers is
characeeristic (see F'igureg 73, 74), The basic number of them is concen-
traCed in the central and easeern pares A separategroup o� earChquakes
is located in Che Chilik and Charyn interfluve in the epiceneral zone of
the 1889 earthquake. A clearcuC law is observed in the mutual arrangement
of the epicenters of the weak (K$10) and stronger (K5,11) earthquakes. The
stronger earthquakes are eystematically located at some diaCance from the
accumulations of epiCenters of earChquakes. They outline the zonea of
i.ncrra4ed nctivity formed hy Che weak earthquakes.
A characrerigcic fenture is the almost complete absence of earthquake
centers beyond the limits of the crust and coordination of the majority of
tliem with the "granite" Layer. The basic number of centers with K~9 have
a depth of 5-12 km; the earChquakea with Ks 0(23)
lttiretuA
rigure 26. Diagram of the arrangement of the deep-well (1),
- the ground surface (2) and portable automatic
stations of the Alma-Ata radiotelemetric teat area.
The black triangles are the atationa of the regional
network.
ICey:
l. Kurty 14. Ozero
2. Kapchaguyskoye Reservo:kr 15. Talgar
3. Kapchagay 16. Plato
4. Ili 17. Talgar
5. Kaskelen 18. Alma-Ata
6. Nikolayevka 19. Issyk
7. Ali 20. Novo-Al(2kseyevskaya
8. Dmitriyevka 21. Turgen
- 9. Chemolgan 22. Chilik
10. Burunday 23. Kurmenty
11. rabrichnaya
12. Kaskelen
13. Uzunagach
_ Let us note that when selecting the lc,cations of the stations, the can-
ciitions oE insurance of stab.le round the clock radio communications in
the ultrnshort wave range,and also the presence of stable electric power
lines for the system transmi,tters had decisive significance.
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(i)
(PI)
~
FOR OFFICIAL USE ONLY
,
,
(1) (z (6) p ro aa 6o eo
~ J/'00 -~-~-r~

v C
Io0
~
e
d
k
d
d
1 ~
�~00
'y
~

~
1100
.
~
Figure 27. Geological
-J00
�
t

lt00
~
sections (a) and tempera-
,
ture curves (b) with
~

~
respect to the Alma-Ata
�600

_1 _
t00
Q41
well (I) and the Novo-
Alekseyevskaya well (II).
~ f
-OD
7

ty00
06'
The provisional notation is
.
Z~c ~

7

as follows
' -t
� ~ e
~
1100
For a(II): 1-- shingle,
2 gravelites, 3 sand-

stones, 4 clay,
-AM
~y
'
1600
argillites, 5 silty
clay, aleurolites, 6
~

clay with sand admixture,
-~00o
b
i�,

1700
7-- clay, lime argillites,
8 carbonaceous-clay

deposits
- ~~oo
~
- =
zsov
Key :

1. grotip; 2. system;
=~ro~~
190D
3. depth; 4. lithologic
column; S. thickness, m;
6. depth; 7. Cenozoic;
F
lJ00
~

JCOO
8. Paleozoic' Pz �
'
9. Paleogene, Pg;
10. Neogene N; 11.
Quatertiary Q
-s.
9
- ~.t~0
. _
86
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Table 5
060- (3) KoopaxHeTU Paccro~N~ Moway araHUxaMr, w
(?raiwwA aNevr.
1 rro Z ~ A A,," I lt, ,i T' 0 A-A A I I-A K q
(5)
(6)
Tairap
03oP0
T
0
430 14,25 0 770 13.55'
43 04
2
1200 - - 27 20 40 17 110
li
(7)
Ama�ATe
A_A
,
8 7E3 89,28
43 17.23 78 58,56
2900 - 27 _ 24 35 41 108
800 L000, 20
2 4 - 31 23
0
(8)
AnM
Hoso-Anon
A
H
A
43 33.02 77 02.13
,
84
' 2000
'
550 800 40 88 31 - 25 72
1S
45
(9)
-
CNbCkIlA
-
49 23,86 ;7 13,84
. .
700 1200 17 4~ 23 25 - 68
36
(i~j
n;~~
n
43 53,6 7u zo
sso - iio ioa e4 72 ea _
'
'
ios
1700
_ i
r e ia as 3e ioa
.
(12)
I7pmwoaaHMe. A_ sucoTe pea ypooHCM Mcpry
ll - rity6iwa npN6ope s cKeemme.
Key:
1.
Station
7. Alma-Ata
2.
Notation
8. Ali
3.
Coordinates
9. Novo-Alekseyevskaya
4.
Diatance
between stationa, km
10. Kurty
5.
Talgar
11. Plato
6.
Ozero
12. Note. h ia
the
elevation above sea level, II depth of instr
ument
in the
well.
53. Radiotelemetric Channel
In 1971 the laboratory of deep well observations began work on the
development of the equipment and the process for centralized recording of
signals. In 1972 V. G. Katrenko took the radio channel in Tashl:ent as the
iniCial one. The development ended with the construction of the radio-
telemetric test area of highly sensitive sutomated stations in 1972.
Later the equipment was improved significantly and a great deal of experience
was nccumulated in its operation. Let us consider the individual assemblies
and units of equipment which are not seriea manufactured by industry.
For this purpose we shall use the materiuls of reference [37] in part.
The radiotelemetric channel includes the equipment at the transmitting and
receiving stations. The equipment makes it possible to input seismic
data ta the communications channel �or which the series radio relay RP.S-1M
stations ,zre used.
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Basic Cechnical specificationa ef radiotelemetric e
(withouC A cnmmunicaCiona ch8nnel) are aa followe;
Frequency bnnd of transmitted aeiemic daCa, herCz
Dynnmic range (withouC the commun3cationa channel),
decibels
Nonlinearity, Y
Operating temperature range, �C
Feed voltage (from storage battery), volts
quipment
0.5-10
60
AO. S
from -15 Co
+40
12
The functional diagram of the telemetric channel ia preaented in Fig 28, a.
The basic linkA of the channel are as followa; a aeismograph with pre-
amplifier, an amplifier-modulator, tranamiCter, receiving radio atation,
demodulntor, low-frequency amplifier and recording device.
The S13U-V seismometers are used as the seismic converters iift the deep-well
stationa, and the SM-2P1 at the ground surface ataCiona.
Amplifier-Modulator (UM). The Ut4 module (Fig 28, b) is made up of the
amplifier, modulator and feed voltage stubilizer. The low-.frequency
amplifier, to the input of which the seismic signal is fed after being
picked up on the preamplifier is a low-noise five-stage amplifier with
direct couplings between stations.' It is encompassed by two loops of
common negative feedback which rigidly stabilize its parameters and 3hape
the frequency characteristic. For compensation of the characteristic of
the pendulum conversion, the transmission coefficient of the UM in the
frequency range of 1-10 hertz is inversely proportional to the first power
of the frequency.
Basic parameters o� the amplifier;
Input impedance, kilohms 8.2
Output impedance, ohms
1
r-i
�
a

.
-i
+I
,
~
41

. . r-I cd o�
,
,
44
~
.
a~
~
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' itselF) piay the role of the controlling awitches. The multivibraCor
Crequenr.y dependa on the charge cuxrent developed tay the input circuits,
and ir is controlled by the output current of the amplifier. Basic parameters of the �requency modulator;
Central frequency, herrz 1850+15
Frequency deviation, hertz g1600
Frequency atability, hertz 1�10'4
Output impedance, ohms 600
The frequency modulator signal of the amplifier modulator unit is fed
to the radio station modulator which takes the signal to the ultrashort
wave band.
r
The ultrashort wave signal goes through the air to the receiving radio
station, from the output of the receiver of which the frequency-modulator
signal is picked up in the 300-3400 hertz band and it is fed to the
modulator-amplifier unit.
Demodulator (D). The basic purpose of the demodulator is converaion of the
frequency spectrum obtained in the receiving radio station (300-3400 hertz)
to the low-frequency spectrum of seiemic information. Let us briefly dis-
cuss its operation (see Fig 28, c).
The demodulator is executed from five triodes and five diodea. The ouCput
- signal of the subcarrier frequency with an amplitude of 5-8 volts, similar
with respect to shape to sinusoidal, goes from the radio to Che demodulator
input where a threshold unit of the Schmidt trigger type (T1, T2) converts
it to square pulses. -
The shaped square pulses are differentiated; then they go through the C3, R7
_ circuit to the slaved multivibrator (the triodes T3, T4) which shapes the
pulses of constant duration and amplitude independent of the input signal
parameters. Only the frequency o.f shaping of the pulses determined by the
input signal frequency is a variable. Then the pulses go through the emitter
_ repeater TS directly to the demodulator D5, D6, R15, C8.
'Che a(lvantages of t}ie described demodulator circuit are the following:
a) Cconomy the demodulator does not require a separate feed and is
connected to one power supply (a 12 volt storage battery) jointly with other
units of the channel;
- b) Absence of mutual effects between the channels and, as a consequence,
quite high noiseproofness;
c) Resistance overload, simplicity, reliability, a small number of parts.
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Uf L.
4 APRIL 1979
,I !
a
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The low-frequency sipnal is .fed from the demodulntdr nutput Cd the recnrding
oquipment.
(.h;iiiiit, l (:n I Ihr;it toil, 'I'lit - iirnhlemy tir rn 1lhr,httng tliv peiqmir equipme nt,
th,it [K, dei.erminatinn of thr frequenry-amrlttudr ind phage charecterigticg
of thr neigmic channel and algo amplification of it have been inveatigated
in many papers, for ea;ample, in (45] and other papera. The callbration df
the racltoeelemetrir r.hanncl hns ita own sper,ific charactprigticg.
Accually, on an ardinary seinmic gtation all of the channel elements are
lor.hted in direct proxfmity to each other. In the radiotelemetrie channel
the individual eleme�ta nre located at grQat dietanCes, in pnrticular, the
recr_ivinR And transmittinK parts are several tens of kilomecers gpnrt. In-
asmurh as Che tran9mittinK radio stati3n is rigidly "tipd" to the AC network
rower yuprly, in the srarch for a"quipt" place it ia necessary to remove ~
the 5ciqmometers to gignifir.anc (up to 300-400 meters) distanceg. Simul-
tnneoualy, in order to avoid induction fren the tranemitter icseif, the
rrc,7mnlifier and the amplifiPr-modulator are moved Chere.
Additional diffirulCiea occur when calibrating well channels, the seiamometerg ~
nf which are located !.n the wells at great depths and are connected tn the
E;round cquipment by lo�g lines (the ronstruction length nf the series-pro-
duced armored logging cables is abouc 3500 meters). 'I'he influence of such
long lines on the parameters of the entire channel must be taken into
account. 1n addttion, at grea[ depths (to 3000 meters) under high tempera-
ture conditions reaching 100�C, the seismometers change paramecers. Thi.s
is taken inco account by introducing the correspondinR directions or
aprroaching the actual operating conditivns to the maximum When calibrating
the channel. Inasmuch as the radiotelemetric channel is made up of seismic
and radio cortmiunicacions channels, the latter must be individually tuned
and adjusted before calibration in order to avoid its influence on the
5ei5mic channet parameters.
Frequency Characteristic of [i;e Channel. Accurding ta Fig 4, b, the
characteristic on the 0.7 level has a pass bnnd of 0.8-7 hercz. In order
to comPensate for the nmplificacion of the seisnopraph emf with an increase
in frequrncy, an inteqrating cell is provided in the amplifying-recording
equirment (see curve 2. Ft� 4).
Whr_n prenaring the r.idiotelemetric channel for operation when all of its
= astirmblies are ]ocaced on the central recording station, the frequency
chararteriscic of bnrh the entire channel and its individual elements can
he nicked up hy any oC the known procedures. When part of the equipment is
instai leci at the svismic� and data transmission point, the most convenienc
for determinatten of the frequenct characceristic of the entire channel as
n whnle is che provedure f.or which the signal is fed from the generator on
v,riouti frequcncirs aireccty to the input of the concrol coil ahe:hPr it is
a Itrotincl gcismomecer or a deep Well seismometer. This prc+cedure is con-
vvnlent for daily nonitoring feeding the signal of a constant amplitule
92
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mxgnetiC generardr (riCpA) to the auxiliatry coi1, it ie poeeible to con-
tral bath the shape and levpl uf the frequency charactextstic of the
r.hannpl operativrly.
1t ia alKO rngeihle to piCk up the frequency charnctpristtc of the amplify-
inti 3nd recording channel, feeding the gignal frnm the generatdr to ite
inrut. Then multiplying it by ttie frequenCy characterisCic of the -
qeiamumeter and introduring a correction for the seismometer `onverter, we
nbtnin the frequency charncteristic of the entire chgnnel.
C:hnnnel Amplification. Under laboratory cdnditions, before-seCting up the
ch.ynnhl Enr operation, the amplification, jugt as the frequency character-
istfc, can be deeermined by varioue methoda (tor examples electrodynamically
or by the mpthod based on direct meaeurement of the diaplacement of the
rendulum by a microscope [321). Usually the recording of the frequency
characteristic and determination of the amplification both in the labora-
tory .hnd in operation are handled in the same way. For determination nf the
amplific3tion by the procedure moat convenient for an operating radiotele-
metric channel, firat it is neceesary to determine Clte senaitivity of the
amplifying and recording channel as a function of frequency, feeding the
signal from the generator co the input of the prenmplifier. Here we
simultaneously obtain the frequency charactertstic of the amplifying and
recording channel.
The amplification of the channel is calculaeed by the formula
V=SU2nGRinput amplifier/Minput amplifier+RK)'
where S=Arer_ord/Uinput' m/volt is the sensitivity of the amplifying and
recording channel equal to the ratio of the recording amplitude on various
frequencies to the voltage fed from the generator to the input of the pre-
-implifier; U is the frequency characteristic uf the seismometer for the
adopted d vnping coeEficient D Which is taken from the standard curvea;
C. is the electrodynamic constant of the seiamograph coil; R is the reduced
length of the pendulum: Rinput amplifier is the inout impedance of the
amplifier; Rk is the resistance of the operating coil of the seismograph. `
Lec us note that the values of the amplification of the same channel taken
by (I{fferent procedurPs usually are quire cloae and do not differ by more
th:in 5 to 10Z. Therefore the choice of procedures is determined by the
arFumenta of convenience under certain specific conditions.
Controlltnk the Identity af the Receiving Parta of Radiotelemetric
Channela. This rontrol can be realized by two procedures. The first
c�onsista in the fact that one transmittinR station is organized at the
rentral recording stntion co which all of the receiying stations are tuned.
Peeding the voltage on various frequencies co the input of the modulator
(nr scismomeier) frc,m the Renerator, it is possible to cons[ruct the
lmplitude-frequency characceristics for each receiver ard then compare them.
93
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A" I n ernnd, striCter and more objective prncedure consiaCg in Cuning all nf
~tha~,rrrriving gtntiong td any one transrniteing etation 1ncnCed aC the
Ae, ismic data transmiesion point and recording identical seismic informaCinn
for some eime from the eame eeismograph.
Channel Control. For operative control of the parameters of each channel
nn the tranemitting station, automatic feed of the control eignal of the
itGrA to the control coil of the seiemograph has been introduced. The
Contrnl signgl makes it poagible to dctermine the parametera of the entire
rndiotelemetric channel and trace their atability. For thig purpoae the
circuit has bepn developed (see Fig 28, d) for automatic feed of the cnntrol
siRnal. The control signal from the rtGPA is fed to the control coil of the
seismograph through a potentiometer by meana of which the required ampl!tude
of the conCrol signal is eaCablished. The circuit diagram of the MGPA
[constant amplitude magnetic generaCor] contains a rectifier, a time relgy
P1, servorelays P2, P3 and the electric motor D, the ahaft of which is
installed coaxially with the ahaft of the MCPA, and both are connected to
earh orher by n epring couplinq.
On rlosure of the contact K of the alarm of the Slava electromechanical
clnck, the relay P1 is connected ttirough the normally closed contacts to -
the relay P2, and the electric motor spins the NGPA. After 10 to 12 seconds
during this time the frequency of the MCPA reaches 10-15 hertz t1le
relay P1 is switched on, and the power is disconnected from the electric
-notor, simultaneously connecting the outnut of the MGPA to the control coil
of the seismometer through the contacts of the relay P3. Thia reTay
remains connected until the contact K of the alarm on the clock is broken
(approximately 2.5-3 minutes). The duration of the control signal is
1-1.5 minutes. The power supply for the circuit is realized from the oower
supply unit of the RRS-1M radio station (12 volts DC and 127 volts AC).
94. Equipment of the Central Recording Station
At the Novo-Alekseyevskaya central recording station, after demodulation
the seismic signals are recorded in two modes: continuous and slaved.
Conttnuous Recording. The recording ia made by a nen recorder, and it i.s
basically a display. It permits observation of the seismic regime, opera-
_ tivc: determination of the directions of the sources of distant earthquakes
and the coordinates of the centers of nearby earthquakes. The directton of
the source can be determined without interrupting the recording several
minutes nfter recordir:g the first wave of the earthquake. In additioli,
the display recording permits continuous control of the operation of the
stations, the noise level, and so on.
For rontinuous recording, the RV3-T visible recorder is used in which power
ampliEiers have been utilized which were developed at the Earth Phyai.:s
Tnatitute oE the USSR Academy of Sciences (Fig 28, e). The amplifierq are
assembled from fivc triodes in a circuit with galvanic coupling and
94
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HymmeCric emiCCer rcpentera nt rhe outpuC. In order to ineure sCgbility
of Chp parametera, the amplif.ier ie encompgesed by Cwo common and two
ineprnal negative feedbacke, and it has five pogitione fnr manual regule-
tinn of the gain (6 dhribels ench).
Basic parnmeters of the amplifier;
Mgximum amplification coefficienC with respect to
voltage 800
rtinimum input impedance, kilohmg 9
Output impedance, ohms 50
Structurally the recorder contains four amplifier modules loaded on the
pen recording heada with a resistance o� 800 ohms and a resonance frequency
of 8 hertz. Inorder to record the aignals from the radiotelametric syatem,
eacti unit oE the.amplifier also has demodulatora mounted in it. Instead of
a collectorleas nC motor, a DSM electric motor ia used to wind the paper
tare. It is fed from the 224 volt network. The power supply for the
demodulntors and the amplifiera comes from the same 12 volt storage battery.
5laved Recording. The slave recording system organized at the central
station makes it poasible to record only the uaeful eventa, the recording
of which is uQed for basic processing of the materials, anal,yais and compar-
isun of them.
The four-cfiannel slaved recording system was first organized on the basis
of the device with magnetic memory developed and manufactured by the apecial
design office of the Earth Phyaics Inqtitute of the USSR Academy of Sciencea.
However, the significant deficiencies discovered when checking out and test
operating the equipment led to the necessity for significant alteration and
improvement of its assemblies and units. The specific peculinrities
connected with the multichannel radiotelemetric recording led to the develop-
ment and manufacture of a special analysis and switching unit. A description
uf the slaved recording system is presented.
'i'1le baqic clements oi the system are the analysis and switching uniC and
the magnetic recorder.
Analysis and Switching Unit. This unit switr_hes on any of the recorders
(one or several simultaneously) on aPpearance of a uaeful signal confirmed
by three radiotelemetric channels and it disconnects the recorders when the
signal intensity drops below the siven level with reapect to a:il three
channeig. The circuitry of the unit (Fig 29) includes a contrnl panel,
threshold circuits, logical �ilters, disconnect relay, connect relay,
servorelays, selector circuits, and comparison circuit. Let us briefly
ronsider the operation of the elements of this unit.
The clireshold circuit is made up of matching stages eaecuted from the T1-T3
triodes and the Tshl-Tsh2 Schmidt triggers. It is used for shaping
square pulses at the output in the presence of the seismic signal at the
95
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inpuC exceeding the gtven tevel. The xegulation of the rpAponae
thrnahnld is reatiyed by the It1-R3 rotenCiomeeQrx.
'L'hr. 1ngLcn1 Ciltet'g whirh genpratp the instrucCi,on Cu AwiCch on axe
exeruCecl from Criggere ronnecCed by the counting circuit in such a way rhaC
the triggers Tgg, T96, Tg9 are set to the one condition when four atart
pulseg nrrive from the tiireahold circuit (which correaronds to four periods
oE the input signal). The -10 volt level ia taken as the onea condition.
Thus, the Eilters filter out ones noiae.
The disconnecC relays periodically c1e=r the logicAl rriggera og the filters
in order Co erase Ealse information. This information is atored by the
logicnl filters on random arrival at the threshold circuiCs of signals
- exceeding the given response threahold. The disconnected relay is nade up
of the trigRer Tglo, the time relay based on the triodes T6 and T7 and the
P1 relay. On appearance of the pulse from the threshold circuit of any
chunnel and passage of it through the Ott collecting circuit (TS, D10-D12)
the tr.igger Tglp is set to the ones condition, it starts the time
relny and after 10 seconds the P1 relay is switched on, through the contacta
oE whirli the clenr signal is fed on closure to all triggera of the circuit,
including Tg1o. The signal light L1 indicates the passage of a single or
periodic signal the given level through one or several chnnnels. On clear-
ing, the entire system is initialized, and the light burns. IJiCh the arrival
of a single signal the operating cycle repeats. This condition of the cir-
cuit is slaved even in the presence of a regular signal at two diodes
simultaneously. I
The switching on relay closes the circuiC of the servorelay IR in the
presence of a signal at the outputs of all of the logical filters simul-
_ taneously and it disconnects IR after diappearance of the control signals
- from the threshold circuits. The switching on relay is made up of the
trigger Tp,ll, the time relay T8-T10 and the relay P2. On arrival of a
regular signal above the given level at all three inputs, the threshold
devices develop the start pulses of the triggers of the logical circutts
with frequencies equal to the f.requencies of the incoming signals. After
passage of four oscillation periods along each of the channels, the ti�iggers
T93, T96, Tg9 fiip to the ones condition and thus switch on the comparison
circuit (Tq, D13, D15)' The signal passing through the comparison circuit
trips ttie trigger Tgil which leads to response of the relay P2 which by
one oE i[s contacts includes the servorelay IR, and the other, the preset
input 2 of the triRger TR11 to the output of the OR circuit.
in this mode the trigger Tgli i,s periodic.ally initialized by the clear
signal from the disconnect relay and it is again set to the ones condition
hy the input signal of any other channels. The re?.ay PZ will stay in the
on state until the input signal level falls below the threshold value on
all channels. After disconnection of the relay P2 the recorders are
disronnected, and [lie connect relav aRain connects only to the output of
the comparison circuit. 'Phe system goes into the slaved regime.
96
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r

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^ 2i aI
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i-. i.
tl c ~ c+~
F'OR OFFICIAL USE ONLY

N M
rl rl rl
, vv v
rIV M/
cm.
Bd
rAff,fd ~~l1Al00P tk
~ p
u u
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 ~ gq~ if6, ' ~loy~, ~ ~ ~
N I "
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( I 44 $4
d200 tan the group ceasee to
onerate for determination of R and only one nomograM ie eufficient to
determine the azimuth at the epicenCer (see Fig 90).
In addition to inconvenience of eelecting a large number of nomngrams,
their deficiency is loa accuracy of detprmining the depth of the center H.
For the poesibility of increaeing the accuracy of determining ttte hypo-
Centere ahich are inherenc in the radiotelemetric multichannel recordittg,
the gelection etep size for the depthA of S 1-m ie too large, and decreas-
ing the scep requirea additional nomograms. This ie not justifi.ed, for
the accuracy of determining N quickly decreases With an increaee in the
epicentral dietance (Ftg 38). At R>20 km from the central statione
(Almn-Aca or Talger) the resolution With reapece to depth is lov, and
for R-30 km it is in practice zero. At the same time under the conditions
- oE the Alma-Ate ceet area for the ma)ority of the obeerved centere the
epicentral dietances frotn the Alma-Ata end Telgar atations are more thgn
30 km.
tn the nomogram procedure only the P Wave$ are used. Exclueion of the
5 waves from the inveatigationg the Arrivals of ahich ueually are clear
on the recordinge of the locA1 earthquakes eliminates ndditional informa-
tion Which percoits control of the convergence of all of the data and the
exclusion of groea errors. Therefore the nomograms aere used to
decermine the poAition of the induacrial explosions (11-0) and for opera-
tive approximate determinAtion of the coordinates of the epicentere.
122
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~
~
t
D
~t

