JPRS ID: 9002 USSR REPORT ENGINEERING AND EQUIPMENT

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• Content Type: REPORTS

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1978 ~ ~ _ ' ~ ~YR' _ 1 OF ~

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JPRS L/$827
20 December 1978 -
= Translation
Seismic Studies with the 'Zemlya' Device
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- JPRS L/8827
20 December 1979
~ ,
SEISMIC STJDIES WITH THE 'ZEMLYA' DEVI;CE
Moscow 5EYSMICIi~5KIYE I~SLEDOVANIYA 5 APPARATUROY "ZEMLYA" ~
in ltussian 1l77 signed to press 31 ~an 77 pp 1-256
Book by I. V. Pomerantseva and A. N. Mo~zhenko, Izdatel'stvo
"Nedra," 1400 copies
- CONTElVTS PAGE
ANNOTAT I ON . . . . . . . . . o . . . . . . . . . . . . . . o . . . . 0 1
INTRODUCTION . . . . . . . . . . . . . . . . . . . . . . . . . . . . 2 -
- Part 1. Theoretical Fundamentals of Using Different Wave
Fields to Study the 5tructure of the Earth's Crust and z~.
Uppmr Mantle . . . . . . . . . . . . . . . . . . . . . . . 15
CHAPTER 1. PHYSICRL CONCEPTS ON LONGITUDINAL P, TRANSVERSE S -
- ??IID COlt'lOSITE pS WAVES ON. RECORDINGS FROM EARTHQUAKES AND
EXPLOS2orTS . . . . . . . . . . . . . . . . . . . . . . . . . . . 15
Wave Fields Observed During the Initial Part of the Earthquake
" 15
Seismogram Recording . . . . . . . . . . . . . � . � � � � � �
Dynamic Characteristics of Single P and PS Waves from Theoretical
Czlculations. . . . . . . . . . . . . . . . . . . . . . . . . . . . 27
The Nature of Longitudinal and Transverse Waves from Explosions
ard Earthquakes and the F,ield of Their Appl9;cation. 32 -
� CHAPTER 2. HODOGRAPHS AND VECTURS OF P AND PS WAVE DISPLACEMENTS~ 35 -
Equations of Hodographs and of the Recording Times of
Single, Multiple and Lateral P and PS ~aves . . . . . . . . . . 35
_ Displac~nent Vector Components of Single Transient P and
- PS Wav~a and Thsir Azimuths in a Z1ao-Layer Three-Dimensional
Medium with a Sloping Exchange Boundary . . . . . . . . . . . 50 i:.
P~.rt 2. The "Zemlya" Deviae, Method of O~i~ervations ~
- and Interpretatian of the Materials . . . . . . . . . . . . . 57 ~
~ - ~a - [I - USSR - E - FOUO] ~
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CHAPTER 3. THE "ZEMLYA" DEVICE . . . . . . . . . . . . . . . . . . . . 57
Main Characteristics of the Optimum Design of the Device
for Continuous Recording of Seismic Signals . . . . . . . . . 57
~lock Diagram of the Device for Continuous Recording of
Seismic Oscillations . . . . . . . . . . . . . . . . . . . . . . 58 - -
~ The Field Recorder . . . . . . . . . . . . . . . . . . . . . . . . 62
A Device for Unified Time Marking of Field Recorders -
Radio Channel) . . . . . . . . . . . . . . . . . . . . . . . . 67
A Field Recording Reproduction Apparatus . . . . . . . . . . . . 71
Frequency and Amplitude Characteristics of the Ciiannel . 74 _
Method of Determining the Relative Sensitivity of the
Channe 1 . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 74
The Nature of Oscillations Recorded by the Channelo 80 `
Checking the Device Prior to the Beginning and During
Field Operations . . . . . . . . . . . . . . . . . . . . . . . . . 82
A Device for Processing Magnetic Tapes of "Zemlya"
Recording Stations on Analog and Digital Computers. 84
CHAPTER 4. NIETHOD OF OBSERVATIONS . . . . . . . . . . . . . . . . . . 86
- Field Operations . . . . . . . . . . . . . . . . . . . . . . . . . 86
Characteristics of Studies with the "Zemlya" Device 95
The Volume and Conditions for Recording Field Signals 98
- CHAPTER 5. WAVE FIELDS ON RECORDINGS FROM EARTHQUAKES AND
EXPLOS IONS . . . . . . . . . . . . . . . . . . . . . . . . . . 105
. .
Separation and Correlation of the First P and S Waves on
Recordings from Local and Near Earthquakes and Explosions 106
Separation and Correlation of P and PS Waves on Recordings
From Earthquakes and Explosions . . . . . . . . . . . . . . . . . 107 _
The Wave Patterns on Recordings from Local Earthquakes
( = 0-40 km) ~ . . . . . . . . . . . . . . . . . . . . . . 126 _
- The Wave Pattern on Recordings from Near Earthquakes �
. 128
( = 50-500 km) . . . . . . . . . . . . . . . . . . . . .
The Wave Pattern on Recordings from Explosions
~ ( = 0-700 km) . . . . . . . . . . . . . . . . . . . . . . . 130
The Wave Pattern on Recordings from Far Earthquakes
- ( p = 10-160�) . . . . . . . . . . . . . . . . . . . . . . . 136 ~
The Nazure of the Wave Field in Fault Zones and in the -
Presence of Subvertical Contacts of Media of Different
~ Petrographic Composition . . . . . . . . . . . . . . . . . . . . . 139
CHAPTER 6. DYNAMIC CHARACTERISTICS OF EXPERIMENTAL P AND PS WAVES
AND THEIR COMPARISON TO THEORETICAL DATA . . . . . . . . . . . . . 143
The Form o f the P and PS w'ave Recording. 143
The Ratios of the Amplitudes of P5 to P Waves and Their
- Dependence on the Parameters of the Medium. . . . . . . . . . . . 146
Visible Periods and Frequency ~pectra of P and PS Waves 151
Polarization of PS Waves . . . . . . . . . . . . . . . ` . . . . . 152 =
The Nature of PS Waves of Different Groups and the Criteria
for Separating Them on Recordings . . . . . . . . . . . . . . . . 163
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CHAPTER 7. METHOD OF INTERPRETING TRANSIENT COMPOSITE PS WAVES
ON RECORDINGS FROM NEP,R AND FAR EARTHQUAKES . . . . . . . . . . . 170
- Compilation of Time Profiles . . . . . . . . . . . . . . . . . . 170
Formulas for Determining the Depth to the Exchange Boundary
- (H), Seismic Drifts (L), Approach Azimuths Epicentral
Distances ( Q ) and Angles of Emergence of Seismic Radiation
(E) for Horizontally Layered Media . . . . . . . . . . . . . . . . 171
Construction of Depth Charts and Profiles for Horizontally
Layered Media . . . . . . . . . . . . . . . . . . . . . . . . . . 172
Method of Comparing Data of PS Waves to Materials of Explosions
and Deep Drilling . . . . . . . . . . . . . . . . . . . . . . . . 179 _
Characteristics of Interpreting Composite Transient PS Waves -
Formed on Sloping Interfaces of the Earth's Crust. 180
The Resolution and Accuracy'of the Composite Wave Method From
Earthquakes . . . . . . . . . : . . . . . . . . . . . . . 186
_ The Accuracy of Constructing Interfaces�by PS Waves 189
CHAPTER 8. METHOD OF DETERMINING THE COORDINATES OF EARTHQUAKE FOCI
AND ACCQMPANYING EXPIASIONS . . . . . . . . . . . . . . . . . . . . 193
~ Determining the Moment of Occurrence of an Explosion or
~ Earthquake . . . . . . . . . . . . . . . . . . . . . . . . . . . . 1 q ~ _
Determining the Location of the Explosion and Earthquake Focus 196
The Accuracy of Determining the Coordinates of Earthquake and _
Explosion Foci . . . . . . . . . . . . . . . . . . . . . . . . . . 198
CHAPTER 9. METHOD OF DETERMINING THE VELOCITY PARAMETERS OF THE _
blEDIUM FROM EARTHQUAKE AND EXPIASION RECORDINGS ( Q = 0-10�). 205
Calculating the Propagation Velocities of Longitudinal and
Transverse Waves from Recordings of Explosions and Near
. Earthquakes . . . . . . . . . . . . . . . . . . . . . . . . . . . . 205
Methods of Determining Coefficients K . . . . . . . . . . . . . . . 209
Determining the Velocity Characteristic of the Medium in
the Focal Zones of Recent Earthquakes . . . . . . . . . . . . . . . 211
Part 3. The Deep Structure of the Earth's Crust
and Upper Mantle of Various Geotectonic Zones. 212 -
CHAPTER 10. THE DEEP STRUCTURE OF THE CRYSTALLINE THICKNESS OF ,
~ THE EP,RTH'S CRUST AND UPPER MANTLE IN THE ~RAYONS OF TASHKENT. 212
_ Criteria of Intrarayon Stratification and Interrayon Correlation
of the Interfaces of the Earth's Crust . . . . . . . . . . . . . . 213
The Velocity Boundaries of the Crust and Mantle of the Tashkent
Depression and Their Geologi.cal Stratification . . . . . . . . . . 215
The Behavior of the Interfaces of the Earth's Crust and Mantle
~ Near Tashkent . . . . . . . . . . . . . . . . . . . . . . . . . 215
The Surface Structure of the Paleozoic Basement East and
Southeast of Tashkent . . . . . . . . . . . . . . . . . . . . . . 221
The Seismic Activity of the Territory of Investigation and -
Its Relationship to the Deep Struature . . . . . . . . . . . . . . 221
- c -
F(1R (1FFT('.TAT. TT~F. (1Nf,Y
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CHAPTER 11. THE DEEP STRL~CTURE OF TI~ EARTH'S CRUST OF THE NORTH
~ ~GERMAN DEPRESSION. . . . . . . . . . . . . . . . . . . . . . . 224
~ The Velocity Int.erfoces of the Earth's Crust and Their
Strat~.fication . . . . . . . . . . . . . . . . . . . . . . . . . . 225
Some Data on the Nature of Prapagation and the Structural
Shapes of the Interfaces of the Earth's Crust. 225
Comparison of the Thickness of the Sedimentary Mantle and _
the Crystalline Thickness of the Earth's Crust of the ~
German Democratic Republic and Contiguous Countries. 232
CHAPTER 12. THE DEEP STRUCTURE OF' THE EARTH'S CRUST AND UPPER
MANTLE IN THE SOUTHF.AST OF THE RUSSIAN SERIES AND THE ~
N~RTHERN PRE-CASPl'AN DEPRESSION . . . . . . . . . . . . . . . . . 236
Velocity~Distribution in the Crystalline Thickness of the
Earth's Crust and Mantle From Data of the "Zemlya" Station
by the Reflected Wave Correlation Method and Deep Seismic
_ Sounding . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 236
- The Structure of the Earth's Crust and Upper Mantle. 238
The Modern Tectonic Activity of the Southeastern Russian
Series and the Northern Pre-Caspian Depression . . . . . . . . . 239 -
CHAPTER 13. THE DEEP ST?UCTURE OF THE CRYSTALLINE THICKNESS OF -
~ THE EARTH'S CRUST OF THE UPPER MANTLE OF' THE AZOV-KUB.~N'
DEPRESSION . . . . . . . . . . . . . . . . . . . . . . . . . . . . 241
The Velocity Interfaces of the Earth's Crust and Upper Piantle -
and Their Stratification . . . . . . . . . . . . . . . . . . . . . 242
The Relief and Structure of the Interfaces of the Earth's
Crust and Upper Mantle . . . . . . . . . . . . . . . , . . . . . . 242
,
CHAPTER 14. PROSPECZ'S FOR DE~IELOPNIENT OF THE COMPLEX SEISMIC
METHOD OF STUAYING THE S~RUCTURE OF THE EARTH'S CRUST AND
UPPER MANTLE . . . . . . . . . . . . . . . . . . . . . . . . . . .245
The Geological Effectivene~s of the Studies. . . . . . . . . . . < 245
Comparison of "Zemlya" Station Data to the Results of Other
- Types of Geophysical Studies . . . . . . . . . . . . . . . . . . 249
The Economic Effectiveness of the Studies . . . . . . . . . . . . .252
The Direction of Further Studies with the "Zemlya" Device. ....253
CONCLUSIONS . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 255
BIBLIOGRAPHY . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 258
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PUBLICATION DATA
~
English title . SEISMIC STUDIES WITH THE "7.EMLYA"
DEVI CE
Russian title , SEYSMICHESKIYE ISSLEDOVANIYA S `
APPARATUROY "ZErII~YA"
Author (s) , I. V. Pomerantseva and A. N. -
Mozzhenko
Ed:itor (s) .
Publishing House . Nedra
- Place of Publication . Moscow
Date of Publication , 1y77
' Signed to press . 31 Jan 77 _
Copies . 1400
COPYRIGHT . Izdatel'stvo "Nedra", 1977
� - e -
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' ANNOTATION
A COMPLEX SEISMIC METHOD OF STUDYING THE STRUCTURE OF =
THE EARTH'S CRUST AND UPPER MANTLE BY USING LONGITUDIIvAL,
- TRANSVERSE AND COMPOSITE WAVES EXCITID BY EARTHQUAKES AND
EXPLOSIONS AND RECORDED BX THE "ZEMLYA" DEVICE WITH MAG-�
NETIC RvCORDING IN THE FREQUENCY RANGE OF ~.5-15 Hz AND
EPICENTRAL DISTANCES OF = 0-160� IS DESCRIBED. THE
THEORETICAL FUNDAMENTAI;S OF THE METHOD ARE CONSIDERED AND
EQUATIONS OF THE HODOGRAPHS OF TRANSIENT AND LATERAL PS
WAVES AND ALSO FORMULAS OF THE VECTOR COMPONENTS OF THEIR
_ DISPLACEMENTS ARE PRESENTED AND ANALYZF.D AS A FUNCTION OF _
THE ANGLES OF INCLINATION OF THE INTERFACES IN TWO- AND
MULTILAYERED THREE-DIMENSIONAL MEDIA. THE "ZEMLYA" DE-
VICE WITH MAGNETIC RECORDING AND THE METHOD OF WORKING
WITH IT IN DIFFERENT GEOLOGICAL PROVINCES ARE DESCRIBED.
BASID ON ANALYSIS OF EXTENSTVE EXPERIMENTAL MATERIAL OB-
TAINED BY THE "ZEMLYA" DEVICE IN FIVE SIGNIFICANTLY
DIFFERENT REGIONS BY HISTORICAL DEVELOPMENT--THE SOUTH-
EASTERN RUSSIAN PLATFORM, THE PRE-CASPIAN, AZOV-KUBAN' -
ANL~ NORTH GERMAN DEPRESSIONS AND IN THE RAYQNS OF TASH-
KENT, THE NATURE OF P, S AND PS WAVES IS DETERMINID AND
CRITERIA ARE GIVEN FOR SEPAR.~TING THEM ON RECORDINGS -
FROM EARTHQUAKES AND EXPLOSTONS AND FOR SEPARATION INTO
. GROUPS. A METHOD OF INTERPRETING P, S AND PS WAVES IN
MEDIA WITH HORIZONTAL AND SLOPING INTERFACES OF THE
EARTH'S CRUST IS DEVELOPED. THE CAPABILITIES OF THE
, METHOD ARE ILLUSTRATED BY CHARTS AND PROFILES OF 'i'HE
EARTH'S CRUST. MATERIALS OBTAINED BY THE "ZEMLYA" APPAR-
ATUS ARE COMPARED TO DRILLING DATA, IQ~IPV [REFRACTID WAVE
CORRELATION METHOD], GSZ [DEEP SEISMIC SOUNAING] AND -
OTHER GEOPHYSICAL METHODS.
~
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INTRODUCTION
Moscow SEYSMICHESKIYE ISSLEDOVANIYA S APPARATUROY "ZEMLYA" in Russian
1977 signed to press 31 Jan 1977 pp 1-13
[Introduction from the book "Seysmicheskiye issledovaniya s apparaturoy
'Zemlya by I. V. Pomerantseva and A. N. Mozzhenko, Izdatel'stvo Nedra,
1,400 copies, 2S6 pages] .
[Text] Many studies have been carried out in the USSR and aaroad [8, 12, -
, 13, 21, 33, 38, 39, 41, 42, 46, 47, 63, 74, 76, 98, 103, 142, 143, 149, 155]
to study the deep structure of the earth's crust and upper mantle, the main
purpose of which was to gain an idea about the shape and depths of deposition
of the interfaces in the crust and mantle, data on the physical parameters of
the crust and mantle and to determine the main relationships between geophysi- _
cal fields.
The most complete and unambiguous data on the structure of the earth's crust
and mantle in the USSR were obtained during regional seismi.c investigations .
by the refracted wave correlation method (I~IPV) and during deep sei~mic sound-
ing (GSZ), cleveloped by a group of Soviet scientists under the supervision of
G. A. Gamburtsev [38, 67]. The seismic studies conducted in di~fferent regions
� of the~Soviat Union during the past 30 years using KMPV and GSZ (G. A.
Gamburtsev, Yu. N. Godin, I. P. Kasninskaya, I. S. Berzon, A. M. Yepinat'yeva,
P. S. Veytsman, Ye. I. Gal'perin and others) made it possible to gain general
concepts about the structure of the earth's crust, to determine the canditions
= of formation and propagation of waves in its layers, to formulate general
- relationships between different geophysical fields and so on. The restric- ,
tions of their application were also established as the ICt~V and GSZ methods ~
were developed. The restrictions included the use of mainly a single class
of longitudinal waves, study of the structure of the crust and upper mantle
using extended`branches of hodographs obtained at distances 2-20 times
greater than the distances from the points of explosion to the initial~~_
points, which leads to signific~nt averaging to th e interfaces of the crust
[107]; the difficulty of studying narrow depressions with large angles of
inclination (up to~45-60�) and its limbs [125]; and the impossibility of
determining recent fault zones whicY~ significantly distort waves fields from .
explosions ~nd earthquakes. Complex and expensive systems of observations :
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are necessary for unambiguc~us determination of the nature of waves recorded
by KMPV and GSZ.
~ All these factors and also the need for rapid study of the enormous areas of
the USSR contributed to.the search for new ways and methods of seismic study
of the structure of the earth's crust and mantle.
The following trends of seismic work to study the deep structure of the .
earth's crust and upper mantle were noted over the last decade in the USSR:
1) detailed GSZ studies by subcritical reflected waves using ordinary explo- ,
sions (2. V. Litvinenko, N. I. Pavlenkova, V. B. Sollogub and others); 2)
regional point G5Z soundings (N. N. Puzyrev, S. V. Krylov and B. P. Mishen'kin)t
~ 3) regional investigations using explosions (Ye. A. Popov, A. V. Yegorkin,
N. A. Belyayevskiy, V. Z. Ryaboy, I. S. Vol'volskiy, B. Vol'volskiy and
- N. I. Khalevin); and 4) regional seismological investigations using mobile
stations by P and S. waves (I. L. Nersesov, A. S. Alekseyev, T. G. Rautian,
A. A. Lukk and others) and also by PS waves (N. K. Bulin and Yu. I. Sytin).
The development of seismology and seismic prospecting and the need to combine
them for more detailed study of the structure of the earth's crust and upper
_ mantle with a significant reduction of the cost of seismic studies and the
use of a more extensive class of waves led to the development of yet another
trend--complex seismic studies with the "Zemlya" device. It was proposed
by using these investigations to simultaneously study: 1) the spatial posi-
tion of the interfaces of the earth's crust and uppar mantle by almost vertical
. rays with an accuracy not below that of studies with KMPV and GSZ; 2) the
velocity characteristics of the crust and upper mantle from P and S waves;
and 3) the seismicity of the crust and mantl~. Among the existing classes of
~ waves, only longitudinal a~nd transverse waves reflected near the point of the
- explosion and tr.ansient composite waves from far earthquakes* satisfied the
first condition [6,18, 20,19J. But waves reflected from the surface of the
basement and deep boundaries of the crust near the point of the explosion were
usually not recorded during IQ~'IPV and were very rarely recorded during GSZ
studies [511. The possibility of recording and separation of composite waves,
- especially from the deep interfaces of the earth's crust, on recordings from
far earthqual~es was subject to extreme doubt or was absolutely rejected by a
number of seismologists and seismic prospectors [3, 4, 31]. However, the
first experimental studies conducted with the "Zemlya" apparatus to select
~ the required class of waves on an area known from deep drilliny and GSZ data
showed the reality of existence of deep transient composite PS waves on re-
cordings from far earthquakes [124]. The rather~simple method of recording
these waves in the absence of any expenditures on their excitation and also
the possibility of statistical accumulation of recordings from different
earthquakes made it possible to select composite PS waves as the main ones
- when studying the interface relief of the earth's crust and upper mantle.
*
Earthquakes were separated into far, near and local from the values of the
epicentral distances 11 . The values of ~ at short distances from the foci
are measured in kilometers and.those at great distances, where the earth's
sphericity begins to be reflected, are measured in degrees. For local earth-
quakes, 1~ = 0-40 km, for near earthquakes 4-500 km (0.4-5�) and _
= 5- 10� and for far earthquakes d= 10-180�
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Table 1. Distribution of Investigations with "Zemlya' Devices by Regions
and Years
HoMeP ~ rou~3 ) ~4 )
~q0p4 PaAos uccneAoaaex8 uposeAesan OTBCTCT88llRE[Q ACQO]I8ll7'BJ36
n0. ~ - pabor
~1 ~
t IOro-Bocxox ~ PyccxoH una~ 4962 A. H. Moasi
~o, II. B. IIo-
2 c~~pa~ l963 a~epaa~esa
3 IIIp~cacusiicxa~ BnaA~a 1965 A. H. Moasxe~co, N. B. IIo-
p (7) I I n~epauuesa (6)
4 I 1966 M. C. 3pos6ypr (g]
5 ~ J~aeupoecxo-Aoaeqxasi nua-I l966 I f1. m. By6nIIic (10)
~a (9)
6 BocTO~ax C86apa t 11) 1964 JI. II. Tp~aIIOSa (12 )
7 1965 B. E. Iuep6axuHA ~ 1~~
~3 l966
9 ~ i967 ~
l0 i966-1967 I'. B. Hpyucxarc (13a)
i! l967 A. j~. IIyraq (14 )
12 1967 H. M� 1uTYTC?a (15 )
13 ' 1968 a
!4 l963 A _
, 15 Aaoso-F{y5ascxaa sua~a 1964 YI. B. IIo~epauqene (17)
, ~s .(16) 1965 I C. C. Tapaces~ (lF3)
H. B. Tpary6oHa ~19~
17 1966 I s
18 Cesepo-l'ep~ascxasc BIIap~a 1988 N. B. IIoa~epa~esa, B. JIanre (21) ~
~20~ A. H. Moaxcesxo, B. nanre ~22~
!9 l969-1970 �
- 20 3aIIa~ns Cx6apa ~23) 1961968968 I0. ni. ;e~snc~ (24) -
::2 , 1969 �
~ ''3 ' l870 a
''4 ~ 1972 B. Yeha,nea (25)
2S i972 r
26 � I SRIiBpIIaTbB (26) I 1967 I B. II. Pyu~cuu (27)
2? l968 ~
?8 hian~ Hasxaa (28) 1967-1968 T. B. Erops~a (2g)
29 1~370 �
'U 197i ~
3i. ~i972 a
32 1973
33 1970 M. C. 3peH6ypr (30)
3~i IOr Typascxoic nnx~sa~~ IIpeR-~ l9fi4-1987 B. ~I. JJ~xoa '(32) ~
- xoIIgrRarcxBii IIpora6 I
_ (31) =
[Continued on following page]
r
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- Table 1 (Continued)
- (33)
35 IOr TypA~cxoii nnaT~a, IIpeA- 1967-1988 A. A. M~ss (34)
36 houernarcxui~ npornG l968-l969 B. A. Searo~toe (35)
g~ I i969-1971 s
38 Ya6excxes CCP (36) i96f,-i967 M. B. IIoxepa8ueea (17)
gg i968 JI. C. IIIy~~a ~ 37 )
- l967-i969 B. M. IIex
4i l9G9 C. B. Mo 3S oHa ~39) _
~ i970-1973 E. M. B}*mscxau ~40)
43 HaaazcraII (41) ~ i964 B. CT}7;e~ (42)
~ 1965 JI. M. JIbtc~tos (43) .
45 1966-i967 M. C. 3pes6ypr
- ~ 1968 s (44)
47 1969 s -
~,g 1970
49 i97i K. A. IIoaos 5 ~
Key :
1. Number of region of studies 25. V. F. Chekalev
2. Region of studies 26. Transcarpathian area
3. Year of investigations 27. V. P. Rudnitskiy
4. Responsible executor 28. Minor Caucasus
5. Southeastern Russian series 29. G. V. Yegorkina
6. A. N. Mozzhenko and I. V. 30. M. S. Erenburg
~ Pom~rantseva 31. Southern Turanskaya shield and
7. Pre-Caspian depression Pre-Kopet-Dag trough
8. M. S. Erenburg 32. V. I. Lykov
9. Dnepr-Donetsk deprAssion 33. Southern Turanskaya shield and _
- 10. Ya. F. Bublik Pre-Kopet-Dag trough
11. Eastern Siberia 34. A. I. Minin
12. L. P. Girshanova 35. V. A. Bezgodkov
13. B. Ye. Shchepbakova 36. Uzbek SSR
13a. G. V. Krupskaya 37. L. S. Shumilina -
- 14. A. D. Pugach 38. V. I. Pak
- 15. I. M. Shtutin 39. S. V. Mogil'nikova
16. Azov-Kuban' depression 40. Ye. M. Butovskaya
17, I, V. Pomerantseva 41. Kazakhstan
18. S. S. Tarasevich 42. V. F. Studenikin
19. K. V. Trigubova 43. L. M. Lysyakov
20. North German depression 44:-~' M. S. Erenburg
21. I. V. Pomerantseva and V. 45. K. A. Popov
Lange
22. A. N. Mozzhenko and V. Lange -
23. Western 5iberia -
24. Yu. M. Chemyakin
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Longitudinal P and transverse S waves on recordings from local and near earth-
quakes and explosions were used to determine the velocity characteristic and _
seigmicity of the crust. The nature of these waves was established in seis-
mic prospecting and seismology by theoretical and experimental investic~ations
of the last two decades [1, 2, 38, 39~. For complex three-dimensional in-
terpretation of the P, PS and S waves excited by earthquakes and explosions,
it became necessary to record them by a three-component apparatus which made
it possible to clearly tie in the kinematic and dynamic parameters of differ-
- ent waves propagated in three-dimensional media. This capability was realized
by the "Zemlya" apgaratus with magnetic recording, developed by A. r]. Mozzhenko
- in 1957. This device has frequency and dynamic bands adequate for simul~aneous
recording of explosions and earthquakes, high amplification of seismic signals,
good resolution, reliable dynamic calibration of the entire record-playbaclc
channel, the capability of multiple repetitian of the reported signals to
select the most optimum conditions for determinata.on of useful oscilla~tions
- and so on.