-
.�e (1)
dt
~
.
! .
a-~ t
o-.  .
~ ~ �
~ ~1~;~ (3)
ti � ~
T T
(4) i
-J? -!B -6 -0 -t / t V i / 11d~�9(2) I
Figure 36. Difference in time of arrival of the 5-Waves (AtS)
at two etationa ae a function of the difEerence
in the time of grrival of the P-aaves (6tp) according
to the data on the local and nearby earttiquakea
for three paire o: atatione.
1-- Ozera-Z'algar, 2-- Aima-Ata-Talgar, 3-- A1i-Talgar.
The light symbnls are in accordance aith the dieplay
recordings, and the dark gymbole, by the slaved recording
seismograms.
Key:
1. stp, aeconde 3. north
2. Ats, 9econde 4. aouth
'fhc divergence with the data of other ,vi~un uutermining the
epicenters by the nomograme ie explained by neglecting the apatiel po9i-
tinn of the system etations; for gimplicity hereafter We shall agy
"negleccing the day surEace reltef."
igikaWn Procedure. It turned nut that the determination of the positions
of the centers by che IgilceWa procedure (4) ueing the fictitious velocity
VF gives large errore. The determinations made by c+ifferent triplets of
atations gave error triangles vi[h 10 km sidasand more. The deptha of
the cencerA Fere also found to be differenc. Bxamples of such conatructiona
are shown in Fig 39. For example, let us consider the construction of the
epicenter of earthquake No 124. Three positiona of the epicenters 5 to 6 km
frem eACh other were decermined by the Iaikawa procedure vith reepect to
three triangles of statione Alma-Ate-Ozero-Telgar, A1i-Alma-Ata-Telgar,
Ali-Ozero-Talgar. The depths at the points of interaection of the chords
are different, and for the different station triangles they are 16, 20
123
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and 22 km respectiveiy. The obaexved conseructi,on errora, as anelysis
has shown, wpre beA3caliy cauaed hy neglectirg thp d3fferent altitudee
of ehp obgervation pointe.
Actually, the differenee in abeoluee aititudee for the tpet area gtationa
exceeds 3000 m@terat the Ozero station is located high tn the mountgine
with an altitude of 3000 metera, ehe Aima�Ata station io in the plaine,
and iCg eeiemometer ie Aubmerged in g aeii to a depth of 1000 metere.
in addition, the eeiernogeological cc+nditione are differpnt for thp etations.
The Ozero and Taiger etatione arp on bedrock. At the Ali station there
are 50 meters of eediment betaeen thp aeismometQr and the roofe of the
bgaement. Under the eeismometer of the Alma-Ata station thQre are 3200 m
of sedimenCary rock. Al1 of rhie led to the neceeeity for eelecting a
aingle reduction ievei. The depth of the baeQment under the Alma-Ata ~
station 4200 meters under the day surface WAa taken as this level.
'Che diegram of huw the gtatione differed aith reepect ro elevgtion relative
to eaCh other and ebove sea level and eleo the positinn of the rpduction
1pve1 are indiceted in Fig 41, e.
rtme Field Nethod. The neceseity for introducing time corrections for the
relief geve rise to exppdiency uf conetructing the opicenters by the time
field method. In order to recalculate the obeerved Cimee for the P-wave
to reach the reduction level it ia eufficient to take croas eectione of
the time field by the horizontal plgnes et daptha equal to the amounts
the etatioea are above the raduction level and to take them aa ehe zero
depth levels. For the different etetions the depeh of these levele is
different. For the Ozero station it is 6360 metera if ve coneider that
the time field ie conetructed with the cencpr at the pnint vhere the depth
is equal to zero; for the Talgar station ir ie 4600 metera, for the
Ali station it ia 3500 meters, for A1ma-Ata it is 3240 meters. The only
time field 'of the P Wave, just ae for the uniform medium aith Vpu5.9 km/aec
was constructed for the firet three stations. For the Alma-Ata station
the time Eield Wae conetructed for a two-layer horizontal-atratified
medium: che sedimentery series 4.2 km thick aith Vp-4.0 km/8ec and the
halfspnce -Vp=5.9 km/aec. -
Further operatione to determine the poeition of the centers ueing the
time Eielde were of a atandard nature (8, 52). Examplpe of these
determingtiona can be seen in Fig 40.
1.et us consider tite detetmination of the hypocenter of earthquake No 203
by che time field method aith and withouc coneideration of the relief by
the four stations (Fig 40, a). The epicentersturned out to be close,
2 km Erom each other, and the deptha of the centers. 14 and 20 iap
respectively. Hoaever, in the firet caae 14 tcm Wae reckoned frocn the
reduction level, and in the aecond case, from a day eurface, the elevetion
of ahich is unkna+n. Reducieg the depth by 6 icn (14 inetead of 20 km)
increases the error triengle by 10-15 timea. Thue, the radiotelemetric
recording made it poesible to reiae the accuracy of determining the depthg
at distances not exceeding 30 km to the nearest station to +1-2 km Which
led to the neceseity for considering the epatial poaition of the atationa.
124
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t,~
J
J
J
A

_j
Figure 37. Nomogram for determiniag the pogition of the epicanters
7'he differences in time of arrival of the direct longitudinal waves
at different patrs of stations are plotted on the axes. The
igolinp parammetpr R ie the distance from the epicenter to the
Alma-Ata station. The numbers of the isolinee are the azimuths
of the epicenters.
Key:
1. aeconds
2. Medeo
3. Kotur-Butak
125
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,
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.
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FOR O"ICM USE ONLY
.
~ ~ a
a
~ L
h ~
A
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N ~
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u
y g'+
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127
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"P 'i' ' i'

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tim+:.~~""
~wr~Arrt
Ci)
fl~ r
nr ''-~r
~
AtiI. J~ A~11 1 Ai'rf/
x~ ~
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r"v
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ti~ 1A! !t~
s r
#~t~t
r
A ~ ~ ~ t ~n r ~ � ~ .

rAl.l.~J .
,
Figure 39. Decermination of the earthquake epicentere by the
ieikaaa procedure aithout conridering t�elief (1)
and aith introduction of a correction for the
relief (2), by the nomogramg (3) and by the time
field methori cons_idering relief (4)
Key:
1. Atroa-Acl, 2. Ta 1 gair
3. Ozero
128
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F l+Mr
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I l
. ~
LV
~`/~III
, C2) r�,.f�p .

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rt-4Mf
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/

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L.
L
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ir
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(7)
7 w~iv
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ii #.i
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r iix,~
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M&Ar,MCr~` ~ .
~z . CS~ 04 /rI
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+v .
~A~ j / ~ Ih/
(1) (4) u,' t ~ p
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t ~ -
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.
FtRure 40. Oeterminatioa of :.he earthquake epicenters by the
cime Eield methad
[See folioving page Eor legend arad key)
129
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[Legpnd and key to Fiaure 40p pxecedi,ng pagp];
a cansidering (i) and Withouc coneidering re13ef (2); b-�. according
to the daea of three, four and Eive etgtiong of the eoot areal
e-- uning the data from Ghiiik and the Ituneeaty stationg
Keyt
1. A1i S. Novo-Aiekseyevskaya
2. A1ma-Ata 6. Kurmenty
3. Taigar 7, Chilik
4. Ozera
Correecions for Relief. The eoneideratton of th@ different elevationg of
the bbeervation pointe changes the porition of the hypocenter deteraiined
Without consideration of the reiia, thet ig, it leads to a change in the
cddrdinateg af the eenter R, # (in the polar coordinate gyet@m) and H. In
ordpr to Qntimete the magnitudeg of theee correctione under the conditions
of the Aj.mg-AtQ teet area, calculatione aere mnde for three etation triangleg:
Tglgar-Ozero-Ali, Talgar-OLero-Alma-Ata, Talgsr�A1i-Alma-Ata, four depthg
0.5, 10, 20 km and for 60 pointa located in the circle 40 km in
radiua atth its center at the Talggr station. On the correction maps
(exampleg gre presented in Fig 41, b) the ieolineg AR,6# and aH have a
compieac ghape, especially A#; their configuratien varies for different
depth9 and different triplets of etations. For the deep earthquakee
(N,1 S-20 1un) the earrection� cfianging the poeition af the epicenter can
reach sR-+3 km, Ad-�15' and even exceed them. -lith a decrease in depth of
the earthquake centera cheme correctione decreage, eR beconee no more than
+1.5 km, gnd e4st(2-5)0. 'Phe correctione for the depthg of the ceaters
for a11 af'the earthquekes are identical, and they are aithin the limits of
0-(-7) km. The introduction of the correction for the relief into the
pogition of the hypocencere determined by the IaikaWa procedure by the
Talggr-Ozero-A1i station triengle (Pig 39) made them cloee to the hypo-
eonters fodnd by the time fieid method. However, in connection vith the
iabor congwaption of the proceeeing by this method, the conetruction of the
hypoGenters beeically aaa done by the time field method coneideriag relief.
Final PrnceeaYng Schetae. for Qarthquakes recorded by no 1ees than three
gtatione, the following gequence of operacione aas used to determins the
;mgitinn of the center.
1. The search for the hypocentr.11 dietance R1*71 7 cs"P km and the time
ac the center TOftcpl-R1/S.9 by the recordirig oZ the station for erhich
cS_p ig dpcermined maec rpltably.
2� Calculation of the cime to get fram the center to the remaining atatione
Tn=tpn-TO.
Srlection aE the depth of the cencer correeponding to the intereection
of the taorhrons wich mioimum erro* 5y the isochron templetes or time
fieldg.
130
FOR OFFICIAL USE ONLY
~
~
~
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Fox oFFicini. usE otnY
The cdnsCrurtione were done on a 1000000 gcg1e. The values of ts_p were
determined with respect to a1i of the etations; redundant in�ormation was
used eo esCimoee the internal convergencp of all of the deCexminaeions.
dnly snme ef the fictitioua wnves failed to be used, for the value of tgp
ig deeermined by the etations with a di�ferenC degree o� reliebility (the
applicetion of only the vertical seismograph ia frgughC with inaccuracies
in determining the arrival of the S-waveg at the same time as the arrivalg
of the p-wnvea are determined more reliably). Examplee of conatruction of
hypocentere in different directions from the teet area according eo the
data di three, four and five stations arc presented in Fig 40, b. For a11
of the determinaCions the intereectiona of the isochrone are within the
limits of the circle (a d3ameter of 2 km on the acale of the mgp) dee3gnating
the epicenter.
F'or pst3matinn of the accurecy of the conetructions, in particular fnr mor.e
rpmote easterly epicentprs, data are presented from the regional network
stations df the Kazal:h 55R Academy of Sciences, Chilik and Kurmenty. Aa
cen be seen 3n Fig 40, c, the agreerient of the data ia good; all the
isochrone intersect within the circle.
Thedretical calculationg to estimate the accuracy of determininF the poaition
nf the epicenters and the depthe of the centers by the described procedure
eonsidering the position of the Alma-Ata Cest area stationa were not per-
formed. The experimental eatimatea of the accuracy of determing the posi-
tion of the epicenters and the depthg of the centers of the baeic number
nf earthquakes (wiehin a radiue of 40 km from the Ozero station) give
values of +1-2 km. For the edge earthquakes adjacent to the eastern part
oE the circle bounding the test area, the accuracy drops to +3-5 km.
In casea where the earthquake was recorded by only two atations, the poaition
of the center could nat be determined by the indicated proceduree. However,
in order co use these recordings to estimate the seismic characteriatica
(the number of euch earthquakes has reduced with the years, Table 9) the
determination of the epicenter was made by the interaection method, the
radii of Which are equal to the hypocentral distances for each etation
Rn07�7 ts_p. For the construction, the intersections of the circles at
two points are obtained, the azimutha of which differ by 180�. However, as
a reault of the actual position of the centers of the earthquakes south of
the northern Tyan'-Shan' fracture zone (see Fig 79) it turned out to be
possible to exclude one of the two points from the inves[igation, for it
fell in nn aqeismic terricory. If this exception could not be made, the
earchquake vas not nrocessed. The accuracy of determining the epicenters
by tWO stncions ia signifirancly loWer, and for small R depends primarily
on the depth of center inasmuch as with the described method of constructionf
the hypocentral diatances Were identical with the epicentral distances.
ThercEore, the deeper the centerl the more removed the epicenter from its
actual poaition. For small centere located west and eouth of the teEt area
(Aee the depche nnp in Fiq 82), the epicenters are detetmined by two
131
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i
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132
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sCgCions with greater accur.tcy than for the eourheaetly deep earChquakea
for which the epicenCral distances can 5 to 10 lan high, Thia is quite -
clear by the summary map of epicenters ~;see Fig 79), in the souehwesterly
cltrection the epicenters found by the two srations are grouped eogether
- wirh the epicenterg constructed by three or more stat3ons. In the south-
ensterly directinn the epicentera as a whole are ahifted somewhae farther ~
eo the eouhhenat with Yespect to the entire mase of epicenters deCermined _
by the ehre-t stations,.
53. :nergy Claesifi:ation
The energy classification of earthquakes is of primary significance, for
the disCribution nf the earthquakea in apace and time ia considered as a
�unction of Cheir energy. The observations at the Alma-ACa tesC area
were made only by verticnl seiamographs; therefore we used the energy
, estimates of the earChquakes by the data from the Talgar seismic station
where ane of the tesC area stations was iocated. The accuracy of determining
K considerinp, the damping of the seiamic energy in the given area is high
6K=0.2 Co 0.3 (36]. UnPortunately, energy estimates were not available
Eor all of the earthquakea in the bulletin (the high background of
Issyk-Kul' microaeiama or skipping of recordings at the Talgar sCation). _
Therefore in order that the incomplete representativeness of the data not -
distort the eatimate of the recurrence rate of the earthquakes of different
energy classea, an effort was made to use the recording time T'of the
weak earthquakes for the energy classification.
The correlation between the energy class K and the oscillation time t was _
used by numerous authors for different areas [11, 39, 40], and good
agreement was indicated with the data from direct determinations of K by
the amplitudea of the P and S oscillations. We selected 122 earthquakes
recorded by the Talgar station and the sCations of the Talgar and Ozero
test areas and thus having an energy eatimate. The value of K of these
earthquakes fell within the range from 4.5 to 10; the majority of the earth-
quakes are characterized by K-5.5 to 8.0. The number of shocks with K>8.5
and KfS, that is, the longitudinAl wave is higher frequency, its
ehape is complex, unexpreesed end unatable (Ffg 48, b).
142
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,
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(2) .
,
.

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11014 OPriCtAt ME C1NLY
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' ~.rc ~i.-~.~~~~ _ ~ _ _ . . . .
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. � ~ '~~t,~: '
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,
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. . : �
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� � . .
FiQt,rt! 48. Display seianagraas (a) end slaved recording
seiamograme (b) of exploeions in Medeo
Key:
1. Tnlqar drifc; 2. 10 seconds; 3. Aliaa-Ata vell. 4. Osero; S. Ali
vetl; 6. Novo-Alekseyevskaya well.
143
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POR OAPICTAL t1S$ OttLY
(1)
(2)
(3)
(4)
~1)

(3)
(4)
Key:
1.
2.
3.
4.
S.
'Calgar drift
Alma-Aca ae11
uzero
Ali we11
20 aeconds
6. 40 geconda
7. 30 secondg
8. SO eeconde
Anocher characteriacic feature of the recording ie obeerved et the Ali
atation where 20 to 30 eeconds efter the Eirst arrivals an inten8e low-
freq uency train af surface vavee ie recorded f requently predominant aith
regpprt to intensfty over the enomalously high-frequency initial part of
the recording (inctuding the P end S wavea, Fig 48, a). No such "tei18"
are obgerved at the recordinEg of otfier etetione, and the amplitude
dpcreaseg eharply with an increase in rerording time t. An analogoue
charecteristic, but less clearly expreseed, ig obeerved aleo on the
record ings of earthquakes at the Ali atetion.
For the exploaion recordingg an unclear arrival of the cransverae aave is
characterigcic which is most frequencly observed at the Talgar gtation and
, 90fA@ti0lE8 et the O:ero etation. Ac the Alma'Ata gtation the arrival of
the S-wave ugually ie good ae a result oE the differ8nce in frequency
composition and the P and S oscillationa.
Explonionn in the Kotur-Bulak Quarry. Just as the exploeion8 in Medeo,
chey .rc recorded syatemetically. buc much aare rarely, on the averege
8 to 10 explosiong a year (see Table 8 and Appendix II). Here more
Erequenciy than in Medeo. there are largp explosions, and the excitation
144
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Pigure 48, b (continued)

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FOR O1rFICIAL U5E ONLY
candieidns are different, This is reflected in variation of the dependence -
n� Kon ehe weight of thp eherge ()Fig 49). rhe atab3.liCy of the exc3cacion
conditioes and the eonotancy of the location of the exploeions give rise to
a stablp characteristic ehape of the recordirig. Let ug eompare it with -
che different Atations.
Thp examples of recordings of explosione in the Kotur-Bulak quarry are pre-
nented in Fig 50. The most intenee recordings are obeerved at the closegt
Talgar and Alma-Ata etatione, and at the reet the ampiitudes are comparable.
rhe recarding at the A1i gtation is dietinguiehed by the presence of
intenae 1oa-frequency oecillations in the tail eection 25 secondg afrer the
first errivale whieh exceed aith respect to gmpiitude by tvo timee or more
nll of the preceding dacillatione (Fig 50, a). At Ozero aCation thp shape
of the recording algn has a typicel configurarion the 5 aave is almost
ndt expressed With respert to inteneity end frequency. The transverse wave
ia �norly ieolated at the Tal$ar and Alma-Ata station, but for a different
reasofl the valUe of ts,r is emall, and the intensity of the P-wave is
lnrge (Fig 50, a). The Pand S waves ere aeparated more reliably as g
regult oE che difference in their frequency composition by the oscillograma
di the frequency aelection seismic etation (Fig 50, b).
r:xplosions from the Vicinity of Kapchagay. The recordings Were started in
1913. There are comparatively few of them (aee Table 8). The e_+cploeions
Were in a largp area (see Fig 45), and the shape of the recording is unatable.
Examples of eeirAograms are shcnm in Fig 51.
The maximum intensity of the recording is obaerved at the Ali station which
is closest to the exploeions. The arrivals of the S-Waves are even. At the
remaining statione 'falgar, Ozero, Alma-Ata the recording u9ually has
a characterietic ehape Which ;ls typical of remote explosions. It is weakly
expresspd dynamically.
Difference in Recordings of Explosiorts and Earthquakea. When atudying the
geigmic characteristics of the cicy, a great deal of attention must be given
to the diACOVery of the criteria for recagnizing the explosions in Medeo,
Eor they nre in a seismically active region. There are many of them, and
unrelinbte classification of them as earthquakes is fraught aith the con-
gtruction dE fictitious centers shifted in the southeasterly direction With
re9peet to Medeo.
Let us formulate the basic criteria for distinguishing the recordinge of
expiosions in ftedeo Erom earthquakes,
The kinematic signs are necessary and of primary aignificance. These
include the values of tS_p and the differences in timrs of arrival of the
Whves nt the test nrea stations (see Table I1). In the case where there
are insufficient kinemacic signs, it is necessary to refer to the dynamic
signg.
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~
~
~
!
1
1
~
I
~
t
~ot
FOR OFFICIAL USE QNLY
P.ff (1)
j

r
r
~
,
�
�
,
,
.
1
�
.
j

.

. e
!i
(2
�
~
�
~ � �
� /
" ~
�
.
o i.r~s�
i
* � f ii X.
_ Figure 49. Energy of the oscillationa K a8 a function of the
weight of the charge Q for the exploaiona in
Medeo (1) and Kctur-Bulak (2). The dotted line
was constructed by the data of F. F. Aptikayev
for an explosion in Medeo [6)
Key:
1. Q, kg
, 2. year
We shall distinguish two dynanic signs r- frequency composition and
recording ahape. The frequency composition of the recordings of earth-
quakea and explosiona in Nedeo differ etably. The average apectra of the
frequency selection seismic station of the P and S wavea from earthquakes
and explosions are compared in Fig 52, The apectra of xhe S waves from
exploaions at all of the atntionA are signif icantly lower frequency=
on che 1.3 and 2.6 hertz filtere the relative amplitudes Ag/A5.1 hertz
; oE tlie explosion recordings are 2 to 4 timeR greater than fmr the earth-
quakea. The intensity oE the recording on the high.-frequency filterR of
5 and 10 hertz for the earthquakes ia eesentially greater than for the
explcsiona. For the P-waves this law is clearly expressed onlq at the
Talgar station.
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- 'Che critprion for the xenording ahape is lesa specific Chan frequency.
The general characteri.sCic of the recordings of explosions includes leas
clenr arrivals o� the S-wavee, wozse dynamic expresaion o� the S-oscilla-
tiong and the worse, the greater the epi.central diatance (thia ia
especinlly nnticegble on the recordings at the Ali atation). The ratio
Ag/Ap for the explosions ia less than for the earthquakes. The specific
shapc of the envelope of the recording A(t) at the A13 station for
explosions is expresaed aignif icantly more sharply than for the earthquake
(see Fig 43). Wherene for earthquakes the intensity of the tail parC of
the recording is smaller or, in the best case, comparable with the intensity
of the preceding oscillations, for the explosion the 1ow-speed componenta
predominate wiCh respect to intensity on the seismogram. Finally, anoCher ;
dynamic characteriatic, also pertaining to the Ali station, is that the ,
recordings of the explosiona are always much weaker than st the other '
stations. Frequently they are in practice absent (except KapchagAy). ~
AC the same time the reccr-lings of earChquakes at the Ali station are ,
comparable with respect to intensity with the recordings of the other sta-
tions. ~
The time of day when an event occurs can serve as an indirect attribute of
the explosions: the majority of the explosions occur in the range of
10-12 houra Greenwich (1600 to 1800 hours local time, see Appendix II).
The recordings of an explosion and an earthquake in the vicinity of Medeo
are illustrated in Fig 53 for comparison, The differences in time of
arrival of the waves at the test area stations for groups of recordings I
and II are cloae. The consideration of the dynamic criteria helps to
distinguish an explosion from an earthquake, namely:
1) The earthquake recording at all stations is essenti311y higher frequency.
'Chis is quite obvious by the oscillograms from the frequency selection
seismic stations on the 5 and 10 hertz filters the disturbance from the
explosion is almost absent at the same time as the intensity of the earth-
quake recording on all filters is comparable;
2) At the Ali station the intensity oE the recording of the explosion is
mtich weakcr than an earthqtiake (by comparison with other stations);
- 3) The clear nrrival oE the S-wave is not as obvious on the seismogram of
an explosion at the Ali station as on an earthquake recording;
4) The intensity ratia of the tail and initial sections of the oscillations
on the explosion recording (Ali station) is more than on the earthquake
recording.
147
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Y
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.
1) Alt I r"' ~ ~~'t ' ~
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71.Bt. fJt. ~7r1~ t.: . : ;
� 'i t ' ~ w...:..