Facperiment,al studies on development of the complex seismic method of studying
the structure of the earth's crust and upper mantle using the "ZemZya" device _
were begun in 1962 on the Southeastern Russian series on KMPV and GSZ pro- _
files of past years [124] and the same studies were then carried out on KMPV
and GSZ profiles in the Azov-Kuban' (1964) and the Pre-Caspian (1965) depres-
sions using data on the velocity obtained by these methods. Subseguent in-
vestigations with the "Zemlya" apparatus in the region of TashJcent and in the =
German Dem~cratic Republic were carried out without using I~SPV and GSZ
materials [109, 111].
Studies with "Zemlya" stations begun in 1964-1965 within the Irkutsk ampi-
- theater [126~ and inother regions of the USSR and also abroad (I'igure 1,
Tables 1 and 2). The total length of profiles developed during 1962-1975
by "Zemlya" stations comprised more than 20,000 kilometers
During this same period, the "Zemlya" apparatus complex, initially consisting -
of five recording stations and one 4-channel reproduction station, was supple-
mented by. surv~y and marking reproduction stations and an SS-24-61M station.
As the method of observations and interpre~cation of materials were developed,
ever greater requirements were placed on the recording and reproduction ap-
paratus, whi.ch inevitably led to improvement of it. Thus, the need to re-
produce P, S and PS waves of different frequencies determined the appearance
of multichannel reproduction; time correlation of data obtained at di~ferent
- stations dispersed in this space resulted in introduction of a radio channel;
the need to use the dynamic parameters of the recorded waves in.interpretation
- of materials led to the introduction of relative channel calibration; it was
necessary to record precise time checks transmitted by radio broadcast stations
and absolute calibration (by displacement) of "Zemlya" channels to compare the
materials recorded by "Zemlya" stations and by ordinary seismological apparatus.
CDC-3300, 5igma-5 and other computers were used for better separatioz~ and cor-
relation of the PS waves. The parts from which the "Zemlya" stations were
designed were changed. Amplifiers based on micromodules and integrated
circuits were developed instead of tube amplifiers.
. ~
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o Z
��r .
I `
N
~ N
~
- ~
a
C ~ ~ Id
a ~
, ~ i I
, ~ ~ ~r ro~
r w _
_ ~ i , ~
~
0 Q ~ ti~�~^~ , N ~
'y ' ~p ,~~b v � ~ A ~ ' -
~ n
~ 1 ro v
O v'i ~ ~ Q j ~ N
. p ~ = Y ~ )3-~ ~ 1 ~ ~
Y $ ~ p ~ y ~
a J
- ri � ~ � Z ~ ~ A N -
~ ~ Q v+~ , N W
W z e ~t , a~o
4 ~ ~ I w o -
,s ~ _
.
Q M EHU^eu ~ Y ~ , a~
~ iN o Q" ob~ vr~ w
u N ~ ~ ~m �E O
l ...o OL �ri FI
o e~' ~a e mp~~ i ~ a~
~'i ~ -
v o` ' t o ~
i,,
_ N ~ ~
y ~ ' .r''
~ d F ~ N ~ _
'y, /~i W s(' +~I 4-1 rl ~O -
~`ti .y~- . ~ ` a . ~ 4~-~ a
t.ti
~ ~a,~~ Pq, ~ ~ ~ f ~ ~
~
< P ~ p' 3
- G'~~ pQ~ ~ Q 1 ~y i o .
~ e� ~ ~ a ~ i ~
m ~1 a~ rP aN ,.i ~ p
a Q ~ 0 o. , � w
o.. ao v o . y -
~ ~3071~ ~ ~
v N j W v O yy
G, ~ ~
" 1, ~oY S ^ y ~ A 3 b~ .
A9yy~X~ ~ P g~1 w u
~ OQ~ ~
n ~,,,J`~ ~',u' 4 E Q~10~' c., '
7
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.
~
Key:
1. Arctic Ocean 13. West Siberian series
- 2. Baltic Shield 14. Anabar shield
3. Leningrad 15. Siberian series
- 4. Eastern European series 16. Lena River
5. Moscow 17. Yenisey River
6. Ukrainian shield 18. OU' River
7. Kiev 19. Novosibirsk ~
8. Volga River 20. Irtysh River
9. Black Sea 21. Turan platform
10. Caucasus Mountains 22. Tashkent
11. Caspian Sea 23. Aldan shield
12. Ural Diountains
All the most improved methods of field investigations by I~IPV, GSZ, rIUV
[Reflec~ed waye method] and seismology were used when working out the method.
The recording stations were faced by profiles and area with spacing whicli ,
- permitted phase correlation of waves of different types. The presence of
cor~elation stations made it possible to correlate material obtained at
different stops and profiles with each other. P and S waves from explosions
were correlated by conjugate points and PS waves were correlal-.ed by i:he
_ ~ times and regions of their common points. Simultaneous recording of waves
from.explosions and earthquakes was carried out. Seismological procedures
on spacing the stations around foci were used during observations of earth-
quake foci with specific ratios of epicentral distances to the depths of
the foci ( ~/hoch~ and seismological calibration of sEismographs and chan-
- nels was carried out according to the polarities of wave arrivals. 7.'he main -
data on the method of field observations with the "Zemlya" device iii different.
_ regions are presented in Talale 2. ~
The methods of study and interpretation of various waves and primarily of
_ composite PS waves were improved simultaneously with developmen.t of field
_ studies. 'Phe dynamic and kinetic characteristics of PS waves [52-54, 58,
- 72, 73, 90, 134, 152, 163, 1.65], methods of separating t,'~em on recordings
_ and correlation from station to station (7, 20, 86, 96, 110] and absorption
of P and S waves [146] were determined. Methods of determining the velocity
- characteristic and seismicity of the crust by P~and S waves [8, 22, 36, 70,
77].and PS waves [9) were developed. Methods of interpretation of PS waves
for horizontally layered [6, 18, 19, 49, 50, 78, 108, 135] and complexly
structured media with inclined interfaces [111] were improved and deveJ.oped. -
A comPlex seismic method of studying the structure of the earth's crust and
upper mantle by longitudinal, transverse and composite waves excited by -
earthquakes and explosions and recorded by the "Zemlya" device at epicentral
distances of 0-160� in the frequency range of 0.5-15 Hc was~developed as a
result of many years of investigations with the "Zemlya" device, carried
out in di�ferent regions of the USSR. This method was named the "Zemly~a" '
method for brevity of outline according to the naminq of the apparatus used.(
It combines the method of transient composite waves from remote earthquakes~:`=
$ ~
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Table 2. Main Data on the Method of Field Observations with the "Zemlya"
Device in Different Regions
( 3) (4 ) 4~+cno uoneaxaz ei~~ce0 aa ! 6 cyr _
~
~ -
m
a ar asecrnmx ar ~tanex~sz
~ 2 ~ ~ a 6n~~axux
~ or eapmeoa aeesner sce- aemnerps-
CRY�0$
~1~ PaAoex~xne- ~ ' (6) (7) ~ (8~
Pernoa Aoeaxx0
5 ~9 :.(9) (~0) ~ (9 ~0~
am ~ a~ e~ ~ ~ m
(5) ~ ~
w~ o s
= dq o b cs.t0 n i.~ ~ -
o,~ ~ a~c ~d ~w ~d $,wc Gad
r~iC w Wa. oK ~wo~ 09 ~0. oC
_ ApeBa$e 1~ IOro-g~
ax~x 1,2 30-60 27 4 8-13 4-i3 i8 I B-i5
- nnaxcpopnua Pyccxo"s
nnazc~opbu~t ~
BH~^rpII n3 IIp~cac - 3, 4, 5 3-50 i-23 i 6-7 ~!-5 2i 3-i3 =
~unaxc~opMe~= cxast S
~e AseBposcxo-
Hnw~$a~ Aoaeuacax (15 ) -
BII~H
goc~ro+~ax I 6-14 i3-43 i-24 1-6 1-24 i-6 3-36 !-i6
Ca6Hpa
c16) ~
Aaosa 15-1715-4i 2~-3! 4 2-4 2 8 6-$
Ky6escxax
Mon~~l ~e~a `
~a~oP~ ,
Cesepo- !8, 1916-29 2-3 ~3 7 - i4-28 l3-i5 -
Tepmascxasc
Hna~pasa
3anatQaas 20-25 5-24 - - - - 4-?.4 2-ii
Ca6$ps ,
(20) ~ t
3axapuaxae 26, 27 4-10 3 3 - - 6 3
{22)
(21) ~
Cei~ca~o- Mam~a 28-33 44--70 6-i8 2 24-42 6-i614-23 6-i2
auraaeue HaBxaa
- paeoau ( 2 3 )
Typxece~x 34-37 7-70 - I- I 53 I 5-6 i8 I 2-i31
(24) I I I
*Long-term observations were made to study the seismicity of the region
[Continued on following page]
, g
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Table 2. (Continued)
_ (2 8) (30) ~32~
� (31) ~
~27~ `2tl, x~ ~ -
625) (26) " p ~ H�' a
Cac'e@Ma paCC2a- BH~ ~ �m 00 ~ o~ ~
aaatce cxaa~ct9 accr~e2onaxng c o ~ p h x
aa~c$ ~ ~ ~ ~ ~ a a
~ ~ a ~
~p ~j O V fJ ~ b
~ T
o ~4 �a
F' o~~ ~ c~ o ei
.7 -rit~Sc~i ~ ~ix U~ UF
IIo npoc~~a3n~ Poraoaa~tssue 10 13-14 4-9 - - -
c ar~ocsr~s ( 34 )
' cxaa~s~a
IIo npoc~unxaa PerROSaubs~te 3-8 14-20 6-15 5 2,9- 0,43-
c B~socss~nin ~g4~ 3,8 0,49
_ CTflHI1,HHMH
(35)
~ IIo ata~mp3*ra~ Pernoaansabie 3-12 15-44 5-20 1,5- 2,0- 0,2- -
c ~saaoca~ 5,i 8,4 0,9
cTa~s~$
IIo npo~isns~ Peraoaa~a~te c Re- 4-7 14-27 9-12 1,2- 2,4- 0,3-
c e~ocas~ui Talmaan~xeR o~r . 3,3 4,4 0,9
- c~ra~t APn*-~' y+tacr
(35) xos (37) -
IIO II~10~111JIAM PerIIOSanaaue c Ae- 5-6 16 9-25 2,0- - -
C H6iHOCH6lMII T8JIE3flI~iteH OT- 5~9
CTBHI;H~ci~ R2IIbHbi ( y~jCTIfOH
` 3
IIo xapm[pyTa~, Pexoraocc~poaoe- 2-6 16-45 5-l5 1,6- 4,6- 0,8- -
irno~a~, $~e, pericosans- $ Go- 3,7 14,1 1,1
H arAer~sbtx aue, Rera.-~a~e nee
T0'~~ (38~ i39)
IIo IIpo~sns~i Pexorsocn~aposoe- 0,8? 11? 3-6 0,3 2,4? -
H arAenaauz srae ( 41)
xo~ncaa ~40
. .
IIo upoc~ans~ Peraosa~~e c Ae- 5-6 25-38 5-10 1,4- 2,9- 0,5- -
c H~ocHbrasa Taaaaamaeu ar 13 135' 1,9 3,9 1,6
cTaa~sn~ Re~aux ysaaT- 0,5 � 31,3 *
. x%~a, Aom~oBpe-
~36) ~es~es ~42~
_ IIo npoc~~:~scn~ peraosa~ar~e 3-5 22-50 5-10 0,8- 2- 0,4-
- I c a~aoca~Ma I (34) I I I I 1'6 I 4'~ I ~'s , -
CT8H~HSMLi
(36)
[Continued on following page]
ia
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Table 2 (Continued)
~~+cno noaeaxxx sauKCeil ae f 5 cyt
C
_ ~
a OT MCCTHdI O7 pBJICKN= -
y it 67IH8i(HZ 3gMI1ETpACE'
~ Oi H3p61H0H 8eHneZpq- ANOI _
paC~of+ nccae- _ cexxR
Pe~umt Aoa~nnp ~
o ~ ~ _ 1 ~
x
z.. c~, ~ �'a F ~
o'K ~3 0 �x o
m~ o Fr tO `e~a m ~'n ~
. F� L v Q ~ Q ~ ~p G 6) ~~y
C.. r C 1O~ e4fr' 10~ GC 0~
~+C P n= C.. nG oS n-^. _
~'3UeTiliCTAII I38-42 6-69 8--i1 2-4 2i-30I 2-4 i0-32 4-10
(21) ~43) I I ,
Ceit cvoa~:rn A-
xbie patiotis~
HaaascraH 43-49 26-97 2-i6 2-4 26-8i 20-3610-38 l2-20
(44)
. 4z
n� ~ K
~ m m z~o s
~ . ~ h F�,
- Cec4era peccTa- BnA '4 n~ ~ x o 3 s~
xostcx csaeu~+~ NCC7ICA088HNII m a o Y F ^
BaIIxCN ~ ~C~ a ~ pGV� o a ~ . .
Fp F a aG EC
p V ~ U d :7
'A ox 0 BT Xa ~G
~
4 O�' U ~ p1~j~ O V -
~ qes~ Gc ci~ ~E
IIo aiapmpy5~r~~t, Pexor~ocy~poBOe- 3-l0 21-13 8-15 1,1- !,7- Q.3-
a~te, peraoaam.- 2,8 3,8 0,9
~t~~ a~e, Reraucbar~e
IIo IIpoc~sn~ Perao$a~sxe, ~e- 5-i! 15-30 5-15 1,4- 2;4- 0,9--
B arRe~sbu Ta~aue, Aonro- 80-350 � 3,4 9,3 2,2
Ta~ntax epeue~e ~
(40) (46)
[Key on following page~
11
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P~y :
~.r
1. Region 31., Cost of a si.ngle observation -
2. Region of inveatigations point, thousand rubles
3. Number of region of inveati- 32. Cost of one kilometer of
gations according to Table 1 profile, thousand rubles
4. Number of useful recordings 33. By profiles with portable
during 15 days stations ~
5, Total 34. Regional
- 6. From explbsions 35. By profiles with portable
7. From local and near earth- stations
quakes 36. By traverses with portable
8. From remote earthquakes stations .
9. Recorded 37. Regi.onal with detailing of =
10. Processed individual sections _
11. Ancient series 38. By traverses, areas and at ;
12. Southeastern Russian series individual points
13. Depressions within a series 39. Preliminary survey, regional -
14. Pre-Caspian depression and detailed
15. Dnegrovsk-Donetsk depression 40. By profiles at individual -
16. Eastern Siberia puints ~
17. Young sEries 41. Preliminary survey
18. Azov-Kuban' depression 42. Regional with detailing of
19. North German depression individual sections, long-
20. Western Siberia term
21. Seismically active regions 43. Uzbekistan
, 22. Transcarpathian area 44. Kazakhstan 4
, 23. Minor Caucasus 45. By traverses, profiles and
24. Turkmeniya areas
25. System of arranging recording 46. Regional, detailed and long-
stations term
26. Type of investigations _
27. Spacing of observations, km
28. Length of abservations on
_ one spacing, days ~ -
29. Number of recordinq stations -
, 30. Productivity of operations,
km/day
I and methods based on the use of longitudinal and transverse, refracted and
reflected waves from explosions and earthquakes. The following problems
can be solved by using this method. , _
1. The deep structure of the crystalline thickness of the earth's crust
and upper mantle can be studied, beginning from the surface of the crystal-
- line base and ending with the interfaces in the upper mantle. The structure
of the interfaces in the sedimentary mantle can be determined under favorable
conditions.
_ 12
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~
- 2. The velocity characteristic of individual complexes of the earth's
crust and upper mantl~ can be studied.
3. The coordinates of earthquake foci and the velocity characteristic in
focal zones and also the mechanism and energy characteristics of f.oci can
- be determined.'
~ 4. The relationships existing between the deep structure of the earth's
crust and displacement of earthquake foci can be established. -
Investigations by the "Zemlya" method conducted on the Southeastern Russian
Series, in ~the Pre-Caspian, Azov-Kuban' and North German Depressions and in
the rayans of Tashkent made it possible to obtain essentially new data on
the deep~structure of these regions compared to the results of study of thezn
by I~IPV, GSZ and seismological methods. Thus, weak tectonic activity of
this region and the adjacent folded system of the Urals was detected during
investigations on the Southeastern Russian Series. Besides the crust inter-
faces in the Pre-Caspian regions, the roof and bottom of the salt-bearing
mass in the sedimentary mantle were traced in Pre-Caspian regions along the
interf~ces of the crust and the position of the~boundaries inside the crust
= was determined. The narrow, but deep (up to 20 km) West Kuban' Trough not
determined by KMPV, was established within the Azov-Kuban' Depression along
the surface of the basement represented by a Triassic-Jurassic mass. Accord-
ing to KN~V data, the depth to the surface of the basement within the West
Kuban' Trough comprised 12 km. An idea of th~ detailed deep structure of
the crust was obtained for the first time in the rayons of Tashkent and the
distribution of epicenters and depths.of aftershock* foci of the Tashkent -
earthquake of 26 April 1966 was determined with high accuracy. Reduced values
(4-4.4 km/s) of stratal velocities ,(vpp1) of longitudinal waves and ratios
(ICpi) of stratal velocities o~ longitudinal and transverse waves (up to 1.61)
were discovered within the focal zone located in Paleozoic and Archean base-
ments at a depth of 3-9 km, whereas vpPl = 5.8-6 ]rni/s and Kpl N 1.73 in the
zone surrounding the earthquake foci. It was established that the foci are
- located in a weakened zone of the crust.
A complex heterogenic structure of the basement was established for the -
North German Depression and a three-level arrangement of the folded phases
in it was determined: Variscian, Caledonian and Pre-�Cambrian; the deep _
structure of the northerr, part of the Ger.nan Democratic Republic was det~r-
mined; and a series of structures along the surfaces of different phases of
basement folding and deep interfaces of the crust was determined. It is shown
that the Eastern Elba gravitational maximum is caused by an uplift of the
basaltic and subcrustal layers, while the magnetic maximum is caused by
effusive-intrusive formations which fill the trough along the Pre-Cambrian
folding.
*
Tremors following a large earthquake from the same epicenter, less in in-
tensity, are called aftershocks according to H. Jeffries.
13 ~
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The resalts obtained in aseismic and seismically active regions permit one ~o
use the "Zemlya" method to ~tudy the structure of the earth's crust, the
upper mantle and their seismicity both autonomously and in combination with
other geophysical methods.* .
* _ _
The authors are grateful to M. K. Polshkov and Ye. F. Savarenskiy for sup- . _
_ port and supervision in workinq out the complex seismia method of studying
the structure of the e.arth's crust and upper mantle and to A. M. Yepinat'yeva
and T. I. Oblogina who reviewed the manuscript and made many valuable
comments.
, 14
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PART 1
THEORETICAL FUNDAMENTALS OF USING DIFFERENT WAVE FIELDS TO STUDY
THE STRUCTURE OF THE EARTH'S CRUST AND UYPER MANTLE
,'i
PHYSICAL CONCEPTS ABOUT LONGITUDINAL P, TRANSVERSE S AND COMPOSITE PS
_ WAVES ON RECORDINGS FROM EARTHQUAKES AND EXPLOSIONS
Moscow SEYSMICHESKIYE ISSLEDOVANIYA S APPARATUROY "ZEMLYA" in Russian
1977 signed to press 31 Jan 1977 pp 14-34
[Chapter 1 from the book "Seysmicheskiye issledovaniya s apparaturoy
'Zemlya by I. V. Pomerantseva and A. N. Mozzhenko, Izdatel'stvo Nedra,
_ 1,400 copies, 256 pages]
[Text] Wave Fields Observed During the Initial Part of the Earthquake
Seismogram Recording
The Kir.~~:atic C.haracteristics of Wave Fields
According to Seismological data [43, 48, 132], LR and LQ surface waves,
longitudinal (P, PP and PPP), transverse (S, SS and SSS) and composite
(PS and PPS) waves refracted singly and multiply in the crust and mantle,
for which the multiplicity boundary is the earth's surface, longitudinal
(PcP), tr~nsverse (5cS) and composite (PcS) waves reflected from the core, -
- transverse waves re�lected from the earth's core and surface (ScSP), longi-
tudinal and transverse waves which pass through the earth's core once (PKP _
and SKS), twice (SKKS) or three times (SKKKS), waves reflected from the
earth's core, its surface and which pass through the carv (PcPPI~, PcSPKP
and ScSPi~) waves reflected from the earth's core and surface and refracted _
in the crust and mantle (ScSP) and waves which pass through the earth's core
once (SKSP) or twice (SKSSK3) and reflected from its surface once may be =
propagated in the earth from the hypocenter to the recording station at
- = 0.180�. Photographs of all these waves, compiled by Jeffries and
- Bullen on the'basis of analyzing a large number of experimental recordings
from earthquakes, are presented in Figure 2 with regard to a number of theo- _
retical calculations.
The first P waves on the Jeffires-Bullen hodograph (Figure 2) at ,0 = 0-110�
- are c~lassified by their nature as refracted in the crust and mantle. Dif-
fracted P wanes may first be traced ~'urther at 130-150� or a shadow zone
will be abserved at this range of epicentral distances [84, 132J. The first
P waves are refracted in the core (PKP) at = 150-180�. Moreover, in the
initial part of the seismograms according to the Jeffries-Bullen hodograph _
r, 15
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t Q ZO 40 60 80 i~70 iZ0 l40 160 18 50
MH~i ~
(1)
- 45 ~
. S~,S
~ S~S
p0 v v QQS 40
SGSP~cP
~ ScSPKP 35
Q`' S~SP
Q
" 30 . 5 psSPKP 3Q _
~ S~,
~KS PPKP
S
15 Qe S~g P~5 25
pKS PKS .
P~CP
20 QQQ PKP 20
y Pr,r~4A~
SGS Q Qq ( Z1pog4d
~ /5 u a ~ 15 -
Acs P a ~
5
10 pG p 10
. Q
S ~ S
. ~ (3) -
20 40 60 80 100 tZ0 140 1604,rpa,qyc
Figure 2. Jeffries-Builen Hodographs at hoch = 0 and
- Q = 0-180�
- Key:
1. Minutes 3. Degrees
2. Diffracted
- and according to [6, 20, 48, 65], the existence of composite SP and PS, trans-
_ verse S and reflected pP and sP waves related to the interfaces of the earth's ~
' crust, the upper mantle and the focus, is possible after the first arrivals
of P and PKP waves. The PS waves related to the interfaces of the earth's `
crust at thickness of 70 km and mean velocity to the Mohorovicic discontin-
uity of 6.2 km/s are recorded on earthquake recordings not less than 11 sec-
onds after the first arrivals of P or PKP waves. At Q= 0-5� and hoch < ;
- 25 lan, sP, pP and S waves related to the .focus are recorded in this same
time interval [65]. With an increase of A. and ho~h, sP, pP az~~ S_waves are
16 -
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recorded at ti~s greater than the times of recording PS waves, as a re-
,sult of which a zone of the absence of any waves related to the earth's core ~
and mantle is observed at the first P and PKP waves. Z"his zone is optimum
_ for recording PS waves formed at the interfaces of the earth's crust.
The nature of P, So sP and pP waves related to the focus has be~n studied
rather thoroughly by seismological investigations. The sP and pP waves are
~ related to composite-reflected and reflected waves in the region of the
focus. They emerge from the focus as S or P waves, are exchanged and re-
flected on the earth's surface and are then propagated to the reception
point as longitudinal waves. S waves are transverse types formed as a re-
sult of shearing processes at earthquake foci.
The matter with the nature of PS waves recorded on the horizontal components
of the recording immediately after the first P waves is more complex. A
- number of investigators (Ye. M. Butovskaya, S. S. Andreyev, N. K. Bulin,
Yu. I. Sytin, N. V. Shebalin and D. N. Rustanovich), who suggested that PS
- waves be used to study the structure of the earth's crust, feel that they
are composite waves which replace a P type for a S type at the interfaces
of the earth's crust and upper mantle. Others (I. L. Nersesov, Ye. I.
G~1'perin, G. M. Tsibul'chik, I. K. Klushin and others) assume up to tk~e
present time that these waves by their nature may be: 1) pS multiple waves
related to the upper ~lev~ls of the sedimentary mantle and incorrectly in-
terpreted as deep composite waves [32, 35]; 2) various types of longitudinal
waves recorded due to~.their own large angles of emergence on the S and Y
components [82, 91, 161]; 3) lateral waves of Raleigh type formed from P
waves on large uneven areas of relief of the earth's surface and propagated
along it for great distances [31]; and 4) additional arrivals formed due to
the presence of "projections" and "hollows" on the surface or the P wave
fronts during their propagation threugh an inhomogeileous medium from the
focus to the interface and unrelated to the crustal boundaries [62].
The first hypothesis was based on concepts of the low intensity of transient
PS waves (from the first erroneous theoretical calculations as was later
- established) and the high intensity of multiple P and S waves in the sedi-
mentary man~le (from MOV materials).