:
~ w i~: ~a : ~ r~~. r. 'r . . . �
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_ . . ~ c~~ ~.e.,~~,~.~.,r,
~ ~ M 
~ r~~; ~~�1' ~ ~ i, . ,
. A 1 ~r~~1~b 'NwJ� ~ a ~r
r~ � ' , ~r+~~~ - I ' �
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~ ~ ~ ' ~ � ~ � ~ ~ ~ ~ '7"
~ ~ ~ . . . ~ . r{...
~.T.i . . . ~ . � rrr~. ,
r� � . `~1~ , ~r~~~.r r~ S.~ N : �r. ~
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w+~ w � .w... ' ~ ti~ ~ . I.
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-
lb MN. N.. 11"ra"

~
� ~
~
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/r

.
as
~I.Ii~
OJtPO
CA'~ AANpv4i710
LUA, T/Al/0 Q
Figure 50. Seismograms (a) and oscillograma of the frequency
selection seiemic atation (b) of explosions in
Kotur-Bulak quarry
Key:
1. Talgar drift; 2. Novo-Alekseyevskaya well; 3. Ali well;
4. Alma-A[a well; 5. Ozero
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19.17. y// .4
1P
l!/X
Arj�rAlOfI ~ 1)
5 ) JOt
. . . . . . . . . r
,r � ~ ~ . ,
. . . .
. r . . . . . � .
. . . . ~ s . . p
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. . ,
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. . P(2)
. ~ .
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~ � V .
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� � � ~1~YA1~~~� �y~~~~~r� ~ ~y
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~ . ~~~M/~1~Y~ rY � I~ � V
~ � �  � ~ ~~rM~ ~ ~~r.I .
�~r ~'y~ ~l. .r~~~...~~%�~ ~dNq~.~r~
. . ~ . ~ o.~�~ �
~~��~~~~r~r...~. ~'V~~.�
. . ~ � � �\~~M.~~ 1�~~ /~/~SM
1~ � � � I~ M~  ~ ~
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FOR O"ICiAL USB ONY.Y
- A. . ~ r~ ~ y
V 1 I
~ (4)
Key:
1.
2.
3.
Figure 51. Explosion seismograms in the vicinity of Kapchagay
Talgar drift
Alma-Ata well
Ozero
4. Ali well
5. 10 seconds
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.i .
TAA OYYYC2At, U31! ONLg
,
A,ft (2) J , .
I
! n n K
40
4~ /1
n
~s
,s ii
~ ro W
F jo
cs0 .
r~ tr rr a
~J t l,1 tt
_ 4e' ` n ~t tt
4f z. .t-f V >i 4f 4 zr 0 AIM
Figure 52. Average epectra of the P and S waves of earthquakee
(solid lines) and exploeions in Medeo (dotted line).
Key:
1. hertz 4. Talgar
2. Ali S. Ozero
3. Alma-Ata
- �S. Effect of Observation Conditions on Structure of the Seiamograma
The development of seismic research and, in particular, thr trend toward
more complete interpretation of the wave field are more and more frequently
leading to the neceseity for considering the effect of local etation con-
ditions on tht atructure of the seismograms.
The seismological situation in the research area and the uae of raadom wells
for the observations have caused location of the stations in the radio-
telemetric test area under sharply differing conditions (see Chapter II, III).
We liave studied the effect of the reception conditions on che ehape of the
' first wave and structure of the initial pert of the recording of remote
earthquakea aqd also the ahape of the recording of local earthquakes.
Unfortunately, the single-component recording has essentially narrowed the
150
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pagnibilitien of nnnlygin, and hereafCpr ie wilt be neeeagnry to keep in
mind eh8e a11 hf the prepented eneimaten are given by recdrdings of the
vertical component of the osciiletions enly.
CEfect nf Obaervntion Condieione on the Recording of Distant Earthquakps.
'Che initial pere of the recerding of disrgne earthquakee i.n the vgrioug
eeisroologicgl seudipA ie of srecigl interpst, Thie pereAina, in partieular,
tn the probiems of intprferhnce recepCien in order to ieolate the ueeful
$ignal, study the exchange tranemieted wevee, and go en.
The initial partg of the recordings of diatant earthquakea recnrded gt one
station, as a ru1e, differ from Qach other. The recordings oE a aingle
earthquake obtained at different stgtions a1so differ. These differencee
are cannected with the conditfone bdth at the gource (center) and in the
recepCinn area. Thp larqe volump of geiemologica1 reeegrch performed in
recent yeare basically when studying pxChange Wavpa hag madp it poegibie
eo aeudy the effect of the gource erea. Ir wae demonerrated [51) thet
firnt of n11 the depth of the center hea astrong effecC on the initial
parC of the recording. The eimple initial part of the recording representad
by one wave out of two or three oecilletion phaseg correspondg ueueily to
depths of renters of 200 km or more, With n decreage in depth, the initial
part of the recording is compiicated. The parChquake recordings are the
moac complicated, the centers of Which are located in the crugt.
Table 12
Azimuth from No of
the ralgar earth-
J Area _ station, deArees quakea
Alaska. Aleutians
20-50
10
Kurils Kamchatka, Japan
50-80
17
Marianas Islands
80-100
10 -
Indonesia
110-150
40
AEghanistan, Hindukush
210-230
14
Chile, Argentina, Bolivia, Peru
.'i0-320
16
Arctic Ocean
330-0
10
151
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m 0!'rICLL m aN.Y
Table 13
xey:

2.
3.
4.
5.
6.
~1)
(
(3) 4xono caeoe~rasna~c wa~cai
~
p
sa~nr-
Aiat~i- ~
T~uvR
Jlraia�
Taiwa
Aiar��
Twm~pe
Tmn

r~np
~
ai
~
'
A'r'ti
,
Po
~
Avti
k~P~"M
0"Ps
k~p'nt
Ary
po~p,o
amm
Amt
A'~'~'
~
~
I1 �
y~~
~
~
�YI7il~
s_

,
AWr-
w� 
~ �
1e72
aa
s~ 4 e ' io
1973
es
as q 4 T sz as 37
1974
til)
t*oro
80
iee
sa _ _
23
iii 8 is 17 ea ee eo
Year
Total number af recordings
No of compared recordings
Talgar, Alma-Atat Otero
TAlgar, Alma-Atat Ozero, Kurty
Talgar, Alma-Atat Kurty
7. Telgar, Ozero, Kurty
8. Talgar, Alma-Ata, Osero, Ali
9. Tslger, Oxern, Ali
10. Talgar, Aima-Ata, Ali
11. Total
5tudies were also madp af the ehape of the recordings aa a function of the
areae in ahich the earthquakes occur. The simpleet form of recording ia
obeerved moat fYequently for the Qarthquakes in Kamchatka, the Kurile-
Jnpane8e zone, the Pacific Ocean and Indoneeia. No clear depeudence of
the ehepe of the firet Wave and the etruceure of the initial part of the
seismograma on the epicentral distence i9 noted.
The eEfect of the reception conditions hae been etudied appreciably lnas.
WQ selected diatant earthquakee recorded by three or four statione of the
test area in 2 yeara from March 1972 to April 1974. The baeic principle
for gelecting the material was eimplicity of shape of the recording of the
first Wave the preaence of a ehort pulee at even one of the test area
etations. For anelyeis 188 recordings of distant earthquakes were taken
which are coordinated aith the different epicentral zones locaeed in differ-
ent azimutha With reepect to the teet area Which made it poaeible to
exclude the effect of the direction of arrival of the wnves. Table 12 shoWa
the basic epicentral zones, their nzimuths and the number of investigated
earthquakee in each of the zones.
In addition, a study Was made of the recordings of individual earthquake8
from Europe, India, Oceania, Iran and other areas.
Sharply different station conditions lead ta the fact that the recordings
_ nt the different atatione differ significantly from each other, Therefore,
even the high quality of visual comparisons Gurned out to be inadequate to
discover the baeic laas of theae differences,
152
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.1. ~ . r � y ; ~ ' ~ ~s..~~ar~+.~. . ~Y
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i~i~i~iiii:ii:.:iiiiii~~a~ ` ~
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aij'~~..~.i~' �1
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ii~ ~ i ~ . ~ � . ~ ~ � w.... r..r..
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Figure 53. (See folloving pageJ
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~ ~ ~ ~ ~!t!kl
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154
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Pil;urr 53 (See precedinp, page). Dispiny oeismngrgms (n) and stgved
reeording neiamegrams (b) and omcil,lagrame eE Che frpquency aetecli,on
npiemie etation (c) of an expiosion (i) and an earthquake (II) in the
vtcinfty oF Medeo
Key:
i. 10 gecondg 6. Novo-Aiekeeyevokaya Weil
2. 'Caigar drife
3. A1tna-Ata we11
4. dzero
S. Ali well
b . c
p j
~
tI j Ll Lop"'If
~ t/ "A T 0 rR,N A, t I A-Al A
Figure 54. Earthquake dietribution With reepect to nature of
recording at the Talgar, nzero, Alma-Ata and Ali
stations
a-- the simplpst (1) and the moat coroplicated (2) structures of
the seismograms of the initial part of the recordinga;
b-- shape of the recording of the first Wave simpleet (1),
moat complicated (2);
c-- Ere4uency oE the first wave, highest (1), loWest (2)
The recordinge of groupA of stationa preaented in Table 13 were uaed for
r.ompurison.
Tiic rcsulta of comparing the recordings at the Talgar, Alma-Ata, Ozero
and Ali xtationA nre presented in Pig 54.
InitiAt t'art of the Recording. When analyzing the structure of the initial
part of the recgrding (about 40 seconds) consideration Was given to the
number oE aaves, [heir inteneity, mutual arrangement, correlatability on
the recordinga of the different stationa. The results of the analysis
lead to the following conclusione.
Among thr ground stations of Ozero, Talgar And Kurty located on outcrops of
bedrock, but under essentially different conditions of the ground relief
high in che mountains, in the foothills and on the plains the aimplest
initial pxrt of the recording is observed at the Talgar station. The
simple$t atructure of the recording is recorded 10-15 times more frequently
here than at the Ozero station.
155
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iiOl dfIRGYeL M tNL!
pra ri~s*~
r~ r* 2117m r ~.rhrR
� . ~.J~ . ~ .
~
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. �
� r I n.l .FIC - I
0 '
.ti
x
Ir
Key�
�I.
2.
loe
s ~
6
1'iRure 55. Compariaon of the recordings of dietant earthquakes
by thc ground surface and deep wells on RTS 8tationa
(times o! Arrivnl at all stationg are camparable)
peconda
16 September 1972
156
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The mogt Compiex atructure di the iniei,al parC of the recdrding in obaerved
ne Otern oeation in 70 ta 902 oE the caees (when comparing the recordin~~
of dtE[r.rent Rroupp cf ntneidna). The iniEf.a1 part of che racording hpre
in the mnpt exrrnded, tntpnoo end ieane reaoived by comparieon aieh the
reCerdinqo of ether stneiona (Fig SS),
Sueh a gharp camplicgtion of ehape of the recording on the station lacated
in the mounCains was of great intereat. in order ta txcludp the effece of
any stricC1y 1oea1 eguaes cnnnected with the ingtaliation site di the
insrrument, obeervations Werp made at three points within g fea kilomptera
af eaeh other on the ehere of 8alahoye A1ma-Atinakoya Lake, at the
corongey station dnd the GAiSh Obaervgeory. AC a11 of these pdines the
reeording differed peraiatently by signifieantly greaeer complexity ehan
at the remaining statione of the eegt areg.
Althdugh the Kurty gtetion is lacated in the p1ains, it is chargeterized
by asfgnificantly more complicated structurp of the iniriei parc of the
rpcording than the Ta]pr gtation end aomewhat simpler or rommeneurate aith
respert to complexity of the recording of the Atern gtgEion. All the aub-
gQqupnt part of the recording at the Kurty etation (Fig 55, recordinge, S. 6)
is represented by groure of oecillations, sometines inferior vith reepect
to intensity to the firet wave, at the same time eg at the other etaeiong
the Eir9t pulee predominatee aith reepecc to intensity. The complex etruc-
ture of the recording at thie etation obviougly is caused by nonLniformi-
ties oE the upper part of the eection. The observations at the Kurty ete-
cion aere short-term, and they ate inadequate for gtacietical eetimates of
the material.
Deep-Wel2 Stations. It is not poasible to compare recardings in a Well
and at its hend on the day surface directly. The Wells of the test aree
are lacated in populated places, under conditione of high eurface noiae
levels; thprefore the recordinga at the day surEece and at depth are nnc
cnmparable. Usually earchquakes which are recorded in a Wpll With rpadgble
_ amplitude arc not recorded at a11 on the day surface. On the contrary, the
recordinPs of stronger events Which give readablp amplitudes on the day
gurface nre crnnpletely Washed out ac the deep�well gtation. Therefore the
oscillograms ot the aell statione can be compared and they can be rompared
Wich the seismograms of the ground atatlons o: Talgar, Ozero and Kurty.
At the Almn-Aca, Ali and NovcrAlekseyevskaya aell stacions the initiel part
of the rccording, As a rule, is much simpler than at the Talgar ground gta-
tion and the more sn at the Ozero and Kurty acations. The recording in the
uell ia characterized by a short Eirst pulse and A smaller number of Waves
er their absence in AubAequent arrivais. The aubsequent o8cillations are
morr frequently Weaker than the first vnve. The seismograms of distant
enrthquakes in Fi$ 56, a illustrate this relation in the exaamle of record-
inga in the Almu-Atn and Ali 'aells qnd in the Tnlger and Ozero ground
stAtions.
157
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The nwnber of cegea ahere the aimplent gtruceure of the reeording at the
Aima-Ata gtAti.ae 3n obgarved ie 702, at the eame time as at che Taigar
station ie ia 202, aad ae the Ozero scaeion, 1.5% (Fig 54, g), This form
of mor8ing at the Talggr anA Aima-Ata eeaticna in observed rimultgneoualy
in the majority oE cases.
The diEferencp in atruceure of ehe recarding at the Ta1gar and Aii stgtione
ig iesg aharpiy expreased. Here about 302 of ehe recordinge arp comparable
wi.th reapect to romplexity, gnd out of rhe ren+aieing onee the simpipet
recerding at the Aii station ie enceuntered on the average'2 timee more
frequently ehan at thp Taigar station. Thue, by Fig 54, g it in obvious
that in 452 of the caae8 ehe A1i station hee the siwplQAt form of recording
(in 252 of them it ie comparabie aith the recordings of rhe Alma-Ata
_ atation) at the agme eime aa at the Talger stetion the simpiest form ia
abgerved only in 202 of che cageg. in the majority of them this in simul-
tanpouely with the Alma-Ata stgtion.
tf we compare the etructure of the rerording of the deep-ae11 steeiens to
eaeh other, then it turns out that it ig comparable on the whole. If it
differs, then the eimpler form is obeerved more frequently at the Alma-Ata
gtation. The eeiemograph is buried to a depth of 1 km in the 4-lcm aeriea
of terrigenic aedimenta. The more complex ahape of the recording ig
characterietic of the Ali station vherQ the eeiemographe are located in
direct proximity to the basemenc (Fig 561 b).
At the Nova-Alekaeyevakaya deep-vp11 atation, obgervetfong Were performpd
in a gignificantly smaller volume then at the Alma-Ata end A1i etatinne.
The recordings are che closest wich reepect to shape to che recordings of
the Alma-Ata station. Let us note that the condition8 of the observations
at the Novo-Alekgeyevekaya and Aima-Ata etations are also close. The
pxgmples of compariaon of the recordinq� of theee etations are ehoun in
Pig 56, c.
It must be emphneized that the similarity of the ehape of the initial part
eE the recording of the well etacions ie greater than the ground etations
(see, for example, Fig 56, b). In casee where the lov frequenciee predom-
inate on the eeigmograms, ahich is characteristic of dietant earthquakes,
che shape of the recording oE not only the first aave, but aleo all of the
predaminant Waves in the eubsequent arrivals cae repeat uell at a11 of the
- test aree etations ground and deep aell in spite of such different
obeervatlon conditions. The examplea of thpse recordinga can be eeen in
pig 56, b, aeismograns 3, 4.
Fig 57 showe the Aeiemogram of a diatant earthquake reproduced from the
magnetic tape oE the sleved recording syatea. When matching the timea of
arrival at nll the stations, good correlatability o! individual intenee
oscilletions in subeequenc arrivals is clearly obvioua on the recording.
158
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a r. ~n i.,:; (2) M,. V 0 rw,
i~ m e'~~~M mvr. th
,,,,M,��,~�W46-M4 , ,~+M,y~,,~~ . . ..1�,~ .
' D
A ~
~ Z , ~ �a~~r~a
b� i9 J a 71.14 I t. r, xro. r
0
r ~
~ t
c i2. P 7Z~ J~t y 72~c T
7z
ww~,N,w~,w~~~~..-._~~~M+~'~~,+w~~w~--~~n;~~~~~~
J 2 ~ ~ /Oc ,
Figure 56
159
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F'igure 5� [eee preepding page], Simple ehape o� a recording 3n ehe we11
~ aCnCians of A1mA-Atn nnd Ali (a), cempnrieon of the recordinga of the
deep wetl and ground eurface etarions (b) and pecu]iaritlea of the
recordings of ehe NovdyAlekeeyevekaya ae1i atation (c)
Key:
1. 10 seconde
2. 7 December 1973
5hgpe of the Firet Wave. Yn order to solve some of the epec{a1 problema,
for example, eetimate the operating efficipncy of groupe of station,s
forming the interference eyeteme, to etudy and interpret the exchange
waves, and so on, the ehape of the first oscillation hae great significgnce.
The ghape of the firet wave wae Qetimated by Che number of extreme and the
nature o� the envelope.
When comparing the recordings of the ground stations at Ozerot Talgar
nnd Kurty it ia po8sible to draw the conclueion that the eimplesC form of
the first waves juat ae the entire initial part of the recording, ie
observed at the Talgar atation. Sometimes the ahape of the first oscilla-
tion at this atation is the aimpleat it ia made up of two to three
extreme (Fig 58, a). However, even in casee where the first pulee ie not
~ distinguished by such a simple shape$ it is etill simplEr than at the
Ozero station.
1)
2)
3)
k)
~v '(4)
Qiapo (3)
R4AW-Arear (2)
W,rop (1)
Figure 57. S1avEd recording aei,smogram obaerved (at the top)
Key: and after matching the times of arrival (hottom)
1. Tulgar ,
2. Alma-Ata
3. Ozero
4. Ali
160
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� P'OR OFFICIAL USE ONLY ~
i
/ (2)J,pld. 72.t!/~7~^ 10~7tttl~! ~lJLr. nd ~ioI/A~
r r - T
.
~
~ ~ roc K
0 I 0 = � i~ : � t , -
, re. r
A-A
~ o
.~a (1)
. , . ~ . . . ~ . ~ .
_ Figure 58. Initial part of the recording of diatant earthquakea.
a-- similar structure of the initial part of the recording at
_ all etationa; b-- ahape of the recording of the first wave
different (1) and comparable (2); c-- complex interference nature
_ of the initial part of the recording at the Ozero station
Key:
1. 1 second 2. 23 AugusC 1972
~ Although a complex shape of the initial part of the recording is observed
at the Kurty station, the first wave turns out to be frequently just as
simple as at the Talgar station (see FiR 55, seismograms 5, 6) and some-
;imes even,simpler (Fig 55, recording 7).
The simplest shape of the first wave, just as the initial part of the
recording, ia observed in the overwhelming majority of cases (70-80%) at
Ozero station located in the mountains and it is an unbroken train of
ogcillations of great duratioc (see Fig 56, a). In essence even here it
- is impossible to talk about the f3,rst wave, for a large number of waves
are imposed-'on each other. This law is stable~ and it does not depend on
the area where the event occurred,
Comparing the recordings of the Talgarw A1ma%,Ata and Ozero stations out
of the investigated 111 earthquakes in 76% of tlie cases the first wave has
the most complex, extended form at the Ozero station, at the same time
as this is observed in only 16% of the cases at the Talgar station (see
Fig 54, b).
161
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Howevpr, it ie neceasary Cu tlbtp thgr recordinRa are encounCered (abouC
15X) where the pulso oE the firat wave at ehe f)zero station has ehe
Aimrient ahape, Frequhntly thie is norpd eimu],taneously also at the
Talgar station (see Fig 56, b, eeiemogrem 3; Fig 580 a, b, eeiemogram 2).
This occure when the firet pulae turna out to be outeide tnCerpreCaeion
with rhe complex train of oacillaCions following it (Fig 55, recordings
S, 6; Fig 560 b, recording 1).
In rnre caseg the shape oE thp f3rst
comparable. Thue$ in Fig 58, b, two
' of which ia typical and illuetrates
ing of the first oecillxtions at the
recording is characterietic, attd it
the good repetition of Che ehape of
oE the ground sttttions.
wave aC the three ground ataCiona 3s
recordinga are preaented, the firer
the difference in shape of the record-
three ground staCiong. Thp second
ia pncountered rnrely. It illustrates
the recording of the first wave at all
At the deen-well etationa of A1ma-Ata, Novo-Alekseyevekaya, and Ali, Che
shape of the firat pulse is usually much more complex than at the Talgar
statfon, but it is esaentially simpler than aC the Ozero station (see
Fig 58, n). Thus, for example, when comparing the recordings of the Talgar,
Almn-Aen and Ozero stationa it turns out that in 439: of the casea the
shape of the recording of the Alma-Ata well is the simplest (here in 12%
of the cases, simultaneously with the Talgar station). Ar the eame time
the aimplest shape of the wave at the Talgar station is obaerved in 55% of
the cases, and at the Ozero station, in ly 157: of the cases (see Pig 54, b).
The recording of the wells is distinguished by a larger number of extrema
(by one or two) and greater duration than at the Talgar station (see Fig
58, a). In Fig 58, c, a aeismogram of the initial part of the recording
of a distant earthquake is presented with matched times of arrival at three
sCations Talgar, Alma-Ata and Ozero. It is obvious that at Talgar
station the pulses at the beginning of the recording have the simpleat
BhaPe. At the Alma-Ata station Chey are much more drawn out, and at the
Ozera station they merge into a long, unresolved train of oscillationH.
Fo+- explanation of the observed changes in ahape of the recordinq of the
wells by comparison with the simplest recording of Che first wave by Che
Talgar Fround station, a calculation was made of the interference oscilla-
tion formed as a reault of superposition of wave reflected from the day
surface on the wave approaching from the bottom. The pulses of simple
shape and ac differen[ frequency observed at the Talgar station were
selecteci as the initial pulses. The time of arrival of the reflected wave
at different depths was determined by the vertical setsmic profiling data
in the Alma-Ata well,
Fig 59 shows the reaults of the calculation for three earthquakes, the first
pulses of which difEer siqnificantly with respect to frequency. The
puises rec:orded in the Alma-Ata well and in the Talgar drift are shown in
Fig 59, a, b Eor each earthquake; in all cases those aC Talgar are simpler.
In Fig 59, c calculated pulses are presented for different depths from
162
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700 to 1600 mererg, It i,s obvi,oug Ch3C a depeh o.� 1200 meeers the pulses
are extended by comperison with the iniCial pulees,,and with reapect to
shupe ehey approach the pulses observed in the Alma�,ACa well. The compli-
catton of the pulse ahapp ie different fur different frequenciea. Thus,
wherens in g pul'se'wieh a peri.od of Tr1.1 aecond at a deprh o� 1200 meeere
only the nmplitude ratio of the aecond and third extrema varied, for the
pulse witlt a period of 0.8 seconda the complication of the ehape is
expressed in the manifeaCAtion of additional extren;a, and for a pulae with
T-0.5 seconde, two hole extrema, which increases the pulae duration by
1.5 ttmes by comparison with that nbserved on the day eurface.
At the differene well stations " Alma-ACa and Ali or Alma-ACa and
Novo-Alekseyevskaya the ahapea of the first pulses are fzequenCly
close (see Fig Sh, b, Fi$ 56, c, seismograms 1, 2) or aomewhat more complex
at the Ali staCion (see I'ig 55, seismograms 3, 4). On the whole the number
of cnses where the simplest (just as the most complex) shape of the firat
wave is observed nt the Alma-Ata and Ali stations is commeneurate.
Out of the ground stntions, the one closest to the well stationa with -
respect to the shape of the firet wave ia the Talgar station. In Figures _
55 and 56 it is possible to see the similarity of the recordings of the ~
Talgar, Alma-Ata (see Fig 55, seismograms 2, 3; Fig 56, b, seismogram 4)i '
Talgar and Ali (Fig 56, a, recording 3; Fig 56, b, seismograms 1, 2), ~
and Talgar and Novo-Alekseyevskaya stations (Fig 56, c). -
A comparison of the recordings of different well stations leads to the --on- -
clusion that the difference in shape of the first wave, just as the inLtial
- part of the-recording is anpreciably less here than between the earthquskes ~
of the sround stations (see, for example, Fig 56, b, seismograms 1, 2). -
This is obviously explained by the fact that the well stationg are located -
in a comparatively uniform series of terrigenic deposits.
In rare cases good similarity of the shape of the first wave on the record-
ings of all of the test area stations is observed (Fig 56, b, seismograms
3, 4).
Frequency Peculiarities of the Fit'st Wave. The estimates were made visually
by the display recording and in small volume, by the oscillograms of the -
frequency selectirn station (ChISS) obtained by reproducing the magnetic
tapes of the slaved recording system.
It must be noted that the predominant oscillation frequencies at the differ-
ent stations differ little from each other, and in 30% of the cases the
recording frequency of the first wave at all stations of the test area are
i.dentical. This is explained basically by the fact that the maxisnum fre-
quency spectrum of the first oscillation of the distant earthquakes is
usuatly outside ttie pass band of the frequency characteristic of the seismic
channel. As an example we have the frequency selection seismi.c statioii
oscitlogram of one of the distant earthquakes in Fig 60, a. Inasmuch .ns
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.1
t 1-
m xn't itf mt
.
. .
, ~ .
,
, b
c
.
7W
-~v
Jt~ '
.
. . .
!
f ~ .
A;,N
~ r s  ,s ~  � : J,t ~ 11(l)
Figure 59. Recording of the firat wave in bhe Alma-Ata well,
H=1200 meters (a), in the Talgar drift (b) and
Key calculated for different deptha (c)
:
1. seconds
the recording with 0.3 hertz filtration is diminished by 6.4 timea with
respect to amplitude, it is clear that the maximum of the apectrum of the
first oacillation is on a frequency not exceeding 0.3 hertz.
In cases where the spectrum of the initial signal contains components with
frequencies above 1 hertz, the frequency of the recording as a function of
the thickness of the sediments under the station is most clearly manifested.
The higheat frequency oscillationa are recorded at the Kurty and Talgar
ground statians located on bedrock (aee Pig 55), On comparison of the
recordings of the Talgar, Ozero and A1ma-Ata stations in 53% of the cases
the recording at the Talgar station is the highest frequency (gimultaneously
112 at the Alma-Ata station and 7% at the Ozero station) and in only
12% oE the cases, the lowes[ frequency, half of them simultaneously with
the Alma-Ata station (see Fig 54, c).
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d I.1d 71~,t 11~1~'~ f ~t~~17~i~ !~!1"! :
JN;r'I I ~ ~
04
u (1) '
IJ n',~;, X �n n n,.A n 1L ~
' .
. ~ . _ . .
�
,,,"Yrt~r
,,.-.r.....-
~1 ' �
4rry ~i
w�~.M.~w�-. ~M...-
.
0"�
T'I
~ A�A
:.,r.~..
i
A
Figure 60. Oacillograma of frequency selection seiemic atation
of diatant earthquakes
a-- Talgar station, recording amplitude with 0.3 hertz filtration
diminished by 6.4 times; b-- Talgar, Alma--Ata, Ozero and Ali
stationa, recording amplitude with 0.6 hertz filtration
diminiahed by 6.4 times. The slaved recording seiamogram is
presented at the top.
~ Key:
1. seconda ,
At the Kurty atation located in quiet relief, the highest frequency record-
ings are observed by comparison with the rest of the stationa of the Ceat
- area (see Fig 55, recordinga 5-7).
The lowest frequency recordings are received at the Alma-Ata station where
the thicknesa of the sedimentary mantle under the seiamograph is about
3 km. In 40 to SOX of the caseg the recordings at the Alma-Ata station
turn out tv be the lowest �requency, more than half of them aimultaneously
with the Ozero station. The low��frequency nature of the recording of the
first wave at the Ozero station located in the inountai,ns is in all probabil-
ity connected with the phenomenon of interference of a large number of
waves under the conditiona of the complex relteE at the day aurface.
In the Ali and Novo-Alekseyevskaya wells the frequencies�of the first
oscillation are usually higher than in the Alma-Ata well, and they are often
commensurate with the frequencies of the recordings at the Talgar station.
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FoR omicYni. usg ornY
Thie is obgerved eepeci,aily fzequently for the Aii etation (Fig 56, b,
Fig 560 c. neismogram 3), which is the reault of the effect of the
sedimentary series (under the geiemograms in the Ali weil a rotal of SO m
of sedimente, in thp Navo-Alekseyevakaya we11, about 1,7 km).
For illustraeion, Fig 60, b showe the recordingg of the sCations of the
radintplemetric test area and the aeiemograme of the frequency selection
aeigmic stgtion nf a diatant earthquake by which it is obvioua that Che
oecillation components ebove 2 hertz have 1ow intenaity (one the 0.6 herc;z
filter the recording gmplitude ie diminfehed by 6.4 rimes). If we estimate
the rario of the amplitudes of the oeciilatien componente at frequencies
df 0.6 and 1.3 hertz for different etationa, it turna out that wherpver
the ingtruments are lncated on bedrock (the Talgar ground station) and in
direct proximity to bedrock (the Ali well atation), the relative intensity
of Che high frequettcy componenta (1.3 hertz) ia greater than at the
Alma-Ata station located in a seriea of sedimentary depoeita.
Effect of Observation Conditiong of the Recording of Local Earthquakes.
In order to study the effect of the reception conditiona on the ahape of
the recording of local earthquakea (t5.p$10 aeconds), the seiemograms of
all local earthquakea recorded by no lesa than three atations in the teat
area over a 3-year period from 1 June 1972 to 1 June 1975 were analyzed.
It turned out that there were about 160 of them. A comparison of the
recordinge was made qualitatively for the ground etations (Talgar, Ozero)
and the deep-well atations (Ali, Alma-Ata, Novo-Alekaeyevskaya), primarily
by the slaved recording aeiamograms where the scanning rate is 6 timea
greater than on the diaplay seiamograma and also by the frequency-selection
station aeismograms.
Whereas for the distant earthquakes the structure of the initial part of
the recording in the shape of the first wave were investigated aepargtely,
for local earthquakes the duration of the recordings of which usually is
20 to 30 seconds, it is natural to investigate the entire recording and to
consider the number of waves in groups of P and S-oscillations, the
intensity ratio Ap/Ag, the overall duration and frequency composition of
the recordings of different stations for its characCeristic. It must be
noted that in the case of nearby earthquakes such factors as the epicentral
distance, the azimuth to the center, the depth of center and the earthquake
energy can have defining effect on the nature of the recording and mask
the efEect of the observation conditions on the shape of the recording.
It is necessary to take these peculiarities into account.
The results of comparinR the recordings af local earthquakes obtained at
stations under easentially dif�erent conditions lead to the conclusion that
on the whole for local earthquakes the same laws are observed as for
distant earthquakes.
EfEect oE the Parameters R, H and K on the Shape of the Recording. It is
necessary at least qualitatively to estimate the effect on the shape of
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the rec:ording of the opicQntrai diatanrp R, the depth nf centpr Nand the
energy oE the earthqunke K under the condirions of the A1ma-Ata teat area.
mhe dintnnce R hns a sCrnng influence on the etrucCure nf the renording
nf the verticnl companene, espec3ally when the cenrer of the earChqugke is
ldeated close to any station. Tt attenuates with removal of the cenCer
frdm the eest nrpa. Although the centere of the local earthquakea occupy
e differene pogition witti respect to the test area stationa (see the map
in Fig 79, Chapter VI), fnr the majority of them the Ozero aeation turns
nut Co be nearest, the Ali etation turns ouC Co be the mose remote. In
urder to study the effect of the obaervntion condieiona, it wge necpeggry
to select earthquakes so that the effect of the parameter R will be
excluded for the compared recordings insofar ae poesible.
`Che efEect of the parnmeter R on the inteneiCy of the longitudinal wave,
rather nn the Ap/AS ratio and the recording time, is clearly illuatrated, _
for example, by the seismogram of earthquake No 265 (aee F'ig 68). This
raeio on the recording of the vertical component depends gtrongly on the
direction of approach of the wave. For the same earthquake the maximum
value of Ap/AS and the greaCeet duraCion of the recording are obaerved at
the Talgar etation closeat te the center (see the map in Fig 80, d). On
going away from the center the ratio Ap/Ag on the recording of the vertical
component decreasea, and it becomes minimal for the most remote Ali atation.
This is connected both with abaorption of energy and with a change in
direction of approACh of the waves. On going away from the epicenter, the
recording time is also reduced (the Ali atation is an exception in th.is
respect).
The other two parameters H and K, which also influence the shape of tlie
recording, can be neglected when comparing the recordings of one eartliquake
at different atations. However, when diacovering the effect of the st:ation
characteristics on the recordings of different earthquakes, they cannut be
neglected. As an example of the effect of the parameter H on the shape
of the recording Fig 61 shows the recordinga of three earthquakes witli
difEerent depths of center. All of the centers are located south of the
Ozero station (see Fig 80, c) and they are cha5acterized by values of
Ka6-7. As is quitc obvious by the seismograms, with an increase in depth
(Eor Rzconst) the intensity of the longltudinal oscillations and the
Ap/AS ratio decrease.
The effect of the parameter K characterizing the energy of the earthquake
is expressed in an increase in the ratio Ap/AS and the recording time
witli on increase i.n K,
The geagraphic position of the center of the earthquake has defined
influence on the shape of the recording.
Thus, when analyzinq the recordings of local earthquakes it is necessar.y
to deal with the total effect of many parameters on the shape of the
recordinE, and it is not always possible to isolate the effect of only the
167
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~d P
16. . M!'z i
"P
(2) l ofrawm's
NII/
*V, r; N.o
6. ld. 70L, 11, 7'Ma ,
y M J P ~
!Ox
A
N-/37
~
A'-7~ N�9KN J P N!#! lU~. roAto
. ~ ~ lla6f j N~/7AKN ~3~
tUm.To~toP
Anao-An~
(4)
A~c~vaAi,Si~
L
R~Jiw~~dlr
(4)
~ (i
i
t+'e
,
(S)
~ra~o ( 5 )
CKQ l~ixt
.rrwAWw4*
(6)
Key:
Figure 61. Recording of local earthquakea at different depthe
of center II
1. seconds
2. 26 June 1974
3. Talgar drift
4. Alma-Ata well
5. Ozero
6. Ali well
observation conditions in pure form among them. Therefore we ehall dis-
cuss only the most stable laws.
Ground Stations. A comparison of the recordinga o� the ground stationa
at Ozero and Talgar for earthquakes identically removed from both atations
indicates more complex shape of the recording at the Ozero atation, which
was also noted for distant earthquakes. If the epicentral distances for
the two statione are different, then more complex recording is observed
at the station which is closer to the center. Let us illuatrate what has
been said by some examples,
168
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- Fig 62 ehows the recordinge of foux earthquakes, two of whioh are located
cioeer to the Talgar station (a), and two closer to ehp Oxero station (b).
On the recordings in Fig 620 a, tha most unreeolved nnd prolonged oscille-
tinns are recorded by the Talgar staCion, and in Fig 620 b, by the Ozero
gCnCinn. Thie can be seen most clearly on the slavecl recording 8eiemograms.
The fase damping of the high-frequency components and predominence o� Che
low frequenGies in the tail section of the recording most charantprieCic
for the Talgnr staCion on nil recordinga attract atCention. Thia ie
eepecially clearly exhibited in the osrl.llograma from the frequency
gelectian aQismic station. For example, earthquake No 231 (Fig 63) at
Ozero e[ation located two times Closer co the cenCer than Talgar has a
more complex rennrding more extrema, more prolonged and resolved record-
ing nn all filtrations except the loweat frequency 0.6 hertz (reCOrdings
with 0.3 hertz filtration frequently turn out Co be unreadable as a result
of the high background). On a frequency of 0.6 hertz the recording of the
Talgar station predominates with respect to intenaity and duration. The
analogous picture can be observed also on other oacillograms of the fre-
quency selection seiamic atation.
Now tet us conaider aome examples of recordinge for which the effect of
the parameter R is excluded, that is, for the two ground stations Talgar
and Ozero the epicentral diatancea are close (Fig 64). The depths of all
centera H=13-15 km, and tlte energy class of the earthquakea K-7.4 to 7.7
vary within their own limits. On all the seismograma the recordinga at
Ozero station turn out to be more complex, more prolonged, less resolved
than at the Talgar station. ~
The recordinge at Ozero and Talgar stations, which are similar with respect
to shape, are encountered rarely, and they are basically characteristic
of the most remote earthquakea. Some examplea of such recordings can be
seen in Fig 65.
The most useful sensiCivity realized at the Ozero station and cloaeneas to -
the basic centers give rise to the recording of part of the signals (on
the average 159;) by only this station (Fig 66). Theae are predominantly
very close shocks with tS_p-1.5-3.0 seconds. Some of the recordings are
characterized by significant amplitudes, at the same time as at other ata-
tiong the usEful oscillations hardly exceed the background (Fig 66, a).
Tlie largest number of auch signals were recorded in 1974-1975 (see Table 8).
Wiien analyzing the shape of the recording of local earthquakes at the
f;round stationa of the test area it was of intereat to compare the record-
ings of the Qarthquakes trom closely located centers (oossibly the same
center) obtained at difEerent times. The selection of such recordings was �
made in Fig 67, The centers of these earthquakes are approximately 27 km
sautheast of Ozero station (see Fig 80, c, d). The depths of centers
H=11-14 km are close. A1l of the earthquakes are characterized by in
practice the same values of K=6.6-7.4. The stability of the shape nf the
recordings at the Talgar and Ozero stationa attracts aitention. ,:n the
deep-well stations the recordings are much weaker, and analysis of their
shape is complicated.
169
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N~N Mal"r a�12"rw
t Y . ~ *,l. .~~J: ll ~dJ~: ~ ~ ~ , ~ , � ~Nlds K�9,J !
~~.-~.~~1, ' ~ i : '�lI. I, f'lM;.?~Jf" j ! 1
1 ~�r ~ ~ ~ . ~
` . ` ~ iLJI
~
' 1 ~ ~ � 1~ . ~
u~ ; t � w(~~~
, a ~l.~ ~ ' ~VVl. , ~t ~'t
i
MlJI IY~6 N~0
'
v/mc Ta.~op (2)