- The second and third hypotheses were based on the fact that the polarization
planes of experimental PS waves recorded on recordings from remote earth-
quakes frequently deviated significantly from the vertical plane passing
through thP station-epicenter. Theoretical calculations which indicate the
possibility of additional arrivals of different waves appearing which are un-
related to the interfaces of the earth's crust and mantre and formed due to
curvature of the P wave fronts in complexly structured media were the basis
. for the fourth hypothesis. The hypothesis on recording of Raleigh wave com-
ponents formed from P waves on unevennesses of the earth's surface on the
X and Y components is hardly probably for series.conditions. Thus, it is
shown in [61] that Raleigh waves at frequencies of 1-2 Eiz at excesses of the
earth`s surface of 0-400 m above sea level may create only a general micro-
_ seism background of intensity less than 7 percent of the P wave intensity
and consequently 4-10 times weaker than PS waves on the seismograms. These
17
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~ ~
o b i m
~ .m ro 1~ H N O I H ~
~ W H N I'J 41 I 1 rd f-1
~1 ~--I H iJ 1 ~ dl H~'i (d N ~t
N fr' �Ul ~ H r~ (d ~ ~A ~ ~ 'J h ~ ~
� -
A~c~n ~ w+~ ~ i a c~i a x 3 ~ = -
~ +~a~~roH ~ ba,+~ - _
w ~ b v~ H a~ ni w+~ cn ~ -
~ � ~ w a~i= ~ ab a~i~ o~+-~ _
a~ ~n a m o ~ a o ~ -
~ .ra a~ b ~ ~n ~ ~ ~n ~ _ ~
> ~i' ~ A ai i ~ o ~ N _ ~
bbro ~~~c~~ va~~ _
3+~ cn ro~s H w o a~ ro a =
3-~ N ~ N~ N 4-i A+~ �~I b N -
- p'J+ fJ1 G! N�.~I tC i~l 1 r-I I ~ -
z ba ~ aaA ~ ui a~v i i ~4 =
p; �~-I I 0 - 1A U ~ ~ N ~ _
w rob i ro ~ b~+~~ ~ ~
O W q 41 H N I H 4-I RS 'd' ~ ~
p Rf tA H rl H I ~I ~1 r-I I ~1 N
'u H (d 'J 'd Rf a3 ,sC ul W -
a w u ro ~n a~ s~ r+ w y
~a~x~~aoH~n ai+~~3 -
w a~ a~ a~ v i a~ ~ ~n a -
o zs r+ v~ ~ ~rs ~p b ~ ~ ~
~-t b~~ w N u~i b~ tn 3 o t� o ~ =
w o o a~ ~n ro,~ ~n b a -
~d U U~ rtf A+~ O w w N N N N~
~roHa,~~~r~s~~a~bx~ib ~N _
~-1 ~f~ (0 ~3a N .t'. ~ ~ td w ~ ~ N ~
`Y' vi�i a`di ~ ~ ~d a a~ ~ h y _
~ ti
~ a~i 'Q ~ v s~ a~i ~ ~ rt .u ti,~ ~
~ ~ ro a~ ~ aai ~ ~ ~ 3 ~ ti s -
i rtl v 3~ nd a! w cn s.~ ~
w H cn v,a~+~ ~ v, oa u -
a � - _
r ~ ~ _
� v ~ a' g h +c
' Vf ~ 0 0 n~ S ~ o ~ ~ , 1 b _
~ H ~n ~ ~ c~' =
h v~ h N y, h v~ b b
q ~ ~ O O O C C p O O ~ ~
f b, ~o b'n kf N H
v n ~o ;e cv
~ o 0 0 o c p c o Q t - N
~ f . . h h ' ~n ~ ~ ^ ~
N i i~ ~ ~ ~ iF ~f h b ~ ~ ~ ~
~ ~ O p O O O O O 0 ~ ~ ~ ~ ~
1 .7 7 Q Q y~ vf ~O ~1
~ f C O O Q O O O C O ~ ~ ~ ~
~ a ? v 'p ^ -
n O p p o~O C o O ,~O ~ c.~
tl b ~ ~
N ~ Q ~ e0 ~ = ~V ~ ~
y 0`, t~ ~ 0 m ` ~ n~ ~
~ _'1 p ~ ~n b oi O ~e
- ~ N N c~ M. c~i '
f' 'K
"7
~ ~ n ~p ~ ~ n
Y b ^~cf tp ~ ~ "7 ' ~ ~ ~ ~ ~
� l~ t(~f' ~C . ~ ~ C` ~
~ ^ ~ ~
` _ ~
~ ~ O ~ ~ ~ _ _ _ _ s
. ~ 1 ~ ~ ~ ~ ~ a ~ _
. H ~ ~Nj' ~ ^ ~ ~ " .
_ O ~ . tp ` ~
O N ~
~ b ~ ~ ~ ~ ~ ^ 1 _1
~
_ , A
, lg
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low-intensive waves cannot be seen on seismograms jointly with PS waves.
The hypothesis of the presence of PS waves which can be caused by curvature of
- the P wave fronts would be valid if the PS waves on the X and Y components
were separated only by their first arrivals, as was done, for example, in [911.
Additional PS waves unrelated to the crustal boundaries are eliminated upon
separation of PS waves by the shape of the recording of the entire packet of
P waves.
Theoretical calculations of hodographs, forms of recording, frequency spec-
tra and intensities of transient longitudinal and composite, single and mul-
tiple waves formed at the interfaces of ~he earth's crust at Q= 0-160�
were made to determine the physics of formation of PS waves at the interfaces
of the crust and the r.ature of their propagation. The calculations were made
for models of inedia which approximate the earth's core of several regions
(the North German and Pre-Caspian Depressions, the Tashkent Depression and
the Southeastern Russian S eries). A diagram of the course of the rays of
aIl types of single and incomplete waves and also one of the variants of
anodels of these media are presented in Figure 3. -
Analysis of the theoretical hodographs of transient P and PS waves obtained
for models of inedia of all the enumerated regions showed that the existence
of the following secondary waves is possible on the horizontal components of
- recording in the time interval of 0-11 seconds after the arrivals of P waves
from the viewpoint of kinematics: a) single PS waves for all crustal inter-
faces separated with an interval of 0.2-2 seconds (Figure 4); b) comple PS -
waves from levels of the sedimentary mantle present at the times of record-
ing PS waves related to the surfaces of basaltic and subcrustal layers; c)
incomplete PS and PP5SS waves from levels of the sedimentary mantle recorded
at the same times as the first deep single PS waves related to the surface
- of the crystalline thickness of the earth's crust (see Figure 4); d) incom-
plete PPSP and PPP waves which occurred at the boundaries of the sedimentary
mantle; and e) the horizontal aomponents of P waves in the~presence of large
- angles of emergence of seismic radiation. Based on comm~n physical concepts, _
one may assume the existence of vertical and inclined contacts of inedia of
different petrographic compesition in the upper part of the crystalline
thickness of the crust [38, 39, 41, 42, 103~. These structural inhomogene-
ities of the crust may be sources of various types of lateral waves: trans-
ient difrracted and transied reflected waves recorded in the time interval _
of 0-11 seconds after the arrival of the first transient P wave [133].
The Intensity of P and PS Waves Different in Nature Related to the Earth's
Crust
Th~eoretical calculations of the amplitudes of all probable P and PS waves:
single, multiple and lateral, were made from kinematic positions to determine
waves dynamically reflected in the initial part of seismograms from earth
quakes = 5-160� and t= 0-11 seconds). It is natural to assume that _
all the waves differing from the first P and PKP waves by no more than an
order or 1.5 ~rders in amQlitude can be seen on the seismograms. Waves
19
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~
:l~''~ ~ ~ . . . . . . ~ - .
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1 2 3~4 5 6
7~
8~-p.~
10
~
f8 ~ .
_ t i~si~ i
1~r, ~ ~ .
- i ; ~i~K -
i ~ b ~
� ~ � fi 28K 39x
I Q Q
/O2 ~ i~~ I~ 31K 37K ~ ~~OK '
~I~i I~. 44 j I .
.l ~ I ~ i
~~n~+ ~ j ~ I
10'~ 3~+ ~ ~ i i Q
~ ~9K ~ I I -
I
IisK ~ j i I ' , _
ro ~ . ~ I i i
~ II ~ 1
25rt . I I I
10 - I ~
_ I ~ -
~0 6 j ~ -
I
j +
I
~a' j -
i
8 i ~2
~ l0
I ~3
APS4 + -
~ -
Figure 4. Theoretical Amplitudes Apgq/Apw for Single and
Incomplete PS Waves as a Function of ~ tps_p,
Calculated for a Model of the Crust Presented ~
in Figure 3:
1--without reqard to P and S wa~e absorption; 2 and 3--
with regard to P and S wave absorption at d p= oC S and _
o(p = 2 o(S, respectively. The figures near the values of
Apgq/Apw correspond to different types of single and incom-
plete waves, the ray of which is presented in Figure 3.
' 20
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which have a greater difference in ar.iplitudes cannot be determined on the
same seismogram with P and PKP waves without using some special procedures
of accumulation.
The amplitudes of single and multiple P and PS waves were calculated from -
the programs of T. B. Yanovskaya [166] and L. I. Ratnikova and T. B. Yanov-
skaya [123]. The amplitudes of lateral P and PS waves were calculated by the
program of A. V. Belinosova, A. S. Alekseyev and S. S. Tadzhimukhamedova
[10]. All the calculations were made both with and without regard to the -
absorbing properties of the medium in the layers of the crust. The values
of the absorption coefficients for P(p( P) and S(0( g) waves were taken -
from [146], where they were determined from experimental recordings of P and
S waves recorded by the "Zemlya" device from explosions at the same profiles
for which the theoretical calculations of P and PS wave intensities were made.
The ratios of coefficients o( p/ 0( g varied from 0.7 to 2.5. Ratios of
p( p/ oj g equal to 0.286, 1 and 2 were taken during theoretical calculations
of amplitudes. The densities G in calculations of intensity were deter-
- mined in the layer according to [167]. Theoretical calculations of the am-
plitudes of single, multiple and lateral PS waves were made for thick-
- layered models of inedia with interfaces of first kind and transition zones ~
between individual layers of the crust. Consideration of the ratios of PS -
wave amplitudes to P wave amplitudes made it possible, on the one hand, to _
eliminate different intensity of earthquakes and to construct the experimental
data on the same graph for earthquakes with different values of mangitudes and _
energy classes and, on the other hand, to avoid errors in measurements of -
amplit.udes caused by the device (see Chapter 3).
The amplitudes of single and multiple P and PS waves for thick-layered media
with interfaces of first kind. The curves of the dependents of the amplitudes
of the vertical and horizontal compon~ents of longitudinal and composite
(single and incomplete) waves are presented in Figure 5, a and b as a function
of the epicentral distance ~ and angle of drop of the P wave to the Mohoro-
vicic discontinuity iM for the model of the medium presented in Figure 3.
_ Analysis of the theoretical amplitudes of P and PS waves calculated without
regard to the absorbing properties of the mediiun for models of the earth's
crust of the named regions permits one to make the following conclusions.
1. The vertical P~^~ components of longitudinal waves have the highest ampli-
tudes among those recorded at epicentral distances of 0-160� in the time
interval of 0-11 seconds on the Z, X and Y components (see Figure 5, a).
2. The amplitudes of the horizontal components of composite single PS waves _
(Apq) recorded on the X and Y components are 1.5-8 times lower than the ampli- _
tudes of the vertical components of P waves. _
3. The amplitudes of the vertical components of single PS waves are lower
than the amplitudes of the horizontal components of the same waves by approxi-
mately ar. order.
21
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4. The amplitudes of the horizontal components of complete ancl incomplete
PS waves have a very wide range (6 orders) of amplitude variation.
5. The amplitudes of the horizontal components of double P5 waves related
_ to levels of the sedimentary mantle have the same order as the horizontal
components of single PS waves related to the deep exchange boundaries of
the earth's crust. PS waves with multiplicity factor greater than 2 have
_ amplitucles greater than one order lower than single PS waves.
- 6. The amplitudes of the horizontal compone~xts of complete and incomplete
PS wa~ves related to the interfaces of the crystalline thickness of the
earth'~ crust are approximately an orcler less than the amplitudes of single
PS waves related to these same boundaries.
7. The amplitudes of incomplete waves related to the interfaces of ~l-he
- crystalline crust are approximately an order less than the amplitudes of
_ incomplete waves related to the levels of the sedimentary mantle.
8. The curves of the amplitudes of the horizontal components of single and
multiple PS waves are identical to each other and have a dome shape with
very sloping maximum at angles of iM = 20-70� ( Q = 17-100�). Minimum in-
tensities are noted at iM = 0 and 90� ( Q,^� 180 ancl 3�) on curves Apsq.
Introduction of P and S wave absorption into the calculations significantly
alters the concepts obtained about the intensities of single and multiple P
and PS waves (Figure 5, b). Consideration of the absorbing pro~erties of
the real medium (at p(, = 0.286 oC S in the uppermost layer of the sedimentary
mantle, o( p= a( S and P p(p = 2 oC S) leads to the fact that not a multiple
wave related to the interfaces of the sedimentary mantle remains in the in-
terval equal to a single dyr~amic order with single P and PS waves. A similar
pattern is also noted for graphs Apgq/Apw (see Figure 4). The values of
� Apsq/Apw for single deep PS waves and incomplete PS waves formed at the sharp
interfaces (vP2/vpl = 1.5) in the sedimentary mantle are similar without re-
gard to the absorbing properties of the medium. Introduction of absorption _
reduces the value of Apgq,~Apw by more than ~-2 orders for incomplete,;waves.
The effect of a sharp decrease of the intensity of multiple PS waves~ywith
different combinations of QCp and D( g permits one to assume that inc~omplete
and even more so complete waves related to the sedimentary mantle are,',absent
in the wave pattern observed from earthquakes.
The amplitudes of lateral P and PS waves for thick-layered media with inter-
faces of first kind. The amplitudes of transient reflected P and PS waves
were calculated for two models of two-layered media with the presence of a
sloping contact in the second (lower} medium. The P and PS wave velocities
- in the first medium and its density were assumed constant and those in the
second medium were assumed variable with depth according to parabolic law.
The following parameters are used for the first model: H1 = 3 km, vpl = ,
_ = 2.8 km/s, vP2n = 5 km/s and vP3n = 6 km/s, where vP2n and vP3n are the
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velocities near the surface af the gradient layer (initial). The gradient -
is ~ = 4�10-2 km 2~3 and ~g = 2�10'2 km'2~3 . The source of oscilla-
~ tions2is located above the medium with greater velocity at a distance of
- xp = 16 and 60 km from the contact. The angle of inclination of the contact
cP is equal to 150�. Absorption was not considered. -
b
~ OZ ~.4 Qs ne 1,0 ~M peJllh7M _
40 50 ~60~ ~peAyc
Q ~ 1~ 140 82 65 SS G r yc
01 4 6 Q8 I, 1,4 i,pa,qi~aH ~ _
' I 1 3 4 6 6..,, 7 l rpeAYt ~2~
~40 82 ss bs ro , rpa~tyc
-
i
10 10~ e '
~B
. M
Pw ~
S ~ ~ ' ~ P ~
t 1p _
10 ~ ..~p4 ' _ ;
~
~ ? 9 a ? `A ~ ~PI~
~i ~ _ ~ ~
~
~ ~ ~ K . ? \
~ ~ i~~ 5 ~ 106 ~ 31K
~ :~z= ~ ~ i _ . ~
~ `,se~~~~___ ~ 6 _ ~ ~\~T6Nff -
JOK ,
% '�~~n~~~~ i~_~~~ ~~13K
: / i~ ~ 29K i ~ ~25K
~ j .S~%- ~~y JJBN ~ -
j ~i~ \ JIK 7 ! \ \
- ~ \ ~X 10 / /j \ \ \
~ ~ ~ 3K
- ~j%' ~ ~ ii~"r=a ~ ~ ~ -
~ i 16x , ~
j~j~%:= ~W~,~`~~ ~
9 r i i , . t
10 ~ / / ? ~ 27K /i i f~ ~ 14rc
\ ! / ~ ~ ? ~
r 13K p'~ ~l``~\~~\H ~KOK
/ ZSK 40K 45K 34x144 ZI/~cJ1K
l, ~ 41K 4JK ~lciYnJSK
~ . .
~ Figure 5. Amplitudes of Vertical Apw, Horizontal Apq and
Apgq Components of Transient Longitudinal P and
Composite PS Waves for a Thick-Layered Model of
the Crust Presented in Figure 3 with Interfaces
of the First Kind as a Function of ~ and iM
Without Regard to (a) and With Regard to (b)
Absorption of P and S Waves by the Real Medium
(With Regard to Absorption o( P= oCs):
1--single waves; 2--in.complete waves. The numbers near the _
curves corr~spond to different types of waves whose rays are
presented in Figure 3.
- [Continued on following page] _
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~ e
10 N 32x
- ~ ~ ~ ~ M29K
y~ ? \ \\\~\\?IR
~ ~ ~ ? ~ / \
~ ~.G--- ? ~ ~ ~
/~iil~ -~~i~ / / ` ~ \~'118K
~ / ~ii~ ~ ~ ~ ~~-9 /`i ~ 1144rc
/ ~i"~�~ ~2N ~ \ \ ~ 4JK
_ 10 ~ %
~i~ .NK / ~ ~ 34K
~ ~ ' ~ ~ ~ 21K ~ ~ \ ~ -
~ ~ \
~ \ \
- / 44K ~~i~_~~\ \\~\~`~145K
4Jn ? ~ ~ ~ ~141K
_ 28K j/~~~~ \ 40K
JSK ~ \ ~ \ ~ T9H
~ \ \
7
10 -
% ~ 4SK ~46K
~
, )i� ~ ~
39K ~
� ~ '
i
~ ~ 3fK
f0e
~ IQ~Z ~ � `
/ \
~ % ' ~ ~3Ax
f
~ 46K , .
-
p \
~ ~ ~ 1 Z 37K
~
A�$q;AP9'APM \`~~f( AP59'~P~Ap" .
= Figure 5. [Continued]
_ Key:
l. Radians
2. Degrees
The following parameters were taken for the second model: H1 = 3 km, vpl =
= 2.8 km/s, vP2n = 5}an/s, vP3n = 6 km/s, 30� and (P = 60�. The sources -
of oscillations were located on both sides of the contact at distances of -
60 (xp = 0) and 15 km (xp = 45 km). Absorption was not considered. The theo-
retical calculations showed that the values of the ratios of composite-reflected
PS wave amplitudes to the amplitudes of transient P waves may reach 0.5-1.5
and may reach 7.5 at extreme points. The amlitudes of transient diffracted
PS waves can be compared to the amplitudes of transient P and PS waves [89,133].
The amplitudes of transient single P and P5 waves for thick-layered media
with transition zones between layers represented by a thick--layered bench.
_ ~
24
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The ratios of amplitudes of transient single and incomplete PS waves to the
amplitudes of transient P waves and the model of a thick-layered media with
transition zones between layers represented by a thick-layered bench are
presented in Figure 6. The relationship between the thicknesses d of thin
layers in the bench and the lengths ~ of P and PS waves is expressed by the
function d~~ A model of the medium approximates the crust (Figure 6,
III) of the North German Depression. The values of distance from the source
are A x= 0-30 km, which corresponds to angles of incidence of P waves to
the Mohorovicic discontinuity of 0-50� and 20-160�. The amplitudes
of all waves were calculateri without regard to the absorbing properties of
the medium. The derived data indicate that the values of Apgq/Apw for PS
waves formed on the benches of thin layers may reach 1-1.25, i.e, the ampli-
- tudes of composite waves may be comparable to and even higher than 'the ampli- !
_ tudes of P waves passing through the thin-layered bench.
Table 3. Amplitudes of Horizontal and Vertical'~~omponents of P Waves _
v 3 xat c~ vP2�8 Het/~ ~P3~7 x~s/~
~l~ PS
ip, rpa7;7rc
ApZ I Ap~ Apz I'`~Pg ApZ I ApR
10 0,96 0,05 0,95 0,12 0,95 0,16
20 0,96 O,i3 0,94 0,25 0,94 0,31
30 0,96 0,19 0,9 0~36 0,89 � 0,44 _
yp 0,96 0,25 0,86 0,47 0,82 0,54
~ Sp 0,95 0,28 0,80 0,57 0,75 0,66
gp 0,94 0,32 0,75 0,62 0,68 0,76 -
- 7p 0,92 0,35 ' 0,70 0,70 0,60 0,83
gp 0,9 0,38 0,66 0,74 0,54 0,87
gp 0,9 0,4 0,66 0,75 0,53 0,90
Key :
1. Degree
2. km/s
The ampli~tudes of the horizontal components of P waves. The amplitude of
the horizontal components of P waves, according to Figure 5, are frequently
comparable to those of the horizon~al components of PS waves. Z'heoret�ical
calculations of the horizontal and vertical components of P waves were made
as a function of the angle of incidence of the wave to the excHange boundary
ip and of the velocity of longitudinal waves near the earth's surface (Table 3)
- to determine the effect of the parameters of the medium on the amplitudes of
the horizontal components of P waves. Analysis of the data showed that the
value of the horizontal components of P waves increases witY~ an increase of-,;
ip and vp. For example, ip = 80-90� at vp = 3 km/s, which corresponds to ~
near earthquakes (Q ~ 8-10� and hoch ^ 0) and the ratio of the horizontal
component at the P wave to its vertical component does not exceed 0.3. The
amplitude of the horizontal component of longitudinal waves becomes comparable
to''.:hat of the vertical component with an increase of vp to 6 km/s~for angles
6.
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. of ip = 70� ~ 14� and hoch ~ 0) and at vp = 7 km/s for ip = 55�
(L1 x 18� and hoch ~ 0~� The amplitudes of the horizontal components of
P waves begin to exceed the amlitudes of the vertical components with a
further increase of angles ip.
. !11 .
, 8 N, 6, �
KM f~CM~ ~ 5 b~ ,kM~C dp,M + G(5 M I _
~ 7,1 19 4D 4,5~10" Z.25�!0
5
_ !1 ~.5 ~ S ~ !,0�f0'y 5.~3'!0's
1,65 6~ I,013'!D'y 5.15�!fl
_ / , i 6 rs 1,95 'a ~ se 2,~�~a"S {ois�?o s
~
3,�s 442 z,orio-S ~,N�10's
~ 4,45 8,1
~ 3,3 1,1�!0"6 5,0�~U"~
~ - 4,6J5 8,~5
- a , S0 3,3 us-yas vP- e,z ~,0�~0_6 s,n�~o-~
~ , A~~ ~ ' ~ , ~ ~Snn b,P1_
APw J,2 5,7
_ , Usn vP Y ~1
3 2,60 S,3 ^
II 3,43 6,1
z
. Z a 6 ~ ~
N
A r Q 8 ~'KM Un68 UP6,4
2,65 ~4 ~
APw ~ ~
J Q d 85 6,7 _
~ ~S VP
2 ~ / 6 B 4,45 7,~ 1~ L
~ S P
~ =-s..t' dx,KM ~ 3,91 6,8
0 5 15 15 g~~ ~
~
- ~2 ~3 q,IJ 72
Figure 6. Shape of Recording (I) and Ratio of Amplitudes
(II) of P and PS Waves for Model of a Thick- ~
Layered Medium (III) With Thin-Layered Benches
(IV): 1--P wave pulse without regard to absorp-
~ tion; 2 and 3--PS wave pulses and curves
Apsq/ApW with and without regard to P and S
wave absorption ( d p= 2o(S), respectively;
a--for basement surface (vpp1= 5.6 km/s);
b--for surface of basaltic layer (vp =
= 6.7 km/s); c--for Mohorovicic dis~ontinuity
(vppl = 8.1 km/s)
26 -
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The Dynamic Characteristics of Single P and PS Waves from Theoretical
Calculations
The dynamic characteristics of P and PS waves include the shape of the record-
ing of recorded waves, their frequency spectra, intensity and polarization.
The Shape of Recording of P and PS Waves
The shape of recording of single P and PS waves formed from P waves at inter-
faces of the first kind in thick-layered media (d/~ 3 1/2) is identical
_ [26-28]. The shape of the recording of P and PS waves [72, 73, 164, 1651
may undergo changes (see Figure 6) in the case when the i.nterfaces are repre-
sented by benches of thin layers and are different for P and PS waves*
These changes are insignificant even when the velocity drops at the boundaries
of the thin layers reach 0.65 [164]. 7che correlation coefficients of the '
normalized cross-correlation function, which we calculated by the amplitudes
of P and PS waves of the same types of phases which passed through the zone
of the interface with different structure, were rather high: 0.73 - 0.95 for
= 20� and 0. 56-0.91 for L1 = 70� (Table 4) .
The Frequency Spectra of P and PS Waves
- The frequency spectra of P and PS waves for models of thick-layered media
with interfaces of first kind are identical [26-281. ~'1'~e frequency spectra
, of P and PS waves, according to theoretical calculations [164] and our data,
also remain identical, but differ in amplitude in the presence ~f zones
represented by transient layers or by a bench of thin layers between the _
- layers of the crust. The amplitude of a maximum frequency spectrum of com-
posite PS waves may be 2.5-3.5 times less than that of the maximum frequency
spectrum of P waves. Displacement~ of the maximum frequency spectra of P
and PS waves during passage through thin-layered transient zones of different
structure at different values of d/T do not excee3 10 percent, i.e., they
are essentially located within the accuracy of determining the periads of
P and PS waves on seismograms. _
Theoretical Amplitudes of P and PS Waves and Their Dependence on the
Parameters of the Medium
The corresponding theoretical calculations were made for three models of
two-layered and a number of multi-layered media with the presence of inter-
faces of the first kind and also benches of layers which approximate ~he
transition zones from one layer of the crust to another~'*to determine the
effect of various parameters of the medium on the amplitudes of P and PS
* _
- We considered P and PS waves only with frequency of 1-2 Hz.
The effect of the structure of the exchange zone on the amplitudes of P _
and PS waves in the case of its representation in the form of a transition
layer or bench of layers is given in more detail in [72, 73, 165].
27
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b ~
_ ~
a
o u ~ ~ ~ ~ ~ ~ ti
y a o 0 0 0 0 0 0
~ ~ .