CN~ l~M~T-~qfQ (3)
A M. F4t.
I � - . . . ~
c~~ cs) mo
lV J.V NJWN.....
~ f JQ~:7qt t0h1/p ' lUa , JQP.7f~~t t0~ll"~ b
7pAae~.
. � ~ (2)
.
Wlip!
~ � ~r (4)
' " (6) � ' ' , � ' ~
. , . .
,
. . .
~ :
� � ''''~""I(~ MOtiI/Ir,a - (5)
. ~
. . ' (3) ' ~ , . .
~
(3)
(4)
5)
Key:
1. 28 January 1974
2. Talgar drift
3. Alma-Ata well
4. Ozero
Figure 62. Recordings of local earthquakea for different
epicentral diatances atnd lacation of the centere
closer to the Talgar (a) and Ozero (b) stations
5, Ali well
6. seconds
170
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yr~c i ~f~ :z, ~
ty W.
~kw,?,~~,
!!/n To~top
t2)
NY! NtDJ
.._..m .._00...1 IV.p 1.u
r
r
Figure 64. Recordings of local earthquakea.
Earthquake centers equidistant from Talgar and Ozero atations
Key :
1. 27 August 1973
2. Talgar drift
3. Alma-Ata well
4. Ozero
5. Ali well
6. 10 aeconda
The time intervals between adj acent earthquakes are not the same 2 days,
17 days, 8 months. On the upper two seismograms (an interval.of 2 days),
impressive aimilari:y of the recordings at the same stations is observed.
Not only the low frequency conEiguration of the recording characteriatic
of Talgar station repeats well, but even its complication with high
frequency. The next seismogram was obtained 8 months later, but the
correlation of the recording at the Talgar station is good, juat as before;
only individual high-frequency contractions are distinguiahed. The high-
frequency recordinS of the Ozero station is reproduced worae. It is
possible to proooae that in the segment of the trajectory from the center
to the Ozero station a change in state of the medium took place during this
172
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(6)
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(1~ Y. 79~~e !t ~ I"' t~r. r:~
IV 1/1 ~"'4d'j MNAWAI d P .N10 AiipA
(3)
r
/
' .
7
I . '   Pi~'I  _ n t ~ ~
AAMQ- a�
~
_ ; .
_ ' ~.~...,~,ry~,~ _
11 tl~ ~
~
1�" ~
~
Ore
(5) - " -
.

� . � , />d ~ ~
(6) . _ , . . _ . . ~ ~
Figure 65. Earthquakes with cloae ahape of the recording of
all of the test area stations
Key:
1. 9 May 1974 4. A1ma-Ata well
2. 10 seconds 5. Ozero
3. Talgar drift 6. Ali well
time which was "noted" in tne high-frequency components, at the same time
as on the path of the center to Talgar eithex the medium remained unchanged
or its variation was not reflected in the low-frequency component of the
recording. Actually, between the center and the Ozero station several
earthquake centers occurxed during these 8 montha, and between the center
and the Talgar station they were not observed (see the maps in Fig 80, c, d).
0� course, it is impoasible to exclude the possibility of nonidenticalness
of the center influencing the hip,h-frequency probability recording.
Finally, on the last seismogram for both stations similarity is observed
(in general features) between tbe sfape of the nscillation recording and
the shape of the waves in the first two seismograms at the same time as
173
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.,r........... . t
. . ~ ..a~, r,
....r,.,. ,
:
CN~ AIlMO-Ili~O (2)
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. ~ . . . r~ ~ ~ ~ ~~~.Mti..
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�

� .
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{
~
_ I, �
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.
IM �~~r4M~r!iV:�
~~-yL'''?;JL: r� A M �tJl' tih~ y~1.wr
.
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:
�
' �

~
i~ `
. ~ . . . . .
, .
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/
,
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�
7~SM ~
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,
D.repo (3)
~ ~ A~� �....~w~..~r+.~+� � . ~ . . . ~
�.r~. � ~,1.r.~ . ~
' . . ' �
. . ~ �G.;�.ri~~.~t,
zat. N,t W^
_ ~ . . ~ :
Z Z. N4
(4) ~ _
I~ ~ l, `Mr 1
t I
f
.M '
J P
�
a. .
_
~i~ t~
Figure 66. Recordings of earthquakes recorded only by
Ozero station
Key:
1. 31 May 1973
2. Alma-Ata well
3. Ozero
4. Ali well
the relative intensity of the 2ongitudinal oscillations (and shape at the
Ozero atation) chanRed several times, The last seismogram was obtained
9 days after an earrhquake occurred 60 km to the west (4 January 1975)
whicfi was the strongest during the observation period (K=11.5), which could
be �elt in the condition of the environment and could lead to an increase
in langitudinal wave abaorption. 174
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I N I'm K~x o
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8 ro,. Ixh 1/A
r
. . ~ .
N
Figure 67. Recordings of eazthquakes at the Talgar, A1ma-,Ata,
Ozero, and Ali stations occurring in one place
Deep-Well Stati,ons. Where the shape of the recording of distant eaxth-
quakes at the deep,.well atations is much si,mplez than at the gxound
stations, thi,s is not so obvi.ous for local earthquakes. When comparing
the shape of the recordi,ng $t the deep-well and ground stations for
local earthquakes it is difficult to exclude the effect of the factor R,
for all of the deep-well stations are north, and the majority of the
epicenters are in the south and southeast, closer to the ground stations.
175
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VrhnuenCly the shnreer nnd nimplex .forma oP xecording at the Alma-Ata well
ytntlon rind aqpeclnlly Che Alt well ptntion, ns the moet remote, cnn be
conneceed with Chie (see Vig 62, No 190; Fig 61, No 141),
In C}1e case where itA,ApEt , the rpcordinge of the Alma-Ata and Talger
gearions are comparable ~ith reapect to shapp (see Fig 61) at the same
timp ns the recording of the Ozero etation which was cloaeet to the epi-
center ig the moet complex.
For the wegtern centern RA_AZRO the recordinge nf the Alma-Ata and Ozero
sCgtions turn out to be eimilar with reepect to ahape at the eame time as
the Talggr station, which ia far from the western c:enters is characterized
by a aimpler shape of the recording (see Fig 68, No 186). The recording
nf earChquake No 265 (Fig 68)0 on the contrary, is more complex at the
Talgar stgtion, for the center is close to the seation, and at the Alma-Ata
and Novo-Alekseyevskaya well atationa the recording is simpler and close
with regpect to shape to the recording of the Ozero atation (Fig 62, No 232).
The recordings of more remote earthquakea can turn out to be comparable
witli respect to shape at nll of the test area statione ground and deep-
wel.l (see Fig 65).
For the observations at internal points of the medium, the waves reflected
from the day eurface can iave significant in�luence on the shape of the
recordinga. For the high �requency local earthquakes the interference of
the incident and reflected waves, as the calculatione have demonstrated
(see Fig 59), can lead to the most different effecta, in particular, to the
nppearance of additional exCrema and extension of the recording. However,
- the experimental data frequently give the inverae picture the recordinga
in the wells for local earthquakes, just as for distant ones, are character-
ized by simpler shape. Obviously, the effect of the day surface on the
shape of the incident pulse turns out to be frequently more aignificant
(15] than its distortion by suoerposition of the reflected waves when
_ recording at the internal pointa of the medium.
As nn example let us compare the recordings of the earthquake of 8 June 1968
in the Alma-Ata well and at the Talgar station (Fig 68). On the well
seismogr.m the recording of the S-wave is shorter; sometimes by one or two
exCrema, and it is more complex than the Talgar station.
l.et ug comp.1re the shape of the recordings at different deep-well staCions.
Ttiia prohlem is nat simple, fer in addition to the influe.;1;e o� the factor R,
which is eapecially strong for the northernmost statio cf Ali, anomalous
recordinRs are observed at the station Y- intensive ioW-frequency oscilla-
tions appear in the tail section, The number of recozdings in the
Navo-Alekseyevskaya well is limited. The recordings of all three well
. stations are compared in Fig 53, a, II, The recordings of the local earth-
quakes at the Alma-Ata and the Novo-Alekseyevskaya stations are similar
with respect to shape. At the Ali station in�the tail section of the
recordings low-frequency intense oscillations are recor4ed with reduced
[
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/,~r rf4 1012rm r :,hAf*
,s
~
N i/i
IY�70,! i Nti/
0
N t6S ' �
A'~7,J; N~J1,S~r R-A
. . MI , ~ ; , , ~  . ~
, " .:t~ , ~ r~l ~
. . . . f~~ q
. . ~i
. 6
;
. � ~ ~ , '
t ~ . .
, . � � D ~ ,
~
. , ~ . � � 1 ~ ~
. . ,
......~...i. < N1I<
I{ i k
� . :,r ~ , ; ~ 0
� ~ 2) . . r; ~
. _ . . : . . . 1 ! .
. l~
i86i~ f~s'"' ~ �
. �
~~~1 j � ~ ~ .
, r�c, .
Figure 68. Recordings of earthquakea at the ground surface and
deep-well stations
Key:
1. 10 Marr.h 1975
2. 10 seconds
velocity frequently rommensurate with respect to intensitywith the group
oE S-oscillations (see Fig 648 Fig 68, No 265). On some of the recordings
the intenaity ef the "loop" decreases (see Fig 61, No 157; Fig 62, No 138,
No 190); in rare cases the low apeed oscillations are aLsent (Fig 61,
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Na 141; Fi,g 65), and then Che Ali stati,on is chaxacCerized by the eimpleeC
ehape nf the recordings. It wae nor poseible uni,quely to relate Che
pecul3arities of the recording at the Ali seation eo poaiCion and parametera
of the center R, 0, H. It is only poesible to noCe that the majority nf
reeordings with 1ow-frequency "loop" are caueed by deeper earthquakea
located to the southeaee of the tese areg, and the ahort recordinge are
connected both wieh shallow attd deep centera located eo the northeaet and
eouthweaC.
Table 14
Kome- (3) 4aarora th (9) KPyr,cM
orMCmn ~2 ~
1
ypow. :a ypow. ,p.od,,.. no" n~
0,7 015 : (8)
caotspos (4) _ (5) Ot8/b~? t07MIO.5
(10) P -"Mv
Tenrap
� 24
2,043,0
1,7-3.6
c~ 03"
ie
1,e-4,3
i,s..e,s
(13) M=
8 �
;L,4-8,8
0,8-8,5
(14) Atom"ra
28
2,7-8,8
1.7-7,5
�
(15)
S-swaw
(i~) T.m-ap
'zs .
i,as,d
0,6-3,5
(12) 03qO
, ie
1,0.3,0
, 0,6..3,7
(13) Anx
.a
i.s-s,s
..s,a
(14),Anwa"As.
' 24
1,5-3,2
-3,8
Key:
2.4
0,65
o,es
2,8
0,79
0,?3
8,0
0180
0,80
4.2
0M
0,8?
1,7
. o,so
0.89
1,7
o,as
0,81 �
2,4
-
aei
z,?
-
0081
1. Station 10. P-wave
2. No of average spectra 11. Talgar
3. Frequency, hertz 12. Ozero
4. on the 0.7 1eve1 13. Ali
5. on the 0.5 level 14. Alma-Ata
6. predominant 15. S-wave
7. left slope 0.5/0.7
8, right slope 0,7/0.5
9. Steepneas
*By the predominant frequency we mean the geometric mean of the values of
the limiting frequencies of 0,7 level,
Everything that has been stated about the peculiarities of the shape of
the recording of local earthquakes at the ground and Well st$tions o� the
test area reflects the complexity of the situation and complicates the
solution of the problem of the effect of the reception conditions on the
shape of the recording.
l
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Frnquenc:y CharncCerisrics of the Recoxdings of Locdl EarChquakee and
tixploaions. Let us consider the e�fect o� the observaC3on conditiona on
the frequency composition of the recordings. It wAS reasonable ati firse
Cu analyze the �requency characteriaC3.ca o� the explosion recordinga 3n
Medeo Canyon, which Cook place in practice ae one location, and their
numher was the greaCegt by comparison wi.th other exploaiona. The fre- `
quency selecCive seiamic statiott ogcillograma of 26 exploaiona were
obtained, the energy class o.f which is basically equal to K-6-8. No
dependence of predominant apectral frequency on the claes K was obaerved
in this narrow energy range.
IE we exclude the effect of the epicentral disCances, it ia possible to
expect thatdifferences in the frequency apectra of explosion recordings
at ttie sCationa of the test area are connecCed with the peculiaritiea of
the observaCion conditions.
T}te bASic information abouC the apectra of the P and 5-waves of explosiona
in Medeo is presenCed in Table 14, and the average relative (reduced Co
f=5.1 hertz) frequency-selective seigmic station spectra of these waves
nre presented in Fig 69, a. The spectra were processed by the generally
accepted ptrocedure [35, 58J.
As a result of analyzing the spectral characCeristics, it is possible to
draw the following conclusions.
1. The spectra of the P,wavea of the explosions in Medeo at the different
sCations differ from each other. The differences are observed both
between the spectra of the ground stations and the well stations, as well
as between the individual apectra at the ground stations (Talgar and Ozero)
_ and the well stations (Alma-Ata and Ali). The observation conditions at
the Talgar and Ozero stations are approximately identical, and their spectra
are also similar. The differences which exist nevertheless (at the Ozero
station the spectrum of the P-wave has more gently sloping sides and is
somewhat broader than the Talgar station) can be explained by the fact
[hat the Ozero station is located closer to the explosion point.
2. The spectra of the P and the S-waves of explosions at the Ali and
Alma-Ata well statians are broader and higher frequdncies than at the
ground stations, which is connected with the complete (Ali) and partial
(Alma-Ata) exclusion of the sedimentary series.
3. The spectra of the S,waves of explosions in Medeo at all of the sta-
tions on the whole are simt,lar to each other, especially with respect to
their right slones. In the example of the Scwave spectra it is obvious
that the observation conditi,ons are felt in the frequency characteristics
essentially more than the diFferences i.n distancesl thus, the spectra
of the S-wave at the Talgar and Alma Ata stations located at an identical
distance from the explosions (approximately 16 km) liut under different
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4
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~
af
Figure 69.
Key:
hertz
Qi Z6 I0~/4 (1)
Average normalized spectra of the shift of the
P and the S-waves of explosions in rtedeo (a)
and local earthquakes (b) at the Ozero station
(1), Talgar (2), A1ma-Ata (3) and Ali (4)
conditions, are different from each other. At the same time the spectra
of the S-waves on the recordings of the A1ma-Ata and Ali atations
although located at different dietancea (about 16 and 50 km respectively)
but under identical conditions, are identical.
- In order to study the e�fect of the observation coriditiona on the frequency
characteristica of the recordings of local earthqual:es, more than 40
seismograms were selected for which it was possible to obtain high,quality
frequency selection seismic station oscillograms. For the selected earth-
qual;es the predominant value of K is included within the range of 6.0-7.5;
H=0-15 km, tg_p according to the Talgar station it is equal to 5.0-7,0 sec.
In order to exclude the effect of random factorso average normalized
shift spectra of the P and S oscillations were constructed for all the
stations of the test area (Fig 69, b), An analysis was made of the
amplitude ratio, which does not depend on the signal level -A,fIA5,1 hertz'
The first thing that attracts attention is the anomalously high-frequency
nature of the recordins at the Ali station. This pertains to the P and
the S-oscillations, and it is a consequence of the observation conditions
(it is remarkable that the Ali station usually is removed to the maximum
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frnm the epiccntere), Thie anamaly was obAerved sometimes A18o for
cliHranr aazrhqunkeA. 'Che avoriiRe sper.tra for the xemaininR etatione
(7'atgnrt Ozero, Almn-Atn) ngree wiCh reeppct to ehapet but with emall
diEEerencea nnd more expressed for the P-wave. The spectra of the
longitudinal waves at the Ozero and Talgar atatione are very similar,
and at the Alma-Ata etation they are lower frequency. This is connected
with the fixed aeriea of sedimenes under th3s atation.
The noted apectral characterisCics of the recordinga of the different ata-
tinns are well illustrated by the frequency aelection seismic atation
oscillograms for local earthquakes. Thus, according to Fig 53, c, II,
it is obvious that at the Ali station the maximum recording amplitudea
are noted on the 2.6, 5.1:, and 10 hertz filtera. For the other stations
the relative intensiCy of the P and the S wavea on these filters is much
lower.
' Thus, during the time of the 4-year observatinns from 1972 to 1976, the
= automated stations of the tesC area recorded more than 18,000 earthquakes,
distant, nearby and local, including 978 signals with tS_p,10 aeconda,
which were inveatigated when studying the seismic characteriatica of
Alma-Ata. Of them there were 692 local earthquakes and 286 explosiona.
Among the latter 10% were explosions in Medeo.
More than 85% of all the earthquakes recorded by the test area stations
belong to the fifth to seventh energy classes which are not represenCative for the Kazakh regional station network. The estimate of the energy of the weakest earthquakes recorded only by Ozero station gives a value of
K on the order of two. The minimum recording time of the earthquakes
with tS_p=1.5-2.5 seconds is 13-14 aeconds. Under the conditions of the -
Alma-Ata test area the earthquakes of energy class 6 are representative.
The relief of the day surface has the strongest effect on the structure
of the seismograms. The recordings of the stations located in the
mountains are distinguished by the greatest complexity and 10v resolvabil-
ity. Many waves, polarized in different directions, are recoxded here.
The nonuniformities of the section under the conditions of azimuths of
ground relief can have a strong influence on the structure of the seismo-
grams.
The developed procedure for processing the multichannel seismograms of
centralized radiotelemetric recording considering the spatial arrangement
of the statians in the test area made it possible to determine the hypo-
- centerq of the earthquakes with high accuracy, The study of the peculiarity
of the recordi,ng of explosions, including those occurring in Medeo in
comparative proximity to the locati,ons of greatest concentration of local
earthquake centers demonstrated that the basic criteria for recognizing
explosions and earthquakes are the frequency composition and the shape of
the recording. The local earthquakes can be higher frequency than the
explosions.
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CHAPTER V. OBSERVATION RESULTS
The basic area of work was the equipment-procedural study. The aeismic
regime was studied by the way. However, the reaulte obtained not only
confirm rhe correctness of the developed procedure, but they can be of
independent interesC.
It is appropriate ta coneider the aeismic regime of Alma-Ats in Connection
with the overall aeismicity of Zailiyakiy AlaCau.
61. Seismicity of Zailiyskiy Alatau
The Alma-Ata seismically active region is wholly within the limita of
Northern Tyan'-Shan'. In the north it ia bounded by the Dzhungarskiy
Alatau and its spura; in the west it is bounded by the line from the
city of Tolanak to the mouth of the Kurty River; in the south it is bounded
by the north shore of Lake Issyk-Kul' and Kyungey--Ala-Too, and, finally,
in the east, by the lower courae of the Chilik River. The central part of
the area is occupied by the Zailiyskiy Alatau Ridge, the axial part of
uhich extends in northeasterly direction, reaching the highest elevation
on the Talgar Peak.
The north slopes of the Zailiyskiy Alatau are expreased by low terraced
Eoothills. The foothills make a sharp transition to the Iliyskdya basin
whtch drops with insignificant slope to the I].i River basin.
The north sYopes oE the ridge are cut by the deep transverse slopes of the
following rivers; ,Kastek, Karastek, Kasl:elen, Aksay, Bol'ahaya Alma-Atinka,
Malayn Alma-Atinka, Levyy Talgar, Issyk, Turgen' and the longitudinal
Pravyy Taigar and Asy River valleys, The sauth slope o.f the Zailiyskiy
ridge is di,smembered by short transyerse river canyons, and in the
western parC it belongs to the Bollshoy Kem3,n system; in the eastern part
it belongs to the Chilik River system.
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Figure 70. TecConic diagram of North Tyan'-Shan'
1-- deep fracture zonea: Northern Tyan'-Shan' (a),
Kaskelenskaya (b), Alma-Ata (c), ?.ailiyskaya (d), Kemino-
Chilik (e), Tyupskaya (f), Terskeyskaya (g);
2-- active regional faults; 3-- inactive regional faults
Key:
1. Kurty 7. Alma-Ata 18. Charyn
2. Malay-Sary Ridge 8. Kirgizakiy 19. Panfilov
3. Ili 9. Tokmak
4. Kapchagay reservoir 10. 2ailiyskiy Alatau R3dge
5. Talgar 11. Kyungey-Ala-Too Ridge
6. Uzunagan 12. Chu
i3, Iasyk Kul' Lake
14. Przheval'sk ~
15. Tekes
16. Kagen
17. Ketshen' Ridge - The hyungey-Ala-Too Ridge extends in latitudinal direction almost parallel
to the Zailiyskiy Ridge from the south o'' it. Cts highest point is
- Chotkal Mountain, located to the southwest of tlie Talgar Peak. In the
west the ridge ends up at the Chu River, and in the east it branches into
two parts between which the broad section of the Chon-Aksu valley is
located. The south slopesof the ridge, dz:opping down, end up as the shore
of Lake Issyk,Kul',
The 7,ailiyskt,y Alatau and Kyungey-Ala--Too }tidges, on approaching the more
central section, form a single Kemino�,Chu Plountain complex, to the north-
west of whicti the city of Alma-Ata is loca..ted in the valley of the Malaya
nnd aol'shaya A1ma-Atinka Rivers, To the west and east the distance
betwec:n tlie ridges increases, and the ridges are s pl.it by the two river
valleys of Chon-Kemin and Chi,13k which are elongated i.n the sublatitudinal
direction.
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The baaic large etructuxal elemente of the inveatigated parC of Northern
Tyan'-Shan' are aeparated by deep faults exi,ating since the Paleozoic,
The intensity of the movemente along the faults in Che I aeC stages of
geologicnL development wae the greateet, The echematic of the deep
faults is depicted in Fig 70. The faults cnntrollins the movements of
the inveatigared region muet be considered to be the Alma-,Ata fault with
the Zailiyslciy fault adjacent to iC aeparating Che mountain aystem of
the Zailiyekiy Alatau from the Iliyakaya baein, and the Kemino-Chilik
with the Tyupekiy branching from it. These faults have the greatest extent
and are characterized by eapecially intenae lateat movements along them.
Obviously, an important role in the tectonic development of the region is
also played by the faults of shorC extenC, the aetivity of which is
exhibited in the Holocene.
The differentiated nature of the tectonic movements of NorChern Tyan'-Shan'
m ~the intenae ascending dieplacements of the mountain etructurea and the
descending basins) finds ita reflection in the nature of the aeismicity
of the region. WiCh reapect to level of manifestation of modern weak
seismicity Northern Tyan'-Shan' differs comparaCively little from the
seismicity of all of Tyan'-Shan'. However, againet this comparatively
"quiet" background the largeat seismic disaeters quite frequenCly occur.
Thus, aC the end of the last century and the beginning of thie century
four earthquakes occurred here, one of which (Kebinskoye 1911) ia the
largest; ita magnitude reached 8.44.6. Close to it with respect to
intensity was the Chilik earthquake of 1889. The magnitude of this ahock
is estimated at approximately 8. The weakest, but moat destructive for
Alma-Ata (previously Vernyy) was the Verdy earthquake (1887 and, finally,
the weakest of them, the earthquake of 1938 (M-6.5), the center of which
is located at the confluence of the Chon-Kemin and the Chu Rivera. The
three strongest earthquakes appeared at the earth's surface in sections
of significant extent of residual deformations (Fig 71). All of them have
been preserved up to the present time.
The center of the earthquake of 18$7 was located between the valleys of
the Alcsay and Talgar Rivers [41], Here the earthquake deformationsvere
exhibited most clearly on the Zailiyskiy fault. The degree of these
deformations decreased from Aksay to Talgar.
The earthquake of 1889 was accompanied by large dislocations with a break
in continuity and landslips in the valley of the Chilik River from its
source to the meridional turning of the river to the north [42], The dis-
turbances of the surface and the landslips were also observed somewhat to
the south in the vicinity of Dzhalanash settlement. The eastern edge of
the center of this earthquake has a moxe intense manifestation at ground
surface by comparisan with the weatern edge, After the meridional turn
1Compiled by V. N. Krestnikov, N. V. Chigarev, T, P. Belousov.
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t ~oa � ~ O
� +
I M; ,
1) ~(2) ~N~ ~
~S 3) ~ 117&

(18)
y rw n A S~7)~ C6, . N~t/t
1
(ti)
6) r ~.e 9)
~ ~
/1
no`10 N TO O .
.0 . ~
~ ~ � ~ � ' . .
. r ~ ~ �
~ (11) A~ '
~
Of *t *r 04 *8 06 OF Qf of
Figure 71. Map of atrong earthquakes in Northern Tyan'-Shan'
_ Provisional notation: 1~- K=12; KQ13; 3K-14;
4-- K=15; 5-- Ka17; 6-- K=18; 7~- 1929-1950; 8-- 1951-1967;
9-- 1965-1975; 10 deep faults; 11 regions oF deformation
_ of the day surface
Key: �
1. Kurty . 11, Tezskey-Ala-Too Ridge
2. Ili 12. Lake Issyk-Kul'
3. Kapchagay reservoir 13. Rybach'ye
4. Panfilov 14. Zailiyskiy Alatau Ridge
5. Ili 15. Kyungey--Ala-Too Ridge
6. Charyk 16, Chu River
7. Chilik 17. Uzunagach
8. Ketshen' Ridge 18. Alma-Ata
9. Tekes
10. Przheval'sk
in the Chilik River at the present time no noticeable residual disturbances
of the earrh's surface are vis3ble, but it must be noted that the isoseisms
of this earthquake have clearly expressed northeasterly strike. The region
of force 9 tremors encompassed a significant area in the eastern part of
the Alma-Ata region. The force 8 isoseism extended from Dzhungarskiy Alatau
185 `
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in the nnrtheast to the xouth ahares of Lake Ieayk-Kul', and from Chundzhi
in the eust to Talgar in the weat. The axia of this recording is
etretched Co 260 lan in rhe northeasterly direcCion and 160 km in the
AublatitudinAl direcCion [31].
The Kebin earthquat;e of 1911 exceeded all of the preceding ones with reapect
to force [7]. The most clearly de�ormation procesaes were expresseci in the
Chon-Kemin River valley over its entire extent and on the Tyupakiy fault
from where it branchea off the Kemino-Chilik fault to the northeastern ahore
of Lake Issyk-Kul'. Significant deformationa are also obaerved now in the
eagtern section of the entire center regi.on of this earthquake. In addition
to the huaic diaturbances along the faults, deformations and landalipa were
obaerved on the Tyungey-Ala-Too Ridge and the Zailiyakiy Ridge. Thus, the
entire southweetern part o� the investigated region of Northern Tyan'-Shan'
was encompassed by this earthquake, The rotation of the center of the
earthq uake from aublatitudinal in the Chon-Kemin valley to southeastern
along the Tyupskiy fault ie a highly characteriatic and important chsracter-
istic of it.
The Kemin earthquake of 1938 had a small region of, force-9 tremor at the
confluence of the Chu and the Chon-Kemin Rivers [10]. Its force 8 iso-
seism was observed only in the weaterly direction, and the force-1
encompassed a significant territory af Central Kirgizia and the entire
region of Northern Tyan'-Shan' of interest to us.
The noted earthquakes are noC the only ones according to the catalog data
[43]. The earthquake of 1807 is known in the Medeo Canyon. There ia
undefined information about the earthquakes of the 18th century.
K. I. Bogdanovich [7] reports a deatructive earthquake in the 9th century.
The geological data indicate the seismoCectonic nature of the rock-dammed
- lake Issyk in the upper course of the Isayk River. There are substantiated
fieological data on the seismotectonic processes in the Kirgiz Ridge.
At the southern boundary of the investigated region 18 km east of
Przheval'sk the Sarylcamyahskoye earthquake occurred in 1970, the magnitude
of which was 6.8 [13].
A brie� description of the strong earthquakes in Northern Tyan'-Shan' -
indicates that their centers have significant dimensions, and the residual