0
~ II ~ ~ ~ ~ ~ ~ ~
a o 0 0 00 0 0 0 0
~
al =
x I I I I~�,~- � I I I
w
o -
N ti c~r'~. o~ a;, n ti rn
~ d ~ N N N N I I N N ~ N
~ M
+J . v
~g~ b ~ N N N N I I I I I
_
a~ ` ~ .
~ b M N M M ~ ~ N N c+'~
~
N
3
~
~
' ~ ~ ~ o c~ o ~ o ~n ~n o
~4 a ~ m ~r .r ~ ~ e� m .r'
~
-
~
~ ~ ~ ~ o o o
~V p a0 u~ h t~ ~ ~ ~D cD t~
~
~F~1 l0
4-1 r"1 N
N ~ " -
U vl .r ~�o~' en cn ~ ~ ~ I ~
" O O p ~
N
roo P m mi I I I I -
a~
H+~ o N ~ m ~o m ec
N �~-I
O N P ~ ~ ~ ~r ~ ~ m m ~
U ro '
~ ~ -
N ~ ~ o O m O~ . ~
N N a oo ~n co ao" ~ ~ cc co ao
U 0 �
W
4-1
O ul
~
v
GNJ ~ ~ . c
~ 3 rr
~ a i A~ ~
- ~ ;~s JL - f ~ _ ~ _
~ ` ~
~
~ ~ r-i N f~1
~A-1 .
E ~
~
28
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and the ratios ApSq/ApW. The first and second two-layered models with -
interfaces of first kind approximated the sedimentary mantle and the
crystalline crust of the North German Depression. The studied boundary in
the first model corresp~nded to the surface of the Variscian basement and
that in the second model corresponded to the surface of basaltic layer.
The third model approximated the crust and mantle. The studied boundary -
approximated the Mo horovicic discontinuity.
Analysis of the data on the amplitudes of P and P5 waves showed that the
absorbing properties of the media, which alter them by 1-1.5 orders, mainly
affect the amplitudes of the vertical components of P waves. 2"he structure
of the overlying mass (the nimiber of boundaries, the velocity drop on them
and replacement of the gradient medium by a homogeneous medium) changes the
amplitudes of P waves within slight limits. Thus, when the number of over-
lying boundaries chariges from 2 to 9, the velocity drop on them changes from
- 0.4 to 1 and the velocity gradient changes from 0.07 to 0.5 km'1, the ampli-
tudes of P waves vary by a total of 0.04-0.06.
Ars4~AP'~ . �
9
8
7
~10 ~
2
/ ~ .
9
-
l
~
6
/ ~
~ ~
~0 ~ e =
_ - l/~~�
/,1~,
z i .
6_.-._.~ .
z ~
10 Q I 2 dS
~2 03
- Figure 7. Graphs of the Dependence of ApSq/ApW on o( p/ o( g
- for the Model of the Crust Pre3ented in Figure 3:
1--for PS waves exchanged at all interfaces of the crust at
~1 = 72�; 2 and 3--for PS waves changed on the basement and
M oh orovicic disaontinuities, respectively, at different
values of : a--140�; b--72�; c--55�; d--20�. The numbers
near the curves correspond to the types of PS waves in Figure 3.
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The ratio of amplitudes of composite PS waves to the amplitudes of longi- _
tudinal P waves are also mainly affected by the absorbing properties of -
the medium and primarily by the difference of the absorption coefficients
of P and S waves. Thus, the value of Apgq/Apw for the models presented in -
Figure 8 varies by approximately 1-2 orders upon variation of ~(p/aC g
from 0.5 ~0 2 (Figure 7).
The second factor affecting the value of Apgq/Apw is variation of the vel-
ocity drop of P and S waves at the interface of the two media. Variation
of vpl/vP2 from 0.535 to 0.98 leads to a decrease of Apgq/Apw from 0.26 to
0.01 (see Figure 8). Variation of vgl/v82 from 0.45 to 0.8 on the exchange
boundary leads to variation of Apgq/Apw from 0.3 to 0.1 at 20�. _
a v
0,4 o,s qs o,~ qa qs
~ ~S R - . ~ 0,8 R9 ~
. o-�_. ~Pz
.
_ .
+ ~~n\.
\,~~`~~w
~ _
_ ~+1"F+~~ ~ ~ � ti,,
!0~ ~ ~
~ ~
, � ~
~
~ ~ ~
. ~
~
1U~ ~ ~1
~
, . .
_ 6 ~ a ~
IP 1 9 4 S?,KM/c f 2 3 4 S 6u,KN/c 1 2 3 4 ~K
L ~ ~ ~ ~ ~ ~
~5f UPI-=-= USl VPl-_ ~Si UP
S7 7,94 iJ'P~ ~6nM/C U511,94 UPi 56 ~S2'~ ~pt
~6
C~' Q2 ~3 Q~ ~5 ~s ~7 ~8 ,
Figure 8. Graphs of the Dependence of Apgq/Apw on the Velocity
Drop of Longitudinal vpl/vP2 and Transverse vS1~~S2
Waves at the Exchange Boundary (a) and the Pxofiles
- for which the Theoretical Calculations were Made (b):
= 1-- ,C1 = 20�; 2-- 55�; 3-- 0= 72�; 4-- = 140�; 5-7--
curves for models of the sedimentary mantle I, II and III, re-
spectively, without regard to absorption of P and S waves; 8-- _
curve for variant I with regard to absorption of P and S waves =
~P - ~S~ 30
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The third important factor whicih significantly affects the value of
Apsq/ApW is variation of the value of coefficient K at the exchange boundary
which characterizes the ratio of the velocities of longitudinal to transverse
waves in the layers. Variation of this parameter from 1.06 to 1 or from 0.95
to 1 at a constant value of ~ leads to a decrease of the ratio Apgg/Apw by
a factor of 30. Unlike longitudinal waves, the amplitudes of composite waves
and consequently the ratio Apgq/ApW depend somewhat more strongly on the
number of boundaries located above the exchange boundary and on the velocity
drop on thesE boundaries. An increase of the number of overlying boundaries,
velocity drop and velocity gradients on them within the same limits, which
was presented above for P waves, changes the values of Apgq/Apw by a factor
of 4-5. Variation of the density of rock G at the exchange boundary and
replacement of a homogeneous coveri::g medium by a gradient medium weakly or
essentially does not affect the value of Apgq/Apw. Variation of the value
of G by 0.3 g/cm2 leads to variation of the value of Apgq/Apw by 0.005.
Replacement of the gradient medium by a homogeneous medium at vpl/vP2 = 0.6
- and L~ = 72� changes the value of Apgq/Apw from 0.12 to 0.131.
Polarization of PS Waves
There are now two points of view on polarization of PS waves. According to
the first, PS waves are close to linearly polarized with regard to the accur-
acy of determining their delay times on seismograms ( A tpS-P) With respect
to P waves. The phase shifts of PS waves recorded on the X and Y components
do not exceed 0.1-0.2 seconds. An exception are fault zones where they may
reach 0.4 second. According to the second point of view (52, 54], PS waves
are polarized elliptically due to the anisotropy of ttie medium. Their phase
shifts on the X and Y components reach values of 0.7-1.5 seconds.
We made theoretical calculations of the phase shifts of PS waves recorded on
- the X and Y components detexmined bg the effect of anisotropy. or quasi-aniso-
tropy of the medium [120, 131, 167]. Theoretical calculations of the quasi-
anisotropy coefficients* dQ of a layered medium, made by formulas of [131]
for PS waves with h~~ d. showed that ~ will comprise 1.01-1.05 for the
sedimentary ~~antle and 1.005 for the entire crust at angles of inclination
of the interfai:es up to 20� and for earthquakes with 20�. These values
of coefficient ~ lead to a time different of recording PS waves on the X
and Y components of 0.1-0.12 second for the basement surface at depths of
its deposition of 5 km and of 0.1-0.4 second for the horovicic discontin-
uity at depths of deposition of 33 km. Since the angles of inclination of
the Mo horovicic discontinuity ~ do not exceed 10� under platform conditions,
the value of the time delay of recording PS waves on the X and Y components
from this surface will also not exceed 0.1-0.15 second. A similar pattern
_ *
Coefficient aC is denoted in [131] as ae 3 and i.s considered for longitud-
inal waves. The assumption of the proximity of the values of ~g for P
and S waves was used in our investigation.
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is also observed for P and S waves propagated from remote earthquakes in
anisotropic media. The low effect of anisotropy or quasi-anisotropy of
the medium on composite transient waves polarized in the plane of the beam
(PSp) and in the plane perpendicular to the beam (PSH) is determin~d by
their propagation in directions close to vertical. Consequently, the aniso-
tropy and quasi-anisotrapy of the crystalline and sedimentary masses of the =
earth's crust (with the exception of fault zones) may not lead to significant
phase shifts (up to 0.7-1.5 second) between PS waves recorded on the X and
Y components. Taking into account that the error of reading the times
~ tpg_p on seismograms comprises + 0.05-0.1 second, uninterpreted PS waves
from remote earthquakes may be regarded as linearly polarized with a spe-
- cific error.
The Nature of Longitudinal and Transverse Waves from Explosions and
_ Earthquakes and the Area of Their Application
The Nature o= Waves
The nature of P waves recorded from explosions at distances from 0 to 300 km
from the point of the explosion has been rather thorouc,hly studied during
the past 10-15 years [38, 39, 55-57, 68, 69, 104, 106]. It was established
as a result of the investigations that there are two types of waves in wave
~I ~ fields from explosions at distances from 0 to 300 km: those reflected before
I and after critical points and refracted waves related to deep interfaces of
the earth's crust. Refracted waves are mainly traced in the first arrivals,
although the~existence of reflected waves is also possible in the "visible"
first arrivals. Reflected wave~ are mainly traced in the next part of the
recording. Since the observations were usually made during extensive inves-
tigations in seis~ic prospecting only by means of vertical seismographs,
essentially no one was involved with S waves and determination of their
nature. However, S waves apparently have the same nature as longitudinal
waves.
During seismological investigations, observations were made by using three-
component.installations which record intensive S waves occurring at earth-
quake foci [48, 132, 141]. Direct and refracted P and S waves are recorded
in the first arrivals on earthquake recordings as a function of epicentral
distance and reflected and refracted waves are recorded in subsequent re- -
~ cordings. Direct P and S waves in the region of the first arrivals are
observed at those values of for which the condition Q< hoch is fulfilled.
- The Area of Application of P and S waves -
The presence of refracted and reflected rather than leading (1, 38, 39, 106)
P and S waves during KMPV and GSZ led to variation of views on the physics
of formation and propagation of P and S waves in the medium from explosions.
Consideration of the process of formation of refracted waves during IQ2PV and
GSZ [30] and the nature of propagation of refracted and reflected waves in
the block structure of the crust showed that the use of refracted and sub- _
critically reflected waves obtained at great distanoes from their initial
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points is complicated for construction of the relief of the crustal inter-
face and leads to their significant averaqing.[1, 107]. Taking the nature
of P and S waves into account, it was more correct to use them in investi-
gations with the "Zemlya" device to determine the velocity characteristics
of the medium. ~
Determination of velocities by P and S waves is possible only by hodographs
of the first arrivals ot refracted waves or by hodographs of reflected P
and S waves from the interfaces of the earth's crust mainly to the initial
points.
The correctness of constructing hodographs of reflected P and S waves re-
corded during subsequent arrivals is determined by the reliability of cor-
relating these waves along the profile lines. The latter in tuz~n depends
- on the distance between the observation points (seismograms) and the fre- ~
quency spectrum of the recorded oscilla~ions. Confident phase correlation
of any types of waves is possible if the following condition is adhered to
[14, 45]: ~ x=(Tvk)/2 or ~x =(Tvk/4), where Q x is the distance be-
tween seismographs, T is the period af the wave and vk is the seeming veloc-
_ ity of the wave along the hodograph. Ths maximum frequency spectra of P
waves recorded during GSZ ( Q = 0-300 km) are located at frequencies of
5-8 and 12-16 Hz [38, 391. The ma~cimum frequency spectra of the first P
waves from explosions and near earthquakes were determined at frequencies =
of 5-8 Hz during the initial stage of investigations with the "Zemlya" de-
vice and those of S waves were determined at frequencips of 3-5 Hz [124].
The apparent velocities of P and S waves from earthquakes on the hodo~
graphs at 5� varied from 8-10 to 20 km/s. Consequently, the distance -
between the observation points 4 x should be given as 0.5-1 km to find a
reliable base correlation of reflected P and S waves. At the same time,
if the same device is used to record P and PS waves from remote earthquakes, _
; which are optimum for construction of the crustal interfaces, then ~ x for
them can be brought up to 2.5-5 km or more. These dastances are unsuitable
for finding the continuous phase correlation of P and S waves reflected from
the crustal interfaces. At the same time it is unprofitable to decrease the
distances between the observation points to 0.5-1 km during regional inves- _
tigations in order to be able to accomplish phase correlation of reflected
P and S waves. Moreover, a decrease of distances to 0.5-1 km, based on the
experience of GSZ operations [38], does not lead to reliable axes of co- -
phasality of P and S waves from the deep crustal interfaces since their
hodographs consist of individual unextended axes of aophasality (up to 1-3 km)
- even at distances of 100 m between seismographs. Based on these concepts, it
was decided to rely on the first arrivals of P and S waves refracted in the
. crust to study the velocity characteristic of the medium. Determination of
the beginning of oscillations of P and S waves on the recordings from earth-
quakes and explosiuns and tracing them from station to station with distances
of 5]an between them is quite realistic. Thus, the first area of application
of P and S waves during development of a rational complex method of studying
" the structure of the earth's crust was study of its velocity characteristic.