Phenomena are in the majori,ty of cases coordinated with the zonea o� deep
faults controlling the tectonic li:fe of the entire region. In addition,
some of the peculiarities of the shape of the isoseisma of these shocks
indicate tnat the centers of these eaxthquakes can he coordinated not only
with the explici.tly, expressed fAultst but they are also connected with
the newl; formed tectonic zones,
These data indicate that both with reapect to strength of the known earth-
quakes and with respect to their recurrence rbte, tha, region of Northern
Tyan'-Shan' muat be considered one of the potenl-ially most dangerous
regions of the USSR in seismic respects. _
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An instrumenC study of the earthquakes of Northern Tyan'-Shan' was started
in 1929 the time of opening several of the seiamic sCaCiona in Centiral
Asia (Alma-Ata, Andizhan, Frunze, Samarkand) to aupplemenC the Tashkent
station exlating at the Cime of B. B. Golitayn, This quite meager network
- equipped wiCh Nikiforov aeismagraphe permitCed deCermination of the
poaition of Che epicentera of Che earthquakes correaponding to clasaes
11-12 with respect to energy K, although with large errors.
" Fig 72 showa a map of the epicenter Por the period.from 1929 to 1950 when
the station network did noC change. In spite of the limited poasibilities
of the first network, it ia impossible not to noCe the fundamentalness of
thia period of instrument obaervAtions giving the firat clear concept of
the nature nf the seismicity of all Central Asia and, in particular,
Northern Tyan'-Shan' [53].
(1) "
lwr.~..~a.....e. (2) ' w+
T~ry11+~1Mw
ON Q+l ~n ~u
~ 14 ~16 ~ (4)
� n ~e ~ ~
44 � O fl~w~r~
3 ~
N
1
(7) , ~6) I O 0~ ~ (4)
O ~ AM �ATA ~ ~
MN
{ ][RJ M Y _m N39 O(B r.~ . 1~
11 IQ ! 1~ 1 ~i ~ nOM~s~NeM .
(9)
~E ~ � p
r r~ c c (14) 0 O
15) .
0
o
Y K... 17 a~
0
~60
b
Fi.gure 72. Earthquake epicenter map �ar 1929-1950
Key:
1. energy class 5,, Kapchagay reservoir 9. Kir!'iz P.idge
2. Taldy-Kurgan 6. Alma-Ata 10. Zailiyskiy Alatau Ridge
3. Pnnfilov 7. Chu 11. Rybach'ye
4. Ili 8. Frunze 12. Issyk-Kul' Lake
13. Przheval'sk 14. Terskey-Ala--Too Ridge 15. Naryn River -
16. Ntlryn! 17. Chatyr-KQ1' Lake
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FAR OFFICIAL USE ONLY , - The year 1951 was the turning point in the development of aeismological
studies o� Central Asia and especi$11y Noxthern Tyan'-Shan'. Beginning -
in thar year a new, significantly broader network of atationa began
operatian in Asia, and Academici,an G. A. Gamburtaev organized the regional
network of etations of the Earth Physica InsCitute of the USSR Academy of
Sciencea in Tyan'-Shan', permitting determination of the epicenters of
earthquukea with quite high accuracy, in individual cases also their
depths were determined, and mak3ng it possible to compile the energy -
classification of the seismic shocks [9]. This neCwork included the
following stations: Ili, Talgar, Fabrichnaya, Kurmenty, Chilik. The
Alma-Ata atation operated as before. The Przheval'sk and Rybach'ye sta-
tions aupplemented the network on the south. As a reault, sixth and
seventh class earthquakes began to be recorded, although from the point of
view of representativenesa, the exiating observation-system for these
classes of earthquakes was atill insufficient. The increase in number of
stations up to 1961 and their reequipment with the new SIQrt devicea insured
a further increase in accuracy of determining Che geometric parameters of
- the earthquakes and also the energy classes.
Beginning in 1969 all of the aeismic operations in Northern Tyan'-Shan'
were transferred to the Geological Institute of Che Kazakh SSR Academy
o� Sciences, and in 1976, to the Seismology Institute of the Kazakh 5SR
Academy of Sciences where the development of the seismic operations in
Northern Tyan'-Shan' is continuing jointly with the Seismology Institute
of the Kirgiz SSR Academy of Sciences. _
The maps of the epicentera in Figurea 11-74 give an idea of the aeismicity
of Northern Tyan'-Shan' in the vicinity of Alma-Ata for different time
intervals. Figure 71 showe the epicentera of the strongest seismic shocks
from energy class 12 and up during the entire period of inatrument obaerva-
tions. A complete idea of the nature of the seismicity of the region is
given by the map of the epicenters of energy classes 9 and 10 (Fig 73),
inasmuch as these classes are the most representative for the entire
observation time. However, it is necessary to consider that the accuracy
of determining the epicenters before 1951 was essentially lower by compari-
son with the subsequent years.
In Fig 74 it is possible to isolate several localized seismic zones. First
of ull, let us note the seismically active zone extending from the sAUrces
of the Chon-Kemin and Chilik Rivers along the southwest slopes of the
Ryungey-Ala-Too Rfdge, This zone approaches the city of Alma-pta with a
small turn somewiiat to the west and breaks off shaxply. Then in the
western part of the region, pximarily along the noxth slopes of the
Kyungey--Ala-Too Ridge to the Chu Riyer a seismic belt is traced which has
compar;titi.vely low activity, From the northeast corner of Lake Issyk--Kul'
to the epicenter of the earthRuake of 1889 thexe is a xegi,on of highest
seismic: activi,ty, The dimensinns of this zone are not great, but the
greatefit density of earthquakes in Nortnern Tyan'--ShanR is obaerved within
its limits. '

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From tho epicenter oL Che ClrLlik earthquake of 18$9 two somewhat worse
l.acntecl directions of propagation of, the epicenter9 are noCed: uE;e of Chem
coincidea closely wiCh the Chilik River valley after its turn in the
meridional direction, and the other has a northweaterly strike in the
direction of the mouth of Che A1ma-ACinka River. It is possible to note
small meridional accumulation of epicentera in the region along the
- Turgen' River in the cenCral part of the first of the investigated zones.
Within the limits o� the remaining part of the territory the epicenters
are scattered quite randomly, and there is an insignificant number of them.
7e
p 0 y40 O ~ 0 EPO CA
Cl) 0 0 ~
N
O
v. 0
O 0 �
(4 ~
0 0 ~ a�
y~ O �3) ~ 1 IIe9r. iA�J
~(O AIIMA�AT(y ~ � C///]
, U
O
~ O ~
~ CS~~, ,r - ' " r a ' ~
N

~

~ '
/
~
O

~
~ ~1911r. _ _ h. O
�
'
(6)
Pr6*4b� ~
~ r ---M~
"
(Dl ~f
7S e ~s.~
~
Figure 73. Map of eaxthquake epi.centers for 1951-1967
The epicenters with Kz-,9 (1) and K=10 (2) �or 1961-1967 are
crosshatched,
Key:
1. Ili; 2. Kapchagay reservoix; 3, Alma-Ataf 4, Charyn; 5. Zailiyskiy
Alatau Ridge; 6. Kyungey-Ala-Too Ridge; 7. Rybach'ye; 8. Lake Issyk-
Kul'; 9. Przheval'sl:; 10, Chilik.
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bF LI tGE I NDUSTR I AL CENTERS
4 APRIL 1979 , .
~ 3 OF 3
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P'OR OPFICIAL U5E ONLX
LJ

0

0~
C 1, yo
GP o e
w
Z~A&A 6 Q
~ e
,
0
~
~ ~10 O
~
�
0
0
o
(3)
"
�
o p
8
o(6) ~
o~ 9)o CSj.
`
. 0
O
0 0 0
O 0
o p
0 10)
A,At
0
p~ o
p
4u~~o W
(11~ o
�
w 0 ~
00 0 ~
t ~~ro .
0
06~ 0 00 ot
~
0
O O
0
0
O

00 ~
~ � ~ 3
~ 19 )
08 0 ~ d 0
0 ~
0
~0 o
Of p�
O�
ON O u
~n
Figure 74. Map af earthquake epicenters from 1965 to 1968.
The numbers on the earthquake symbols indicate the energy clasa
K.
Key:
3. 11i; 2. Altyn Emel' Ridge; 3. Ili; 4. Kapchagay reservoir;
5. Charyn; 6. Kaskelen; 7. Talgar; 8. Turgen; 9. Chilik;
10. Alma-Ata; 11. Talgar; 12. 7.ailiyskiy Alatau Ridge; 13. Kyunge/-
Ala-Too Ridge; 14. Chon -ECemin; 15. Tokmak; 16. Chu; 17. Rybach'ye;
18. Lake Issyk-Kul'; 19. Keqen
r
v
On ttie map of the strongest shocks (see Fig 71) on the whole an analogous
pic�ture of the earthquake diseribution is observed, The moat active is
the cnrthquake belt coincidir.g with the Kyungey-Ala-Too Ridge and ita
poK! tion in the direction c+f Alma-,Ata. Some "fuzziness" of the observed
Jistrihution ot ttie epicenters is explained by the lower accuracy of
determination for 1951. Ic is necessary to pay attentlon to the fact that
Rtronger and stronger shocka in recent vears have occurred in the eastern
: parts cif the region alonq the line coinciding with the meridional direc-
tions of the Chilik River.
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Finn]1y, lot us dineuen the map in F!,R 74 conoeruCted by the observarlnn
data f,or 1.965-1968 eeparaCely. Durtng th1s zimp the complex eeismolngiral
pxreditian in Northc-rn Tyan'-Shgn' openc�d up a number o� tempornry etn-
ttorin which mndp it rogAible Co increasc the accuracy of determining the
epicenterg gnd their depthe (Fig 75). Frrnn investigaCion of Fig 75 it
followg that the majority of the earthquake centers of low energy c1asseg
gre AgBdCiAtP.d wieh the narrow range of depehe from the first kilometers
eo 12. T'he deeper centers are encountered significantly more rgrely
(acedrding to the data for recent yeara). and in the majority of cases
they belong to the etrong seismic ghocka nf clasa 11-12.
In Fig 74 the basic nature of the earthquake distribuCion ig analogous to
the earthquake distribution on ttie preceding mapA. Nevertheless, it is
possible to note some characteristic features. In the west two clear beltg
nf epicentera of nnrthwesterly gtrike are isolated whirh intersect the
deep belt zones. The basic number of earthquakes in this map, the region L
of propagation of which occupies a eignificantly greater area, belong to
energy class 7. Beginning with energy class $ the earthquakea are located
- ncar the bagic seismically active zones (aee the beginning of thig item).
- The "contraction" of the earthquakes of stronger clasaea into narrow zanes
is 7 quite characteristic feature of the manifeetation of seismicity.
Thus, tlie geiemic material indicatea that the modern :einmicity appears
quite stably in different obaervation times, and the use of weak earthquakes
_ to isolate the seismically active zones turns out to be juatifiable in
spite of the high degree of "diEfuaion" of the epicentera of the weakest
shocics.
On all of the maps of the epicenters it is obvious that east of the city
' of Alma-Ata on the Alma-Ata and Zailiyskiy faults no r.learly expressed
grouping of the weak earthquakes is detected althoug~i the strong earth-
. quakes of the past were connected with them.
The region of increase in modern seismicity is closel;i connected with the
sections within the limits of which the disastrous earthquakes at the end
of the past century and the beginning of this century were atrongly
exhibited. The available material does not permit a definite conclusion
to be drawn about whe[her the modern weak activity is aftershock activity
of the strong earthquakes of the past or the zones isiilated with respect
to weak seismiciry will be future locations of strong earthquakes. Never-
theless, the fact that the seismic activity of recent years is gradually
inrreasing in the eastern part of the region (on the tneridian of the Chilik
River) deserves fixed attention, The experience of studying atrong earth-
quakes in the different seismically active regions of the earth indicates
that the Atrong earthquakes occur nost frequently againat a backRround of
a general rise in activity of the regton adjacent to the center of a strong
shock although before the shock itself on this background uz increasing
activity weakening of the seisml.c aetivity can be observed.
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Q

~ f o (P. ` O

8 ow~
Ce ,d O .
. rs p ~ 0 O
rt '
b -
. ' o ~ m-
J('~b ~ ~tr3#o~~ d
~o~r
v
Of
~o o~o o a,
o,
u . 010
i t0 vOK~ O n-
Figure 75. Diagram of the dietribution of the depthe of the
earthqueke centers in the directions from the
northeaetern corner of Lake Isayk-Kul' to
Alma-Ata (a) and to the epicenter of the earth-
, quake of 1889 (b)
Cey :
. 1. energy class

� s A is A
_ Figure 76. Recurrence rate of the earthquakes of Northern Tyan'-Shan'
1-- 1929-1950; 2-- 1951-1961; 3�- 1962-1967; 4-- 1972-1975 (RTS)
n
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I
Figure 77. Benioff graph for Northern Tyant-Shan'
Key:
1. years; 2. j aijles
Let us consider the grapha of the recurrence rate of earthquatces for
different times of instrument observations (Fig 76). The period from
1951 to 1961 is marked by increased activity by comparison with the later
times. During this period the activity A10 reduced to an area of 1000 km2
and the time interval of 1 year had a value of 0.2 for an anqu:ar coefficient
of the slope of the graph Y-0.47. The next time interval of 1961-1967 has
A10=0.1, and the slope of the graph Y-0.55. 7'he increase in the slope is
connected with general attenuation of the activity for the 1962-1965
period. During this period the number of earthquakes of energy classea 9
and 10 was mininww 1 for the entire observation time. The later time interval
of 1968--1972 (not presented in Fig 76) is similar with respect to level of
activity to the preceding one, Y=0.5 [55, 56]. A comparison of the graphe
with the radiotelemetric syatem data (RTS) of the observations in recent
years indicates that the graph of the recurrence rate 4 turned out to be
somewhat higher with respect to activity level, A10-0.13, and the angular
coefficient of the graph Y-0.46, which is connected with general Weak
increase in activity of Northern Tyan'--Shan' in recent years. It is sig--
nificant tha[ the weak earthquakes of sixth to aeventh energy clasa are
indicated with a common behavior of the recurrence rate graphs in the
preceding years. This fact justifies the study of the characteristics of
the region with resnect to weak seismicity, and the relation of the weak
earthquakes to the atronger ones (K-10-12) can indic$te the nature of the
activation of the region in the future.
The graph for the isolation of seismic energy of the region o� Northern
Tyan'-Shan' is presented in Fig 77. On construction of i[, the assumption
was made that during the periods of weakening of the seismic activity
oi the region the course of the energy release differed little from that
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observed by the instrument datx �or the period since 1929; the energy of -
the seiemic shnck of 1807 was npproximately ~he same 4s the earthquake
of 1887. From the graph it is poes~,ble to draw the conclueion that the
relative quiet in the seiemic activity observed in recenr yeare muat be
replaced in the near future by e3,gnificantly growing acCivity. The gvail-
able time reserve muat be apent on the development of more detailed geo-
physicgl and seismological operations in order ro predicC the time of a
possible strong shock. On2 of the phases of this work is the radio- `
telemeCric recording system. -
42. Seismic CharacterisCics of A1ma-Ata
The Aima-AtA tPat area is in a seiemically active territory which has been
studied by aeismologista for a long time. The most complete information
~ an the seiemic conditiona of the entire region and also the A1ma-Ata
- seismically active region for the period from 1951 Co 1967 were obtained
as a resulC of the work ;,t the complex seiamological expedition of the
Earth Physica Institute of the USSR Academy of Sciences for the period
from 1966 to 1972 the Iliyskaya expedition, and in recent years, the
Institute of Geology and Ceophysice of the Kazskh SSR Academy of Sciences.
The specific nature of the obaervationa of the test area of highly sensi-
tive (even in the territory of the city) sutomatic atations with radio-
telemetric multichannel recording and a united time service inaured more
complete recer.ding of the weak ahocks and higher accuracy of determination
of the position of the centera of the local earthquakes in this area
(+1-2 km) at the same time as in the preceding papers the accuracy of
determining the position of the epicenters and the depths of the centera,
as a rule, did not exceed +3 to 5 lan. This made it poasiblp to atudy the
time-space laws of the distribution of the weak loca' I earthquakes in a
very local region adjacent directly to the city of Alma-Atn wliich is
impossible to do by the regional network observations.
Let us proceed with the discussion of the results obtained by the observa-
tion of the seismic conditiona for the period from June 1972 to July 1976.
Wlien studying the seismic regime, in addition to determining the spatial
position of the earthquake centers (the construction of the epicenters)
estimates were also made of the mean recurrence rate of the earthquakes
and its variations in time for the area as a whole.
Cpicenter Mara. The maps of the epicenters reflect the spatial position of
the centers in the investigated region, In order to construct maps uf the
epicenters under the conditiona of the test area, the fixed energy class
of e:trthquakes is representative, for the epicenter distribution does not
depend on the location of the atations for it, The epicenrers of the
fifth energy class earthquakes are basically constructed by the two southern
stations of Talgar and Ozero; for thero tg~ uaually is 3-5 seconds, These
earthquakes characterize the seismic conditions in a radius of 25-30 km of
the Talgar and Ozero stations.
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The depths of the centezs are reckoned from the reducCion line (aee Fig 41p
a). Their gradation on the epi,center maps is given every 10 km; on the
depth maps it is given every 5 lan. The maps of the epicenters are pre-
aented both wiCh respect ta years and for the entire observation period.
The center depth map wgs compiled aeparately.
Over the exCent of the entire period of insCrument observation from 1929
to 1967 according to the data from the complex seismological expedition
and from 1966 to 1971 according to the reaearch data of the Iliyakaya
expedition with the Zemlyn cyre equipment [3, 50, 54, 55], the 2ailiyskiy
- and Kungey Alatau region appeared to have the same seismic activity.
rig 78 ghows a map of the epicenters of the nearby earthquakes of the
- Alma-Ata seismicnlly active zone for 1966 to 1971 from reference [54].
The territory that we investigaCed is outlined on it. The reaulta of these
~ studies are of inCerest as directly preceding our obaervations in the
radioCelemetric test area.
As follows from investigation uf Figures 78 and 79, the epicenters of the
earthqunkes in the inveatigated territory are distributed highly nonuniformly.
The greateat density of the epicenters of all the energy clnsses on both
maps is observed south of the test area. This is the central part of the
Zailiyskiy and Kungey Alatau Ridgea.
A line running through the sections with increased density of epicenters
according to the 12-year observations of the complex seismological expedition
(1956-1967) and also the belts of high seismic activity according to the
data of reference [3J is plotted on Fig 79. Accarding to our data, it is
possible to rezlize a more detailed breakdown of the region of High seismic
activity and locate the individual sections of concentration of the earth-
quake centers. We have provisionally isolated three zones of high seismic
activity. Let us call them the "western" cone, the "central" zone and
the "eastern" zone.
The "western" zone oF concentration of epicenters extended in the form of a
strip with a width not exceeding 20 km in the southwesterly direction from
Alma-Ata is more clearly outlined (it is also no�.ed in Fig 78). The earth-
quakes are observed here in a wide range of energy classes, including K-9,
10 and 11. The western zone in the southwest ends with the epicenter of
the strongest earthquake during the enttre observation time in the test
area with K=11.5 on 4 January 1975. The direction of the strike of the
strip forms a small angle with the direction of strike of the Alma-Ata
and 7,ailiyskiy zones of deep fractures (Fig 79),
The second zone the central zone K- is separated from the first section
hy reduced seismicity; this is a section of maximum concentr.ltion of epi-
centc�ra of all energy clagses. It ,'.s located to the vouth and southeast
of the stntions of the test area and it is associated ;oith ttie central part
of the 7,ailiyskiy and the Kungey Alatau Ridges, The zone does not have
a clearly expressed direction of strike. In the south It is surrounded by
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� ~r

Figure 78. Schematic of the epicenters of nearby earthquakes of
the Alma-Ata aeismically active region for 1966-1971
[54]
Provisional notatton: 1-- deep fracture zones penetraCing into
the mantle (a) and into the basaltic layer (b); 2-- deep fracture
zones renewed in alpine time; 3-10 epicenters of earthquakes
of the following energy classes: 3-- fourth, 4-~ fifth, 5--
sixth, 6-- 9eventh, 7-- eighth, 8~- ninth, 9tenth, 10
cleventh; 11 epicenter of the disastrous earthquake; 12-16
locatian of hypocenters With respect to depth in km; 12 to 101
13 11-20, 14 20~300 15 more than 30, 16 depth not
de[ermined.
The fracture zones (the mimbers in the figure) are as follows;
1-~ Taukumskaya, 2-.- Central Kazakhstan, 3-- Bakpatinskaya,
4--- Yuzhno-Dzhungar9kaya, 5Sarykumskayai 6�-.� ALtyn-Emel'skaya,
7-- DzhaZair-Naymanskaya, 8-- Chemolganskaya, 9-. Severo-Tyan'-
Shantskaya, 10 Chiliko,Keminskaya, 11 r- Severo -Isayk-Kul'skaya.
[See key an following page]
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~ (Key to Fig 78]:
_ a. Ballihash block; b, Taukunskiy block; c, Chuiliyskiy block;
d. Moyunkunekiy block; e, buzhungarakiy block; f. Koskudukskiy
block; g. Targalakiy block; h. Chilikskiy block; I. Chuyskiy bYock;
J. Alma-Ata; k. Zailiyskiy block; 1. Kungeyskiy block;
m. Iasyk-Kul'skiy block
a region of quite sharp reduction in seiamicity (at a distance of 40 to
- 45 km south of Ozero atatton) although the earChquakes wiCh K>6 would
have to be recorded by the Ozero, Alma-Ata, and Talgar statione. To Che
east the densiCy of the epicentere decreases gradually, and the outline ~
of the zone is blurred. i)n the whole rhe strike of the zone close to `
latiCudinal which matcheg wSCh the aCrike of the mountain ridges in the
general acheme of the tecCOnic atructure is noCed.
The section with three zones of deep fractures joined is characterized
by the greatest activity: Severo-Tyan'-Shan'skaya from the west and the
Kemino-Chilik and Tyupskaya from Che east. Within the boundariea oE the
_ zone there are tcoo centery of disastrous earthquakes in the past: at the
southwest extremity, the most serioue disaster in the world, the Kebin
earthquake af 1911 (MQ8.7), in the central part of the zone, the
Vernenskoye earthquake (Mn1.2). The zone spreads to the east, and the
epicenter concentration increases.
The third zone of clustering of the epicentera is located on the eastern
edge of the region of investigation. It separates the strips of retatively ~
low activity which are less clear in the southeasterly direction from the
"central" zone. The position of the epicenter concentration belt agrees
generally speaking with the zone of high aeismic activity isolated in
reference [3]; it is true tYkat the epicenters are shifted somewhat to the
east. The denaity of the epicentera in the zone is not very high. It
increases in the southern part of the zone in the eastern spurs of the -
ZailiyAkiy A3.atau. In this zone the e{ghth energy class earthquakes are
concentratea to a hi�her degree than ttll the rest (especially in the south).
This is partiully connected with the remoteness of the zone from the station
network.
tJhen investigating the summary map of the epicenters (Fig 79) the complete
absence of centers north of Alma-Ata and Zailiyskaya fracture zonea is
noticeable, indeed even in the central part of the zone. This fact was
not noted earlier (see, for example, the map in Fig 78). The high accuracy
of the construction provided by the radiotelemetric recording made it
possible to locate both the xegions of accumulstion of centers and the
aseismic regions,
Activity of Indi,yidual Sei,smi,c 2ones in Time, The annual :paps for 1973,
1974, and 1975 and the semiannual maps fox 1972 and 1976 give qualitative
representations of the variation In acti,vity,,of the investigated region on
the whole and individual zones of it in time, From Fig 80 it follows that
the migration of the centers in time and in snace ts significant. This was
alsa noted in a number of other papers j3, 54, SS]. The activity of the
aones is manifested differently in time.
197 ,
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J
Figure 79. Summary map of the epicenter according to the �
observation data in the Alma-Ata teat area for the ~
period from 1 June 1972 to 1 July 1976.
Provisional notation: 1-- deep fracture zonea: Severo-'Tyan'-
Shan'skaya (a), Alma-Atinskaya (b), Zailiyskaya (c), Kemino-
Chilikskaya (d), Tyupskays (e); 2-- zones of high seismic
activity according to !-'~e data of [31; 3-- line passing through
the sections with increased density of epiccntera fo�r 1956-1967
according to the data of the complex seismolof;ical expedition;
I^I,, II-II', III^III' axes of the Rtrips for which the time-
space laws of the earthquake disttibution were analyzed.
Key;
1. Energy class; 2, K not determined; 3, depth; 4, not determined to
10 11-20 21-30; 5, K,:skeleni 6, Alij 7, Talgarf 8, Issyk;
9. K.zlchagay reservoir; 10. Novo-Alekseyev,icaya; 11. Aa,ma-,Ata;
12. Talgar; 13, Ozero; 14. Chiliki 15. Zailiyskiy Alatau Ridge;
16. Kyungey-A1n-Too Ridge; 17. Lake IsaykrlCul'.
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In the second ha1� of 1912 (k'ig 80, a) the seiamic activity is low, -
The acaumulat.tons of the cenCera are observed in Chree azeas; eauehwest
n� A1ma-Ata - the grea,teat concentx$tion in the "western" zone; south -
n A1m.-,Ata' in the azea of the "central" zone where two earthquakes
of energy class 9 were recorded in di,rect proximity to the city, one of
them was fe1C as a force 3 Co 4 earChquake, and in the eastern spure of
Kyungey-Ala-Too Ridge where the accumulation of epicenters ia associated
wiCh the Tyupskaya deep fracture zone. An earthquake wi.th K-9 was
recorded here. Tn the eastern zone only individual earChquakes were
observed, one n� them with energy class 10 on 4 November 1972.
' In 1973 (Fig 80, b) the aeismic activity of the area increased signifi-
cantly basically as a result of the weak earthquakea of the sixth energy
_ class and lower. The number of earthquakes of energy class 9-10 decreased
from 8 in 1912 to 3 in 1973.
The seismic activity in the "western" zone and in the vicinity of the
'Cyupskayu fracCure zone was reduced aignificantly. South of Alma-Ata,
no earthquakea were observed. Then the "central" zone of Zailiyskiy and
Kyungey Alatau became active. The high concentraCion of epicenters here
encompaesed a large territory of latitudinal strike. Two energy class 9
earthquakes occurred. A separate group of centers appeared east of the
Tulgar station (by 25 to 30 lan).
Fina?ly, the seismic activity of the eastern zone increased, in the northern
part of which an earthquake occurred on 24 January with K=10, the only one
in 1973.
In 1974 (Fig 80, c) high seismic activity remained in the region, but the
_ internal structure of the epicenter distribuCion changed. Again the
western zone became active. An earthquake of energy class 10 occurred
tiere on 6 May. Near Alma-Ata a small accumulation of centers of weak
- earthquakes wns obaerved (46). The concentration of the centers in the
central zone did not decrease. Only the configuration of the area of high
seismic activity changed somewhat it moved toward Alma-Ata (close to
Ozero station), growing in the southwestern and northeastern directions
where it encompassed a group of epicenters to the southeast of the Talgar station. In the centrai seismically activa zone an earthquake occurred on
27 April with Kl10, one out of three in this year. The "eastern" zone
became ac[ive in the soutt;. An accumulation of centers with K=8-10 was
observed here (an earthquake with Ka10 occurred on 31 December) characterized
by shallow depths of occurrence.
6y the epicenter map for 1975 (F1g 80, d) 1,t is possible to determine some
decrease in seismic activity in the "central" zone and in the southern part
of the "eastern" zone, The activl,ty of the "western" zone remained. On
the southwest end, at the yery beginning of the year (4 January), an earth-
quake of enzrgy class 11 occurred (Km11.5). Two months later in the oppo-
site, northeastern edge of the "Westernv zone an earthquake was recorded
with Ke9, one out of three in that year, and then an earthquake with KQ8.
199
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Figure 80. riapa of the epicenters for the period of 1 June to
31 December 1972 (a), for 1973 (b), 1974 (c),
1975 (d), for the period from 1 January to 1 July 1976
(e)
Key:
1. energy class 8. T$lgar 15. Kyungey-
2. K nut defined 9, Issyk Ala-Too Ridge
3. depth 10. Alma-Ata
4. not de�ined 11. Talger
5. to 10 12, Ozero
6. Kapchagay reservoir 13. Zttiliyskiy Alatau
7. Kaskelen 14. Chilik
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Figure-80 [continued]. The numbers near the epicenters are
the order numbers�of the earthquakes in the catalog (Appendix I)
Key :
1. Kaskelen 8. Ozero
2. Kapchagay reaervoir 9. Zailiyskiy Alatau
3. Ali 10, Chilik -
4. Talgar 11. Kyungey-Ala-Too Ridge
5. Isayk
6. 41ma-Ata
7. Talgar
In the central zone the configuration of the area with maximum density of
the epicenters again changed i,t extended i.n the latitudinal direction.
The group of epi,centers in the eastern part of this zone between the
- Zailiyskiy and the Kyungey Alat$u T:idges was singled out Where dt the end
of the year twa earthquakea of energy class 9 occurred. A small group
of epicenters has been observed in the northern part of the zone near
Talgar station.
201
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Figure 80, c L'continued].
Key:
1. Kaskelen 7. Talgar
2. Ali 8. Ozero
3. Kapchagay reservoir 9. Zailiyskiy Alatau
4. Talgar 10. Kyungey-Ala-Too Ridge
5� IgeYk 11. Chilik
6. Alma-Atu
The seiamicity of the "eastern" zone$ 3n contrast to the preceding year,
is very weakly exhibited, including in the active southern part.
During the first half of 1976 (Fig 80, e) a clear drop in seismic activity
is observed. Although the map was compiled by the observations for only
the firat half of the year, the decxease in activity is obvious. This is
especially noti,ceable In the area Frl.th the usual maximum deneity of the
epicenters - to the south of the test area,
202
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,S�PIt , n r
, ~
t_ -
3 ~
(x-p-
~ . ~
(1)~~'~ ' (4 )
~
(6)
H0n0�A NCssiCNsII
Asra�Ata ' si0
79J~3I9 Tig~J ~ 4 311 820
L~
964 263 ~76 ~791
?ap  260
0911 ~ 0960 � 4d6
l ~e~ A A t ~ r
21e ~;loo 317 t)a��aee 9w5 A ~ yra.. 2e1
K900 294 307Q267 329 309
*2eo aoa~ *~07 S 3I3 480~733 2e9 334 (12~)
� 4796~ 2a2+~s~~~sii�~ro 23aa~ 0 i~aos
A ~ei~r2
33ZZi7 314 3:4Q t:ZpB ~Y ~
Y70~ 7B~ C N 3~0 3489D7 ~398 321 320
J/ N ~ p 7953 4~:5 :1319 ~304 . 786 L3 *471
(10) 7930316 295 r E 1 #315 jA- T 0 0
p M ~see
~
f� ~1~ - t
x - - -
�
� -b =
0=-8
Figure 80, d [continued)
Key:
1. Kaskelen 9. Ozero
2. Ali 10. Zailiyskiy Alatau
3. Talgar 11. Kyungey-Ala-Too Ridge
4. Issyk 12. Chilik
5. Kapchagay reservo{r
6. Novo-Alekseyevskaya
7. Alma-Ata
8. Talgar ;
Out of the highly lctive broad central zones (accordi,ng to the obaervations ,
of 1973--1975) a small chain of epicenters remained in the headwatexs of the
Chilik River in 1916. The "western" zone was represented by .four earth--
quakes on the northeastern li,mb,
- The strongest of the earthquakes recorded du;-ing this 6-months period
included one with K-9 and two with Ke8 they were concentrated in the
203
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~ ,
i ' ~ .
. . c3,t
ALZ) ~ ~
 C6, -'i~4) . , '
~r~
, ' C~ "
o~~
T
. pwN / yu.~
(9) (12)_
~m s'�
A ' r � � ~
. (10) i *ft, ~~u
. �
~
. - - - _y_.._i=
Figure 80, e (continued)
Key:

Keekelen
9.
Ozero
2.
Ali
10.
Zailiyskiy Alatau
3.
Talgar
11.
Kyungey-,Ala-Too Ridge
4.
Issyk
12.
Chilik
5.
Kapchagay reservoir
6.
Novo-Alekaeyevskaya
1.
Alma-Ata
8.
Talgar
southern part of the "eastern" zone, A small group of epicenters Wae
located
by itself in this zone northeast of the Novo-nAlekaeyevskaya
station
. An anelogoua group was
obaerved
in 1974,
204
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Time-Spnce Grapha. Td gupplemene the annuai:mapg di the epiceneerg 1ee
ug canaider the sequpnce of earthquakes of differenr energiea and time
w4ehin the ]itniCe of the limited BecCl,ona of the invesei,gated areas Three
strips were aelected about 12 km w:lde each - two along the direction of
etrtke of the northern zoriee of the fracrurea and the mountain ridgeB
(i-i' and and one acroas the gtriket �ncompaesing the region of
maximum conreneraCion nf the epicentere (ZII-2II'). The longitudinal
8xps nf rheee etripg ere ahown in Fig 79. The earthquake, the epicenters
df which fell into the etripg, beinng ro the axial line.
The gplt I-I' (Fig 81) stretchee aYong zhp Alma-ACg gnd the Zailiyeltaya
fracture xone. Ita eeismic activity ia very nonuniform. The "wegtern"
zonp of increased activity iselated by us was encompasged by this etrtp
and extended lrom 0 to 60 km (to Alma-Ata). The seiemic conditiona of the
western zone were analyzed in Cime by the annual epicenter mape. LeC us
give attenrion to the fact that the etrong earthquake of energy clage 11
in the wegternmoet end of the zone (0-20 km) where rhere were very few
earthquakes Wae essentially amaller than in the eastern half (20-40 km).
It accurred against a background of almost C0f11p10t0 seismic quiet and
was noC gccompanied by gubsequent ahocke. The center of the earthquake
ig 15 km from the cenCer of the dieaecrous Kebin earthquakp of 1911.
'Che central part of the fracture zone, ae has already been noted, is in
prnctice eaeiamic. The northeast end of the atrip (110-150 km) encompasses
the northern part of the "eaetern" zone. Tfie comparatively high aeismicity
was observed here only at the end of 1973 and the beginning of 1974.
Belt II-II', which is similar With respect to etrike to belt I-I',
encompasses the Zailiyskiy Alatau Ridge and the north slopes of the
Kyungey-Ala-Too Ridge, that is, it passes through the section of the
"central" zone (20-100 km) wtth greatest density of the epicenters. As is
obvious from Fig 81, over the extent of 3 years of observations the central
part of the zone (40-60 km) is characcerized by increased seiemic activity
and the maximum comes in 1973 and 1974. A tenth class earthquake occurred
here ahich wae preceded by some increase in activity and then quiet
directly before the earthquake. There aere feW eubaequent ahocka. The
level df bctivity was high in the central part, decreasea sharply to the
southwest and northeast where individual, rare earthquakes nre obaerved.
The wectern edge of the belt (0-20 km) looks in general aseismic (although
the Kebin earthquake was located here) and it reflects the aeak activity
of the Wesc end of the Alatau ridges during the entire period of the
instrumenc observations aince 1931.
The time-space graph of the seismic conditions in strip III-III' clearly
itlustrates the displacement of the centers for Lae 1972-1975 period from
the aoutheast to the northWest,
Cemter Depch ttap. By the data oE the precedirig studies 13, 30, 311 the
earthquakes with K400-,500 km) were SBiICtEd Which have been
recorded -.luring the 1972-1974 period and Which had sufficiently clpar
arrivalb of first wave insuring accuracy of determining At no luwer than
*0.2 aeconds. The majority of the earthquakee were recorded by the
slaved recording gyatem where the accuracy of deteraaining At Was �0.10-0.05
seconds.
The majority of the procesaed 366 recordinga of dietant earthquakes are
$rnuppd aith reepert co defined regione, each of which characterizea the
predominant valuea of V* (eee Fig 90). The obaerved values of the
apparent velocity lie wfthin very broad limita (from 6.5 to 60 kai/9ec),
the angle of Arrival e variea from 25 to 85�. Thp predominant values of
V* nre 10-30 km/gec (e-55-80�). The represencativenegs of the regiong
ia not identical. The maximum number of recordings aere obtained from
the reRiona of Indoneeia, the Philippinea, Japan and the itamchatka-Japanese
zone; the minimum number, from the arees of Chile, Argentina, Peru and
Mexico. The processing reaulte are illustrated in summary grapha of the
nzimuthal deviations as a function of azimutha of the epicenterg (Fig 92).
Thc curves for the maximum inscrument errors for tWO valuea of V* are
depicced on the same graphs. The azimuthal deviatione are of intereet,
the roagnitude of xhich atably go beyond the limits of possible errora.
Let us consider the azimuthal devl,ations defined by the Talgar-Ozero-A1i
triangle (Fig 92). The values of Aal and Qa2 for the earthquakes are
plotted on the grAphs from the provieionally 3.solated five sectore
located in different di,rectione.
224
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Tabie 17
Key:
Am
~tt
cftow
P.Aoa
~ttmwrpan~�
ra pooo*c+i�
V40a4/6
'
(1)
(3)
103 ar
(S)
20r Xlf
21o01
loro-soorovmee o-w Xorco (g~
D65
11t8
20. XI
7,38
Npea
'
2o3
13,4
14. Xtl
. 8o18
g)
KacnMAdooo Mopr ~
2,8
1810
10. x1
8j48
Mopo GewAas NauoueouM C~)
968
2860
28. Xlf
7o38
6oramn��4sw ' (10)
i8
32,0
1.
DaCe
6.
Southeaseern Honahu Ieland
2.
Time of day, hours, minutea
7.
iran
3.
Region
R.
Caepian Sea
4.
Epieentral dietgnce, 103 km
9.
More Bandg, indonesia
S.
V*, km/see
10.
Bolivia-Chf1p
1. The Kamchatka-Japgnese aectnr (azimuth 50-80�) corresponds to the
range of ema11 in9trumpnt and atation errorg. The lntroduction of
cnrrectiong for the relief ingignificantly change the pogition of the
experimentnl poinrs, but it grouped them more corepactly. The emall, but
gtable negative azimuthal deviatione on the ordpr of 5� are etill observed
after introduction of correctiona for the relief.�
, 2. The Indoneeian sector includee azimutha to the epicenters of 90-140�.
Por this sector a maximum number of recordinga Were obteined, and eig-
nifirent scaetering Qf the expQrimental pointe is observed. 7fhe large
rorrectiong for the relief in the sector essentially diminish the diepersion
of the points. The azimuthal deviations of the beama in the sector of the
azimuth 90-130� are etable. They are negative and they anwunt to 10�, that
is, they coincide With respect to sign With the Aa for the Kamchatka-
Japanese aector, but they exceed it by 2 timea with respect to magnitude.
3. The Chineae sector contains azimuths of 110-190�. The number of
observation points is smell, and the centera are near; therefore the _
values of V* are amall. The large time corrections for the relief dt
ahich can turn out to be aomewhet high and the azimuth range correspond to
the maximum 6ngt, The introduction of the correccione for the relieE
ghifte the pointe beyond the lf,mita of poesible errora; the valuea o� che
azimuthal deviations become poaitive and equal to 5-10�. The results of
eetimatinq Aa for the earthquakea from thta sector are not very convincit .
4. The Nindukuah sector is the aztmuth oE 210420�. In thia very narrow
sector af dirertions there are mAny o6servation points ahich are piled
together. The correctione for the relief are In practice zero. Stable
posicive azimuthal deviations of 10-15� are obeerved. The most reliable
results are obtained in thie aector. `
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Tobie 17 Cconebued.j
Mradr� (i)
(2
~t, o � ~ '
,
e.
~ 1~~ i"1 p~' lT"'tA &1 '~s
C3)
~
~3
o
~'s4
-o,,2a
e
`..ia
�.7
~
zi
sa
Q~
~tZZ
,
�8
't
4
;4
177
289
280
433
AZi
-0
l1
3
0
izo
++oaa
117
aso
-aso
xo
-22
.9
to
SOZ
918
268
0*30
-420
~ZO
16
�r1
is
Key: t. azimuth, �
2. azimuthal deviatinne, �
3� Aaingtr
5. The Lat3n Araerican eeGear (aaimuthg 30-350�) has fpa data gnd great
digpergidn of the experimeneal points ea�+30�. The correeeioas fnr
the relief are large; rheir introduction has decreaspd the dispersinn
of the pdintg eomeahat. All of thie end aloo the large valuee of V*
reduce the accuraCy nf flstermining Ag. Hoaever, on the whdle it ig
possible neverthelpgs to eay that the paeitive signg of gzimuthal
deviaeidns predominate, the magnitude of whieh ia diffieult to eseimate.
Thus, the experimental obeervationg of the dietant earthquakee by a group
of gtations in the Alma-Ate tegt area revealed stable deviatione of the
directiong of propngation of the firet longitudinal waves from the azimuGh
ta the epicenterg caused apparently by nonuniformities on the path of the
benms. The values of the size of the deviations are different for beams
and different azimuchs. The accuraulatinn of thig inforaation ia of greac
interesc from the point of viea of gtudying th~s nonuniformitieg of the
medium. The development of the procedure for such obaervationa under
complex conditions of the ground relief and also the diacovery of azimuthal
deviations as n function of the epicencral distance are of intereat. This
' analygis has not been specially performed. it ie only pogeible to give
attentinn tn the fact thAt tWn such regions as Indonesia and China, ahirh
are in the game azimuth sector but at different dietances from the obgerva-
tinn point, are characterized by azimuthal deviations of the seismic beams
of diEEerent gign.
226
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Q C~) ~y,~~ ~~wi( A'.~,Mi r~6,~ . ~ +~arr .
I'"1
)
, a
46
~I � � M~M~N1M ~ ~..]~1~i
~iMM~y ~ s~ ~ ra �~~~i~'~I~
, , � ~ ~ w
! j~ ~M � ~w
~M~.~� ~ ~ w,i~ ~�.~..N+~�� �
. ~ ~."1"~"1~~
j

Iit' am..e p
I
.
' �
+ 4.

Figure 92. Azimuthal deviationg aa a function of the azimuth
of the epicentera vithout considering (a) and
considering (b) the ecatian correcciong
The maximum instrument errors (1) and the correctiona for the
relief (2) Were calculatkW for two values of the apparent velocity
g Itti1/8EC (the side lines) and 20 km/sec (the dottpo lines).
Key:
1. Kuri]a 6. Ninduku8h
2. Japan 7. Chile
3. Kemchatke 81 Argencina
4. Indonesia 9. Peru
S. China 10. NexS,co
22y
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94. DirpetiOng aF Puturd Roaeaxeh
Thp inventigatpd rpsuita of the highiy aenaiti,ve dbeervat3ons aieh r$din-
teiemetric reebrding indicate thae the generai nature of the aoismic
picture obtained in the Alma-Aca highiy eensitive teee area and by eho
drdinary netaork of sEeEiona turns out ed be appreximately idenfica1,
This makeg it possible to tnakp e flumbpr of remarka wieh respece eo fureher
imprnvement di the highiy sangitiva oporationa with the radioceiemecric
recording oygtpfi.
Firat of a11, it in neeoanary ta note that under the catnditione of fixed
norieg of sedimeneary deposies With a h3gh ieve1 of microegiamic int@r-
fprpncp in the vicinity nf alarge city the seirmic obgervationa in deep
velis gre the oniy mpans of recording earthquake� of weakpr energy
claaaes vhieh increaapo the reprogentaciveneea of the aeismogeological
dgta for acomparetiveiy low ievei of overeli seismic background. The
pdanibility of uging the aeaker ahocka to charactertae the reismic con-
ditfann in time is the moet Impercant reauie of the research.
Une of the basic prublpmg of the development nf seismologicgl gtudien in
the regtang of probable oCcurrence of etrang ppinnic evente is the use
nE inatrumenc ob9ervetiong to predict the time of occurrenee of strong
earehquakea. in order ta expand the foreceeting poegibilities in the
inveaeigaEed arpe the firsc gcep is the expanslon of the observation oyatem,
first to the eaet, and then to the wpar, and then eouth. Beginning aith
the noige 1eve1 of the erea, the nev eaetern nnd weetern etntione muat be
lncated in especiatly drilled weils. rhe developmpnt of observatione in
the south is posaible under the condition oE tieing lov-pover and economical
rfldio communicatiane ehannele, the operation of ahich is inenred by the
autvnomoug poaer eupply. The improvement of the entire radiotelemetrtc
obsprvetion ayetem, aa a minimum, requiree the organizgtion of cwo or three
stgtidne in the aeet, one in the eagt and two or thxee in the south. The
experience in operation of the R'C5 indicates thac after expanding the
encire obeervatica ayetem it will be po88ible basically to do away With
the application of ordinary eeiemic etatione and etthe same time eignifi-
cantly gimplify the pntire organization of the eeismologicai aork in
Northern Tyan'-Shan'.
Lt is neceesary to convert frmn the vertical geismographe to the obaerva-
tion sygtmn vith cricamponent ingcruments. This observation syetem wi.ll
pe nait more reliable gcudy of the variation of the ratio of the velocities
of the longitudinal and cranaverge aavea in Alma�Ata geismically active
region. The expaneion of the p$ss band of chc- :.elamic channela in the
direction of the low frequenciea will permit ua co etudy the spectral
composition of the seiemic recordings, including ac the timea of BcaCtering
of the voltage at the Qarthquake center.
These characteristics can be uaed for forecaeting atrong eerthquakes. The
syatcm of observacions muat alao provide the poeaibility of reliable
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deeerminaei,en bf the mechanigm d# thtCenee_g, The exrprience of ouch
atudi.eg tn the Garmakiy ttayon of Tadahik 3S1t 3,ndicateg eltat during the
period nf preparation of stxdng earthquakes,. a ehange eaken piace in the
mechanism of the eentera of the weak ghockgt Ye ie eignt,f3cant ehae the
eentralizpd reCbrding9 can ingure reliable deeerminatlon of the di.fference
in paeh of the spismie Waves through the zone af the prepared etrong
aHaek. The avai1ab1e daeA indi,cate ChaE thia eheracterieeic can a1ao be
df n fdrpcasting nature.
Thus, the ceneraiized h3gh-frequency reCOrding of earthquekes can insure
signiEicant pxpans3on of the aQigmolagicei data obeained as applied eo
the prablpm of prediceing serong earthqUakes. The effectiveneeg nf the
prediCtion studipe can be inereaeed ag a reeule of the uee of large
gtationg not only for etudying the eeiamologicgi observetions, but aleo
ae a reau1e of the drganization of obeervations of other geophyeical gnd
genchemical ateributea in the same we11a. in particular, in the we11s
obgervationg can be madh of the acou9cic noisp, threshold pregsure in the
deep water-ggturnted horizon, the pgrameters of the gpochemical regime of
grdundaater uging automated geochemical analyzers. The expaneion of the
rgnge nf observed parameters Will require the appl3cation of more mu1Ci-
channel radiotplemetrir gyscem8 reepectivfly. Thie systpm cen be crented
nt the present time by the industrially manufacturpd Konreyner (Containerj -
gtatian.
In order to incregge the opQrativeness of the forecaeting obaervatione
it ig necegsary in the negr future to organize the input of all of the
information to the computer and insure ite automatic proceeaing.
The areas of gubaequent experiments noted here Will depend in the future
on a number of techniCal poeeibilitips, but the prospeceivenesa of such
experiments is quite obvioue.
Thus, ne a regult of the 4-year operation of the radiotelemetric test area
a gtudy ie made of the seiamic characteristics of Alma-Ata for the period
from 1 June 1972 to 1 July 1976. Tt1e basic peculiaritiea of the regime
are as follows.
1. The seigmic eCtivity for the Alma-Ata area i$ A6=0.7, And the angular
cnefficient of the repetition rate graph Y-0.46.
2. The seismically active region of 2ailiyskiy and KungEy Alatau known
by the data from the preceding atudieg i,e broken dotm into several zones
rharuccerized by defined laWa of the seismic regime. The ectivity of the
diEErrent zonea ia exliihited diEferently in time. The highest activity
is associated With the section ahere the three zonea of deep faults join
;Iorthern Tyan'-Shan' wich the taest, Keaino-Chilik and Tyupskaya with
the east located 25-,30 1n i,n the southeasterly direction �rom Alma'Ata.
3. Signifirant migration of the centers occurs in time and in space.
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4. '1't�rc ure Nec:tore nf the axi,muehis td the diseanC earthquakee foz
which the eeablp deviations of ehe direetions of propagatinn -of ehe
�irse 1angitudina1 waves are characeeriaCice For the Japanese-,KAmchgtka
geCtor negaeive aximuthal deviations of 5� are observed; fox the
Indonesinn eector, negative deviations of 10�; for the Hindukush sector,
poaitive nximuthal deviations of 10-15�.
The experience Chat we heve gccumulaeed indicgeee the expndiency of
further work in the following areass
a) Expansion of ehp genphysical research dnd crpaCion of equipmenC for
such observgtions in we11a;
b) The development of mulCiplexing equipment for the radiometric
recording channels and the use of eeries, economic radio relgy syst ans;
c) The development of Che method of eCudying the set of phyeiral
pnrnmeCera;
d) The study of the polarization of seiemtc waves, in pnrticular
Crnnsverse waves.
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CONCLUSION5
The most aignificanC difficulty wi.th the detailed study of the Reiemic
chargcCerietica of large induetrial centers located in seiamically danger-
ous rpgiona ie the high level of interference connectecl with the vital
ncei,viCy of the city. The baeic requir.emente on the procedure are
insurgnce of highly seneitive observations and high accuracy of determining
the centers of local earthquakea. Theae, Co a great extent, contradictory,
requiremenCs correapond to the developed procedure based on seiamological
observations in deep wella permitting a sharp increase in useful seneitivity
of Che equipment under the conditions of high ground noise level, and in
centralized multichannel recording with a united type service aignificantly
raising the accuracy of all of the conatructions.
The effectivenesa of the aeismic observations in the wells arisea from
the fact that the noise level decreasea more rapidly with depth than the
uaeful eignal. The gain in useful aeneitivity during observations in
wells for different regiona is different, and it depends primarily on
~ the noise Ievel on the day surface. The higher the ground noise level,
the higher the gain in aenaitivity. At shallow depths (to 100 meters)
in loose aedimentary rock the gain is determined primarily by the absence
of the interference of wind origin which is not felt at depths of 40-50 M.
A large gain can be obtained for observations in shallow wells discoveripg
the basement. Here even at a depth of 30 to 40 meters with a very high
level of sround noiae sensitivity can be realized which is close to the
sensitivity of the ground atations located under favorable conditions.
At average depths (to 500-600 meters) the gain is determined by a sharp
decrease ln noise level in the upper part of the section and also atability
of the noiae. Under hish noise level conditions the observations in loose
sedimentary aeriea .zt depths of several hundreda of ineters can give a
significant gain,
Ttie observations at greater depths (2000-3000 meters) in practice in all
rases permit us to obtain sensitivity which is close to the sensitivity
tor ground observations under favorable conditions, However, the diffi-
culties of working at great depth under the conditions of high temperatures
and pressure Justify such observations only in cases where there is no
free choice of the investigatioct point, In particular, this pertains to
the study of the seismic characteristics of large industrial centers.
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1'hc! 4-yr.ar expcrimrnt .in the npereEion df the tpat axed of automated
htghly genditivp deep ae11 and grdund stationg created in th@ vlciniey
of Alma-Ata with centraltzed muicickanhe1, radidtpiemeEric recnrding
rnnfirmed the effectivpneee of euch obgervAeions oyaeoma f~~ ~tudying the
nciAmic regime df ierge induntriai centers, Such oyateme are charaGeorizpd
by high usefui sensitiviry of the ataeiohg, high eccuracy of the construc-
Cinns, operativeneee of proeeaaing permiteing datetmination of the poai=
tion of the cpaters nne to tvo minutpn after the beginning of the @areh-
ryuake and aiao eeeneiniCalnese of the operationa baaed on the tiutdmatic
mode of aperation nf the stations. A toeal di three apecia1isto nerviee
n test area of f ive atetione.
Under the conditiona of eeiemic quiet charaeterietic uf the florth siopes
of the zuiliyekiy Aletaut the automatpd etatiana of the eeat Area racarded
about 700 local eerthqunkee in 4 ypgrs With tg,.p(10 aee gnd about 300
exploeions. More than 85% of the local earthqugkee rpcorded by the
test areg stgCions belong to energy ciaesee 5 to 7 vhich are not represpnt-
ative for the regionai netaork of eeationg. 'Che veakegc parthqugkes
recnrded only by Ozero station belong td energy claee Z. The strong
ef�ect nf the observation conditions on the structure of the seismogrgms
in Eelt. The eEfect of the dey eurfaee relipf end alsd the nonuniformity
oE the upper part of the section have the greateet eignificance. Nhen
atudying the seiemic characteristics of the city it ie necessary on the
recordinge to diecover the local explosions and exclude theca frao the
subsequent proceseing of the local earthqugkee. The explosions in the
vicinity of Medeo differ froto the local earthquakee vith respert to ehaQe
of the recording and lower frequency compogition.
The procedure for proceasing the multiGhannel eeismograme from centralized _
radiotelemetric recording considering the spatial arrangement of the
test nrea etations insures determination of the centera of the local
earthquakes with an accurecy of +1-2 laa in plan view and aith respecC to
depth.
This makes it possible to recommend the dEVelopment equipment and the obsetva-
tion proceduXe to etudy the seiemic characterietica of large industrial
centera or other local sectiona in seismicelly dangerous areas end to
sulve various problems of aeiemology.
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49. Pavlova, I. N. "bynamic Ppculiarities of the Aleutian Bgrthquake
df 4Februnry 1965 and its Aftershocks According to the Recordings
oE the Frequency-Selective Seismic 5tation," EKSPERIMENTAL'NAYA
SF:YSMOLOGIYA (ExperimenCal Seigmologyj, Moecoa, Nauka, 1971.
50. pevzner, L. A.; Popov, K. A.; Puehkarev, I. K., et al. "Ceophysics
Reaearch During Microregionallzation of thp City of Alma-Ata,"
CEOFIZICHESKIYE POLYA i SEYSMICliNOST' (Geophysicai Fields and
SeiamicityJ, ttoecoa, Nauka, 1975.
51. Pomerantseva, I. V. "Isolation and Correlation of PS Waves Recorded
by the Zemlya Statione," TEORETICHESKIYE IElCSPERIMENTAL'NYYE ISSLEbO-
VI.:JIYA 012iG?iNYitH VOLN ZQ4,ETI;YA5E~IIYA ;Theoretical and Experimental
Studies of the Exchange Waves of Earthquakes), Moscoa, V*1II Ceofizika, 1973.
52. Riznichenko, Yu. V. "ttethods of *tase Determination of the Coordinates
of the Centers nE Nearby Earthquakes and the VelocitiQe of 5eiemic
Weves in the Area Where the Centera Are Located," I2V. AN SSSR.
5LR. GEOFYZ. (News of the USSit Aeademy of Sciencea, Geophyeics
Series), No 4, 1958.
53. Rozova, Ye. A. "Earthquakes of Centrel Asia," TitUDY SEYSMOLOGICH.
IN-TA AN S5SR (Works of the Seiamological Inatitute of the USSR
Academy of Sciences), No 123, 1947.
54. Urazayev, 9, M.; Akishev, T. A.; Antonenko, A. N., et al. "Rosulte
of the Forecasting Work et the Alfoa-Ata Geophyaics Teat Areal"
POISKI PREDVESTNIKOV ZEliLETRYASENIY. ;tEZHDUAIARj SIMPOZ.
27.05-3.06.74 [Search for Earthquake Predictor8. International
Sympoexum 27 *fey to 3 June 1974), T$ahkent, Fan, 1976. _
237
FOR OFPICIAL USE ONLY
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55. Urezayev, B, Mef Anconenko, El M.j d8pandv, p B, "5eismoCectonic
_ 3ppciai Geophysicxil and Seismmological 3tudi,r~a in A1ma-Ata Seiamicaily
, Active Rogiono," SEXSMICtiESKOYTs MIKRORAYDNIRaVANIYEjSeiem3C
Mieroreg~,onalizacian), AlmarAtal Nauk4l 1976,
~
56. Uraxayev, D. M.; Oepanort A, H.j Latypov, Zh. A., pt ei. "Earthr
quakes of Northern Tyan1q,Shan'," ZM4,ETRYASENIYA V SSSR V 1972
[Earthquakea of the USSIt in 19723, MogcoW, Nauka, 1976.
57. Pedugeyenko, N. Ye. "glecerodynamic Seiemograph," USSIt author'g
Certiflcgtp, ki. 42 a., No 475581, d'TttRYTiYA IzOgRETENIYA,
OBRAZTSY I TOVARNYYE ZNAKI [Diacoveriee, Inveneione, Mode1e and
TrademarkaJ, No 24, 1975.
58. Khalturint V. I. "Procedure for Estimating the Spectral Compoeieion
of 5eigmic Oscillgtione by the Recordinge of a Frequency SelpcCive
Station (ChIS3)," 'fRUDY IPZ AN 55SR, No 25, 1962.
59. Shnirmant G. L.; Raxorenov, A, A.; Agafonov, A. G. "Systenm for
Remote Control af Spiemir IneCrumpnte in Wellg," CEOFIZICHfiSKAYA
APPARATURA [Geophysica Equipment], No 59, Leningrad, Nedra, 1976.
60. Afamaty, K. "Microseism in Frequenry Range 1-200 cpe," BULL.
EARTHQUAttE RE5. INST., Tokyo Univ., No 39, 1961.
61. Hrune, J. N.; A1len, C. K. "A fticroearthqnake Survey of the
San Andreas Fault 5ystem in Southern Californiat" BULL.3EISMOL. SOC.
AMERICA. No 2, 1967, p 57.
62. Crampin, S.; Willmore, P. L. "Smell Earthquakes Obaerved with Local
Seismometer Networks," PHILOS. TRANS. ROY. SOC*0 LONDON A, 1973,
No 1239, p 274.
63. Croeaon, R. S. "Small Earthquakes Structure and Tectonic of the Puget
5ound Region," BULL. SEISMOL. SOC. AMERICA, No 51 1972, p 62.
64. Uouse, E. I. "Raylelgh Waves in Short Period Seismic Noise,"
BULL. SEISMOL. SOC. AHERICA, No 4, 1954, p 54.
65. bouse, E. I. "Signal and Noiae in Deep Wells," GEOPHYSICS, No 5,
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66. Douse, E. I. "Noise Attenuation in Sha11oW Noles," BULL. SEISMOL.
SOC. AMERICA, No 3, 1966, p 56.
67. Douse. E. I. "Short Period Seiamic tJoisel" BUL1.. SEISMOLl SOC.
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68. Faton, J, P.; 0'Neill. M. E,R MurdockT J, N. "AfteTahocks of the
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MiERICAN, No 4, 1970, p 60.
238
FOR OFFICIAL USE ONLY
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FOR OFFICIAL U5E ONLY
69. Cupea, i. N. uStanding Wave Phenomena in Shnrt-l'eriod Seiamir
Noise," GEOPHYSICS, No 60 19650 p 30.
70. Takanot Koj Nagi,waka, To +pbservaeten of Mtcroearthquakee With a
Deep-,We1i Seiamompeer," BULL, EARfiHQUAKB, RES, TN3T.~ Tokyo Uni.v,,
1968, p 46.
71. Levin, P. K.; Lynnl R. U. "Deep.Noie Geophong Stud3esg" GEOPHYSICS,
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72. Itnden, R, B. "Norizontai and Vertical Arrays for Teleoaiemic 3ignel
Enhancement," CEOpNYSICSt No 4, 1965, p 30,
. 73. Roden, R. B. "Sp38mic Experiment W3th Vertical Arrivea,"
, QEoPHYSICS, No 2, 1968l p 33.
74. Sax, R. L.; Hartpnberg8r, R. A, "Theoretical prediction of Sdismic
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75. 3ax, R. L.; Nartenberger, R. A. "Seismic Noiee Attenuation in
Unconeolidated Materialp" GEOPHYStOSO No 4, 19640 p 30.
76. "Second Phase of Earthquake Prediction program in Tokyo Area,"
mEcHrtocttqr, rto 3, 1976, p g,
77. Takana, K.; Hagiwakat T. "Preliminary Obeervation of Microe8rthquakee
aith n Deep We11 Spiemometer," BULL. EARTHQUAKE RES. INST., Tokyo
Univ., No 3, 1966, p 44,
7$. Hirono, T.; Shyehiro, S.; Furuta, M.; Koide, K. "'.Voise Attenuation
in Shallow Holes," PAPL METEOROL. AND GEOPHYS., No 2, 19549 p 19.
79. Hirono, T.; Shyehiro, S.; puruta; M.; Koide, K. PAP METEOROL. AYD
GEOPNY5., No 2, 1961, p 20.
80. Tntel, H. C.; Tuve, M. A. "Seiamic Obaervation at One Kilometer
Deptli," Contributione in Geophyaica in Nonor of Beno Cutenberg,
Vol 1, London, 1959.
81. Ward, P. L. "Comparison with DatA from a NetWOrk of Stations and
Small Tripartite Arrays on Kilaneal Haa$iip" BULL, SEISMOL. 30C,
AMERICA, No 2, 1973, p 63.
82. Zoltana, A. D. "Surface Wave Componenta in Microseisms" SULL.
SEISMOL. SOC. AMERICA, No 2p 1969, p 54, ~
239
FOR OPFICIAL USE ONLY
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APPROVED FOR RELEASE: 2007/02108: CIA-RDP82-00850R000100040010-5
FOR OFFICIAL U5g ONLY
APPSNbIX I. BULLETIN OP LOCAL B41THQUAK83 RECO1tDED SY ftADIOTEI.DW1tYC 5Y5Tffirt
FROM 1 JUNS 1972 TO 1 JULY 1976 pOR WNICH SPICBN'TSRS ARE CON3TItUCTTiD
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Key: l.
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number of RTS
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(b)
day,
month, year
(c) Ch
240
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APPROVED FOR RELEASE: 2007/02/08: CIA-RDP82-00850R000100040010-5

APPROVED FOR RELEASE: 2007/02108: CIA-RDP82-00850R000100040010-5
FOlt OFPICYN. USE ONLY
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. 1.76 r.
19.49.4118
268
8,7
a
12,5
'348
Y.., 11.76r. '
1. 0.:~O-j
408
8o2
9
1?,a
380
2.1 V.76 r.
13.19.000
4o2
7,a
8
12
351
12.IV.76r.''
2.22.82t1
601
so
9
0
352
300.76 r.
7.38.46.8
4o1
8,8
� 3
0
. 383
4.V.76 r.
2.20.85o8
8,3
7ob
4
6
354
15.V.76 r.
3.28.14~0
7,0
7,0
3
14
355
27.V.76 r.
,~7.49.88~7
400
6o3
2
-
350
. 1.V1.76 r.
17.12.49.3
4,6
� 6,9
4
8�
387
1.Vt.76r.
17.13.82,0
5.0
7,4
~4 .
4
358
S.V1�16r.
S. 3.85,8
8o4
T.3
3
0
_ 359
20.V1.76 r.
20.27.31,2
8,7
9,3
4
0
380
21.Y1.76 r.
20,81.11l8 �
407
b,8
3
30
3E31
27.VI.76 r.
12.21.18,5
808
8t8
3
O
382
28.V1.76 r.
21.48.11o3
3,0
7o8
4
la
Noteg. The depth of the basement under the Alma-Ata atation of 4.2 km
ie taken as the reduction level HrRO.
*The Kurmenty (K) and Chilik (Ch) stations of the regional network are
indir.ated, the data of which were used to find the coordinates of the syatem.
**Tha earthquakes not recorded by the complex aeismological expedition
atntion. The time was taken by the T(RTS) station,
246
FOR OFFICIAL USE ONLY
~
19
~
i
,
APPROVED FOR RELEASE: 2007/02/08: CIA-RDP82-00850R000100040010-5

APPROVED FOR RELEASE: 2007/02108: CIA-RDP82-00850R000100040010-5
FOR OIFICIAI. U58 ONLY
~
APPENUtX II. UULt,E'CIN OF NEARnY IWriUSTRIAL EXk'LOSiONS RECORDED riY TNE
itAbtdTN:f,EME'CRIC SYS'CEM FRpM 1 JUNP, 1972 to 1 JULY 1976
1~1 Aer~ Ap~M~ ~~.~.o K ( M~cro apA."
i
- -Ny1.72 r.
~ 0. 1.32ea ~
7.9
2
Is.vt,72r.
e.31,49,7
$;a
4
19.W.72r.
11,80,67o9 �
409
4
S.Vt1.T2r. ~
12.,97'
7it
8
6.Vtf.72r. ~
11.84.48,4
5,9
6
I1.V11.72r. �
1.14. 104

7
15.V11.72r. -
0. 1.3208

e
30.V11.72r. �
~
0.0. 1008 '
8
a
9
1.IX.72r.:
11.38.49ii
0
y0a
10
11
18.1-X.72 r. -
20.tX.72 r. '
=Z;22,2:00 ~
i0
'3.30i9 .
00 .
8
4
12
22.1X.72 r.
.
8.34.08,2
0
4,4
13
14
8.X.72r.
1lf.i4.lAiO
a,a,
.
3.X1.72 r. �
10. 0. 3e2
7,3
18.
2.XII.72r.
10.20. e#2�
e,A
ie
13.L73r. ~
8.81. 804
lf07
17
31.1.73r. ~
10.80.4A*2
703
18
S.ti.73r.:
8.53,38.8
b03
19
23.N.?3r.;.
8.36.45,2 '
706
20 '
I1.VI.13r.
e. 5.43,8
_
21
S.V11.73r.:
14.40.1169
7,8
22
19.V11.73r.
0.13.4790
7,4
23
19.V11.?3r.;
10.27,31.0
6.8
24
29.V11.73r. �
22.12.4Ar0.
603
25
31.V11.73r. �
11.18.08,2

28 ,
4.V111.73r. �
8.28.3203
7.3
27
8.V111.73r.;
18,25. 803
' 8e8
28
10.V111.73r. ~
10.37. 8ea
7,3
28
18.V111:73r. �
20.'7.8198

Mideo
of
of
u
of
of
u
of
Kotur-Bulgk
Madao
KoCur-Bulak
Medeo
Kotur-Bulak
n
of
of
it
Medeo
Kotur-Bulak
Madeo
Kotur-Bulak
Iseyk
Kotur-Bulak
Kapchagay
Medeo
KaRchagay
n
North of Alma-Ata
30
4.IX:73r.
A.11.8018
5~a
Kotur-Bulak
31
S.fX.73r. �
8.40.28,4
' �
Chilik
32
93
20.FX.73r. ~
25.FX.73r. �
il. 2.54,2
10. 1.1802~
9,a
8,8
K,a chagap
KoCUr-Bulak
�S4
4.X.73r.
11. 7.38,8
5.2
Medeo
.
35 38
S.X.73r. �
6X
7
f.33.30,2;
12
4
-
chagay
~g
.
3r.
.
8, 8,0
8OA
eo
37
B.X.T3r.
11.50.28,8
5,7
Medeo
38
9.Y..:'3r. �
11.28.27,7
' 6,0
"
39
10.X.73r.
11.28.85,5
_
"
40
12.X.73r.
11.48.45,8
. 5,8
_ 41
U.X.73r.
11.31.45,6
a.;
"
42
14.X.73 r. .
11.31.54,8
8,4.
Key; 1. date; 2. time, hours} minuteal seconds; 3. place of exploaionf
4. dny, montli, year; S. *at Ta7.gar atation
247
FOR OFPICIAL USE ONLY
APPROVED FOR RELEASE: 2007/02/08: CIA-RDP82-00850R000100040010-5

APPROVED FOR RELEASE: 2007/02108: CIA-RDP82-00850R000100040010-5
FOR OFFICIAL USE ONLY
Appendix 11, coneinuQd

~ I
, g
;a 11
4
f R

_...1
4
...-~~.73...._..+
1
.
3.29.2007

I
.
, I WedeA
44
16,'.73r.
12.34.1402,

r
4e1
' 17,X.73r.
3,04 al D
. � .
' . .
i8
19.X.73r.
ii. LQi;D
' 602
+7
20.X.73r.;
1%.18.5803 ,
. 4,6
�
4e
24.X.73r. �
12.28. 904
�
'
40
25.X.73r.
e. o.aa,a
. a
� .
80
27.X.73r. ,
ii.i4.340i
8jy
� ' .
81
.27.X.73r. �
11.98.2a04
808
82
�2.X1.73r.
il. R,;JA#O
' 83
3.X1.73r.
.8.22:18e3
B07
54 '
3.XI.Z3r.
I1.27.3700
408
~6a
16.X1.73r.
11.38. 4,0
a64
, �
ae
20.XI.73 r.
B. 0.2402
1008
~
87
25.X1.73r.
10., 4.12,5
lSoe,
� '
8s
28.X1.73r.
. ii. e.34,e
a,a
~ � .
ae
'30.X1.73 r. .
ii.ie.az0a
s0s
�
~
80
30. XLT3 r.
i i.17.11, A
~ 8~ A�
, :
ei
4.XI1.73c.
10. 8.28j9
790..
Korur-Bulak
' 82 ,
� 4.Xt1.73r.
11;87:30ld
lSj7
Medeo .
83
11.X11.73r.
~ ii. 3.2504
8l8
.
64.
18.XI1.73r.
11. 8:14# d
7p7
.
88
19.X11.73r.
18.87. 000
902
Kapchagay
88
25.XI1.73r.
8.33.Z9,1
-
Medeo
87
2
6.XI(.T3r.
11.13.44,3
8,7
8B
~
LA.{~A1L73r.
7W4.57,4
~ .
�
.
ge
29.X11.73r.
I1.53.1e,3
e0a
Kavc)aaav.
7p
7.L14r.
11.31.24,0
. 8,4

71
8.04r. �
5.10.0104
3.7
.
Medeo
72
8.1.74t'. �
12. 2187o1
' -
t
' � ~
73 .
9.1.74r.~
il. 7.89,9
-
' ,
74 �
22.1.741'�:
11. 9.27.4
r
�
73
� 23174r. �
8.44+1160
4,6
. ,
fig
25.1.74r. ; .
8.10.15,0.
'
.
,
77
25.1:74r. .
11.39. 8,7
. -

78
99.1.7 4r.
10.59. 3.8
-
'
'
Kapchagay
78
30.t~.T4r.
10.42.82.6
.702
Kotur-Bulak
80
.5.11.74r. �
11.14:28.9
703
Medeo
81
7.104r.
1l.1 7.42.3
� a0s
�
82
9.11:74r. �
1.57.41,0
7s0
, � � . ' �
~
83 .
. 12.11.74r. �
11.13.14,1 .
� ' 501
, .
� �
84'~
12.11.74r. �
11.38.14.1
� 8,3
ICB
chagay
~ ga
16.IL7ar.
11.10. ^~s
507
~
s
Mc eo
. 88
'19.f1.74r. .
21.28.b2~e
706
.
West� of Alma-Ata
87
22.I1.74r.
12.28. 70b
7.0
Kotur-Bulak
88
23.11.74 r. �
9.28. �360T
8p2
_Medeo
8e
1.!it.74r.
11.23.44,8
' 8r?
~
' � ~ � ' �
90
3.I11.74r.
12. 8.87.4
' -
'
. ' . .
~
81
4.10.74r.
11.22.54,9
, 792
�
. '
82
12.IiI.74r.
12. 7.38,4
818 -

~
83
13.111.74r.
i. 8.24,8 .
4;8
�
94
' 22.I1I.74r.
5.47.28,8 �
8o8
Itapchagay
248
FOR OFFICIAL USE ONLY
APPROVED FOR RELEASE: 2007/02/08: CIA-RDP82-00850R000100040010-5

APPROVED FOR RELEASE: 2007/02108: CIA-RDP82-00850R000100040010-5
FOtt nFFICIAL
U8B ONLY
Appendix 1I0
aontinued
r
a
s
4
e
an
211i(.74r..
0.42,97,9
~
Kotur-Bulak
A8
30.111.74r.
19.90.1110
8,0
Kapchagay
67
14m4r.
19. 8.18f8,
8Ia
-of
98
4 r.
11. 5.54o4
S,4
Madeo
'
99 .
4r.
i1.10. 6.8
slO
10p
'11.I-Y.74r. '
0.27.10,0
l~~d
� ~
. 101 ,
I2.1-V.71r.
1i.37.4Aoi
�

ioz
16.1y.71r. ,
io.s4.aiqe
a,5
tcotur-Buiak
103
18.'V.74r. ~
11.18,4804
-
Mado0
104
22.IV.74'r.
11.48.Z86o
8#7
Kspc}utgay
105
23.IV.74r.
ii.ii~48,3
8O0
Madao
108
24.IV.14r.
12. 1.90j4 �
7,1
iCotur-Bulak
.
107
26.IV.74r.
11.28. 718
704
Modgp
108
28.(V.74r.
8.44.18j2
s,d
'
109
7.V.74r.
11,12. 212
d,s
�
110
B.V.T4r.:
i1,lA.2Ao8
' 8,8
Kapcyaggy
111
22.V.74r.
11.17.1,902
8,2
Miadac
112
29.V.74r. �
11.21.2A04
8,8
113
29.V.74 r. �
12.10. �,A
-
Kapchagay
114
10.Vi.74r.
ii. 9.24,9
8,7
"
118
12.V1.74r.
11.18.84,8
5,8
Mgdeo
118
13.VI.74r.
11.18.98,2
8o8
'
117
22.V1.14r. �
8.11.23,4
807
'
118
23.Vi.I4r. �
8.38.14,4
S�B
'
119
29.YI.74r. �
i. 0.9317
8.S
�
120
30.Vt.74r,
a.ss.4soe
605
~
121
9.V11.74r.
11;36.24,4
807
'
122
13.Vp.74 r.
1. 0.12,5
887
I8e4_Kull
123
13.V11.74r.
4. 0.15,0
' '
124
18.ViI.74r.
,
11.29. 9,4
- ,
Medeo
. .
u
125
'..'O.V(I.?4r.
ii. 8.20,9
'
126
25.VTiN r.
0,28.19A
807
'
127
128
6.VII1.74r.
9.V111.74r.
0.28.30,0
0,48.9104
8.5
IC,~tr-Bulak
128
I1.YIII.74r.
b.25.23.5
8~8
, t~edso
�
130
13.V111.74r.
0118. 010
7,8
131
24.V111.74r.
0.43.19,8
701
'
132
27.V11I.74r.
11. 1.13,7
-
133
28.V111.74r.
11. a.44,2
8,1
134
135
2.tX.74r.
3.iX.74r.
il. 8.2702
20.22� 2.7
8.1
7,7
Kapchagey
138
4.FX.74 r.
11. 0.30.5
-
Medeo
137
7.IX.74r.
7. 8.34017
7,9
138
1.X.74r. �
11.28.23,8
-
' .
- 138
6.X.74r.
0.32.48.0
7,8
�
140
19.X.74 r.
10.57.41,0
8,0
'
141
22. X.74 r.
11. 1. 8.3
5,5
'
142
30.X.74 r.
11.57.40,2
7,4
'
143
2.X1.74r.
8.47. 4,0
3,7
Kotur-Bulak
144
3X1.74r.
9.20.38,7
5�9
Southeaet of Osaro
~ 145
12.X1.74r.
11.17.22,5
7.8
Medeo
249
FOR OFFICIAL US8 ONLY
APPROVED FOR RELEASE: 2007/02/08: CIA-RDP82-00850R000100040010-5

APPROVED FOR RELEASE: 2007/02108: CIA-RDP82-00850R000100040010-5
FOR OFFIGiAL U3E ONLY
~
Appendix It, conCinupd
148
.17.X1.74r.-
8.87.4007
. 8,1
' Medao
147
2b.Xi.71r.
Z2.43.4808
qjg
itapchagay
149
22.XI.74r.
10.22.20j8 -
8'g
140
22.XI.74r,
ii. a.40i6
_
~
18Q
29.XI.74r.
'
7.33.4810
gj7
Medeo
151
B.XI1.74r.
10. 8. 2,3
9,1
Kapchagay
182.
1S.X11.74r.
a. e. 0;0
709
North of Alma-Ata
M~�
183
15.XII.74r,
g.48.371e
'

184
16.X11.74r.
10.90. 003
8 2
North of Alma-Ata
18b
17.X11.74r.
7,2i.31j4

Madeo
1SV
19.X104r.
ii. JL. 2 G7. 1
',i
� y
157
22.XII.74r.
8:33.2102
7,4
~
lg8
20.XI1.74r.
9.34.11,8
8.8
I North of Aima-Ata
188
27.X11.74r.
8.82.9908
70p
KaPehgggy
180
28.X11.74r.
10.49.4904

Kotur-Bulak
181
31.Xi(.74r.
10.29.480A
,8
Medeo
182
9.1-.75r. �
7. 5.4008
3
~g
� ,
183
I 4.1.75 r.
11. 7.0411
70a
� .
164
20.1.75 r.
10. 1.41,3

185
21.1%75r.
7. 6.02,7
507
.
188
26175 r.
e. 1.14,8
.7.8 ,
�
187
3117Sr.;
8.48.23,0
-
�
188
2.(i.75 r.
7.82.29.4
7JI
�
18A
6.I05r.
11. 0.20,9
804
�
170
&N.?Sr.
7.48.Zi1p
8'8
�
171
10.105r.
11. 7. 6,8 .
5.8
� '
172
11.11.75r.
11.18.58,3
5,2
�
173
16.105r.
2.02.3408
805
~
174
20.H.ISr.
8.35.28,0

� .
178
21.H.75r.
11.23.50,8
7,8
� '
178
1.[iuSr.
11.39.54.2
8,8 .
� ,
177
10.HI.75r,
il. 1.38,8
8,2
.
'
178
I1.111.75r.
li. 7.4509
768
Kotur-Bulak
179
12.N1.75r.
e,5e.13,8
70g
Medeo
180
12.111.75r.
18. 3. 4,0
4,8
�
161
14.Ii1.75r.
12.38.41,8 '
8,0
~
182
15.H1.75r.
11,23.21.8
' S04
f�
183
15.NI.7Sr.
11.24.18,1
�
5.8
�
184
18.I0.7Sr.
1.98.20,6
9,2
Kapchagay
185
23.01.75r.
8.10.51,2
8.4
Medeo
186
28�I11.75r.
8.18.3@01
~
" ' �
187 .
1.W.75 r.
6032.42,2 r
804
~
168
4.tV.75r. �
ii.Z3.Z1l9
8ta
�
ieA
8.tV.75r.
12. 4. 890
'
Near Medeo
1~
10.tV.75r.
7,94,6
~
8,0
Medeo
191
15M.75r.
8.48. 8,7
802
~
182
WV.75r.
11.90.24,8
a,8
� .
183
. 18.tV.75c.
7. 2.2ioa
a.8 �
� . . , ,
194
18.V1.75r.
' T. 2.8000 ,
507

250
FOR OFFICI
AL USE ONLY
APPROVED FOR RELEASE: 2007/02/08: CIA-RDP82-00850R000100040010-5

APPROVED FOR RELEASE: 2007/02108: CIA-RDP82-00850R000100040010-5
FOR OFFICTAt U98 ONLY
Appendix II, conCinued
Z
I, 9 j
, 4
!f
160
19.1V.75r.
. 13.41.19o8
7~g '
K~pchagay
198
20IV.75 r.
14.ai.29o4
7~8. ,
Modao
197
23.iV.75r,
8.23,4$t0
oth
KoCur-Bu1ak
ice
23.iV.75r.
11.14.5sl3
ri,7
MedBo
168 .
6.V.75r.
11. 8.9801
7
8
�
200
12.V.75 r.
11.96.48o9
0
8I9
.
'
201
18.V.75r.
3.98.3911
8,8
�
.
202
22.V.75r.
12.16.14,0
8~i
~
703
23.V.75r.
11. 8.4~6A
8~8
Kptur-Bu18k
204
25.V.75r.
7.51.26,6
'8,8
Madeo
ZOa
91.V.75r.
10.38. 7j0
8
'f

208
2.VI.75 r.
11,48.2A,0.
,
8t0
Korur-'Iulak
207 -
11.32.38,7
8o1
MQdao
208
8.VI.75r.
e.88,87o0
7pA
�
'208
13.VI.75:'.
8.11.1303
7v0
�
Z10
14.V1.75r.
6
02.42
3
7
7
211
17.V1.75 r.
,
0
8.97.34,4
l
718 ,
�
ziz
22.v1.75 r..
e.34.42oa
-
. ~ .
213
.22.VI.75r.
8.de.OZ~B
-
'
214
27.VI.75r.
T. 8.44,4
'7,3
�
215
1.V11.75r.
7. S. 9
0
-
7
0
"
218
7.V11.7Sr.
.
0
11. 8.22
6
,
8
4
217
8.V11.75r.
,
ii. 8.87
1
,
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8
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8
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.
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of Alma-Ata
240
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8,4
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242
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r
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11.22.3302
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11.X.?Sr.
6.50.1002
8,9
Kotur-Bulak
251
FOR OFFICIAL USE ONLY
APPROVED FOR RELEASE: 2007/02/08: CIA-RDP82-00850R000100040010-5

APPROVED FOR RELEASE: 2007/02108: CIA-RDP82-00850R000100040010-5
Appendix II, conCinuad
FOR OFFICIAL U5E ONLY
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l
.
~
3
4
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148
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707
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the northweeC
of A].ma-Ata
248
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8.10. 8t8 .
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8.8i.47j8
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281
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8.48.87j6
8tA
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252
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708
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283
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7,5e,28,7
8,A
'
254
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.
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266
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288
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287
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8l8
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289
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20,33.1668
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9
8
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281
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7.12.35.7
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283
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6~ 83.11,1
70.4
284
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608
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Kotur-$ulak
287
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8,7
288
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288
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8,3
270
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7,0
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11.20. 6,7
8,0
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. -
277
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278
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-
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7g5
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280
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7,2
�
281
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8,7
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:
283
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8.11. 708
8,5
�
COPYRIGH'T: Izdatel'etvo "Nauka," 1978
10845
CSO: 8144/0935
- END -
252
FOR OFFICIAL USE ONLY
APPROVED FOR RELEASE: 2007/02/08: CIA-RDP82-00850R000100040010-5

APPROVED FOR RELEASE: 2007/02108: CIA-RDP82-00850R000100040010-5
APPROVED FOR RELEASE: 2007/02/08: CIA-RDP82-00850R000100040010-5

APPROVED FOR RELEASE: 2007/02108: CIA-RDP82-00850R000100040010-5
.
40
APPROVED FOR RELEASE: 2007/02/08: CIA-RDP82-00850R000100040010-5