It was assumed in this case that P and S waves be used both from special and -
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accompanying explosions (KMPV, GSZ, MOV, guarry and so on) and from local
- and near earthquak~s. The next tasks, solution of which was possible by
using P and S waves, were seismological: determination of the coordinates
of earthquake foci and study of their dynamic characteristics (energy, _
class, magnitude, intensity and so on).
~
~
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HODOGRAPHS AIVD DISPLACENIENT VECTORS OF P AND PS WAVES
Moscow SEYSMI~HESKIYE ISSLEDOVANIYA S APPARATUROY "ZEMLYA" in Russian,
1977 signed to press 31 Jan 1977 pp 34-53
_ [Chapter 2 from the book "Seysmicheskiye issledovaniya s apparaturoy
'Zemlya by I. V. Pomerantseva and A. N. Mozzhenko, Izdatel'stvo Nedra,
1,400 copies, 256 pages] _
[Text] Equations of Hodographs and Recording Times of Single, Multiple
and Lateral,,P and PS Waves
~ Equations of surface hodographs of all these waves and equations of their
delay times with respect to transient P waves for two- and multilayered
three-dimensional models of inedia were derived to study the kinematic char-
, acteristics of single, multiple and lateral P and PS waves from remote -
- earthquakes.
Difference Equations of Recording Times on the Surfaces of Variot~s Ho.ri-
zontally Layered Media of TranGient Sincle P and PS Waves
-
Difference equations of the recording times of single P and PS waves
( 0 tpg_p) were derived for two�, three- and multilayered homogeneously _
stratified media and also for a gradient medium covering the exchange _
boundary. Since clear P and PS waves can be separated both on recordings
from near ( L1 = 1-10�) and from remote = 10-160�) earthquakes, it
makes sense to present formulas of A~pg_p for < 10� and A> 10�.
The difference in these formulas includes the following. Since the front r
of transient P waves may be assumed flat and the angles of incidence of
these waves to the exchange boundaries may b~ assumed small at A~ 10� on
spacing of recording stations of 100-200 km, they can be simplified when
deriving equations of ,L~tpg_p. As a result, the Hasegawa formula [176]
will be found for a~wo-layered model of the medium. Making use of a simi-
lar procedure for multilayered media as well, the formulas for ,Q tpg_p can
be reduced to a more convenient simplified variant. The formulas derived
below,prior to expansion of them into a series by sines, can be used for
~ ~ 10� [1081. .
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_ . ~
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A two-layer`ed medium. Let us denote the velocities of longitudinal waves
in the first (covering) and second (underlying) media by vpl and vp2. The
delay times tpS_p c~f the PS wave with respect to the P wave enter their
approach to 0 a'ccording to Figure 9, a after a number of mathematical
tranaformations [lU8] can be written in the form
n
2 sin i 21 1~
~tps-p= ~1 ~K~-1)(1+ ' a- ~2.1)
uPl
~
where H1, vpl arid K1 are the depth, velocity and mean coefficient of the
velocity ratio of P waves, respectively, to the v~locities of S waves in
the first medium covering the exchange boundary and ipl is the apparent
angle of emergence of the P wave to the surface of a two-layered medium.
Taking into account that ep1= Kl sin ~21 L141] , one can find
Otpg_p= P! `Kl-1~ ~1-~- ZKl COSZEpiI, ~2.2~ -
\
where epl is the angle of emergence of seismic radiation. -
b
F i ~v~
~
tP~ ~
M
;x. p ~P1 ,Z
H~ Un
~PI I ~ tP
, i~, ~ E~,
Q a N' e~ ~ y
ii is, ~ -
- ~ ~ ~ Q ~ H vPi
P1 Z
~P2 1 � vP2 ~s2
(PZ` tP2 ~ 2 t
P � y l~3 ~PS LPJ
. � P P _
P
Figure 9. Diagram of Path of Single P and PS Waves in
Two- (a) and Three-Layered (b) Media With
- Horizontal Interfaces -
Formula (2.1) was derived by Hasegawa [176] in 1930, but in a somewhat dif- -
ferent manner than was done in [108]. This formula was subsequently distorted:
the apparent angle of emergence of waves to the earth's surface ipl was taken -
- 36
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~
\ -
by investig~~tors who used this formula as the angle of incidence of the
P wave to th~ exchange boundary. This error was noted and corrected [108].
The three-lay \~d medium. The velocity distribution in the medium is as
follows (Figure~a, b): vP3 ~ vP2 ~ vpl and vg3 ~ v82 ~ ~S1� The
delay time of thi~ PS wave with respect to the P wave at point F can be
written in the foi~n
\
_ / t 1
~tP~~p= ~p (KZ-1) (1-~- 2' sin2 29 1-}-
~
A' (K,-1) 1~ R1 sin~ `P1 ) (2.3)
upl ( � 2 2
`
1
or
~tPS-p ps ~Kz-1) (1-}- 2Ks cos$ epa) -I-
(2.4)
-f- pi (Kl 1) ~ 1-F- 2K1 cos' epl _
where the parameters contained in the first term characterize the first
layer and those contained in the second term characterize the second layer
(see Figure 9, b); iP2 is the apparent angle of incidence of the P wave to
the bottom of layer I(Figure 9, b). -
The multilayered medium. By analogy with formula (2.3), the formula for
determination of ~ tpg_p ior a multilayered medium (n~.layers above a half-
space) will have the form
_ Otpglp=~ gm ~K 4)r1+~ vp~ 'X ~2.5~
m_a UP m ~ vP (m+1) ,
1 a
X ZK~ S1II ~y r
where im is the angle of incidence of~:~the P waves to the exchange boundary or
Otpgl~'p_~ Ae` (Km- 1~ (1-}- 2Km COSZ em) .
yi11~ m~l ~P m ( 2. 6)
Gradient media. If there is a gradient of velacity variation with depth, ,
formula L~tps_p can be derived from formulas (2.5) and (2.6)' by an unlimited
increase of the number of layers with simultaneous approach of their thick-
- ness to zero. As a result of derivation, the formula for a gradient medium
will have the form
37
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n H~ ` Up-m ~ X
OtPS-P- s upm ~~m_1/[1+CvP(m+i) -
m-1 (2.7)
X ZKm siu9 t~] dH~
where vm and Km are the variable values ~vhich vary with depth by some law.
The Equation of Hodographs of P and PS Waves and Time Differences of Their _
Recording on the Surface of a Two-Layered Three-Dimensional Medium with
Inclined Exchange Boundary
The equations of surface hodographs of P waves at Q~ 10�, according to -
[45, 112], can be written in the form (Figure 10)
t, _ ain tpa r V ~xp COS (Q~Z'F ~yp~2 - xP sin ~ -Spl ~ ~ (2 . 8 )
' p �Pa ~ tg iPi
where ipl and iP2 are the angles between the paths of the P waves and to the
normal to the exchange boundary in the first and second media, Mp and y' are
" the coordinates of the point of emergence of the rays of P waves to sur~ace
Q in the x'.y'z' system and Hpl is the depth along the normal at the point
of separation of the P wave from the exchange boundary.
y
, � N '
A~
f~ F
z
,z e ~ ~B a,F iP~ y Sp-'-
SID� i% ~ / C~ ~ ` ~p~ /
\ ~ ~ M / ~ ~ ~ P 1 ~t? / ~
q p~ y ~T~S~~ .
d~+~ -
. - � ' y ~ i,P, L ~
~e
vn ~ / - -+P
~ i /
i ~
P p ~
_ . , / .
R ' .
Figure 10. Diagram o~f Ray of P Waves in a Two-Layered Medium
With Inclined Interface: ' -
- R--inclined interface; Q--horizontal surface of E~arth
38
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The value of Hpl is determined by the formula
gP1- cos~K ' (2.9)
Here Z is the''3epth along the vertical drawn through the point of separation
of the P wave from the exchange boundary and ~ K is the apparent angle of
inclination of the exchange boundary
Cos ~ = cosa ~ sin2 ~ cosz ~ ,
sin ~K ~ sin ~ sin
where ~ is the approach azimuth of the P wave counted from the line of -
strike of the boundary for the coordinaty system x'Oy'.
Equation (2.8) can be written in the form
eini x' sin~-Bp~
tP = UPl l ~ ~xp COS (P~2'f ~yP~2 - p tR iPl , . ( 2 .10 ~
The equation of the surface hodograph of the PS wave, by analogy with (2.8)
can be written as
siII i x' Sin H
tps = v Pa r l/(xg cos cp)Z.-I- (~"s)=- S 8 is~ gl,' (2. ~1)
Ps L
where isl is the angle between the path of the S wave and to the normal to
the exchange boundary in the first medium, xs and ys are the coordinates of
the point of emergence of the rays of the P waves to surface Q in the system
x'y'z' and HgZ is the depth along the normal at the point of separation of
the S~vave from the exchange boundarY. ~
The difference equations of the arrival times of PS and P waves to the sur-
face of a two-layered medium with inclined exchange boundary at 10� have
the form:
H ,
~ AEpg_p= vpl (Kl-1) (1-}- 2K1 cos~epl, -
P1
- (2.12)
- Upl (KI -1) C1-~- 2K cosz ePi)%p ain
~
where ePl is the angle of emergence of the seismic radiation of P waves to
the boundary inclined at angle :P to the earth's surface and Xp is the co-
ordinate of the point of emergence of the P wave to ~the Q surface along the
Ox' axis.
~ ~ ~ 39 '
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~
- T'he relationship of angle epl to the ordinary angle epl is expressed by
the formula
ep~ = epl t _
where the plus corresponds to a di~ of the boundary and the minus corresponds
to a rise. Coordinate Xp is determined by the formula
Xp = [l S1II 2pp ~ ( 2 . 3 ?
where a is the major axis of the ellipse MF'NF, x~p is the extent of dis-
placement of the center of the ellipse MF'NF with respect to the center 0
of the coordinate system x'Oy' and is the approach azimuth of the P
wave counted from the mi.nor axis of the ellipse (see Figure 10) parallel
to the strike of the boundary. ;
The relationship between the values of p' and ~ is expressed by the function '
. , 3iri - -asop-I-tB ~ ~-xop-~-ap (1-I-t6~ � .
ap (1-?-tga ~2.14)
At 0, the second term of equation (2.12) approaches zero, the clepth (H)
along the perpendicular to the interface coincides with the depth along the
vertical and the entire formula (2.12) is transformed to a Hasegawa formula
for a two-layered medium with horizontal interface [108, 176]:
~ZP3-P= pi ~Rl-1~ 11-f- 21ft COS~BplJ.
~ (2.15)
The value of t~,g_p from formula (2.12) can be written as _
Otps_p= H~ ~K~-1) ~1-I- ZKl coszepl)~ (2.16)
P1
where H' is the depth along the normal eliminated from the point of recep- .
tion to the exchange boundary (Figure 11).
If angle ip2 (denoted by ip2 in Figure 10) is located between the ray and
the vertical to the point of incidence of the ray to the sloping interface,
then for the same value of but for different values of we will
- have different values of the angles formed by the rays of the P waves and by
the normal to the interface, equal to iP2 + c~ along the rise and dip of the
boundary, respectively. Formula'~.(2.12) for tps_p remains the same; the
values of ipl,, xpp, ap, bp, sin and Xp become variable for different
40
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~
�N ~4
x p
b ~,v` ~ri
.
Q
4 ~
~ I
p�
~ rM
~7
'
q
~ 4
Figure 11. Diagram of Rays of Single P and PS Waves in a -
Two-Layered Medium with Sloping Interface
- values of ~ , but for the same angle cP K. In this case an ellipse with
its own pafameters ap, bp and xo must be calculated for each value of ~S '
and ~ K. The value of Xp will be determined each time in this case for
each value of cQ K as the coordinate of the major axis of the ellipse. At -
_ 90�, Xp ap + xpp. Angle ipl is determined in this case for each
value of Cp K as
sin iP1= Upl SiII ~iPa ~N)�
vpa ,
Moreover, the plus inside the parentheses corresponds to the rise of the
- boundary and the minus corresponds to a dip.
Equations of the Lines of Intersections of the Aggregate of Rays of P and
PS Waves with the Daytime Surface of a Two-Layered Medium
For P waves
(xp)a [cos2 ~ - sin~ ~ tgz ip1)~-(yp)2 2xp 9iII ~HP ~a tP i =
- (2.17)
� ~HP t$ lP1~Z.
In the case of a horizontal interface (C~ = 0), equation (2.15) assumes
the form
~~P~z + ~~?P~a = (HP tS iPi~2~ (2 .18 )
41
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I _
I
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. ~
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i.e., the line of intersection of the rays of the P waves with the surface
of a two-layered medium will be a circle with radius Htgipl. The line of
intersection of the rays of P waves for a sloping interface [equation (2.17)]
with second-order invariants of curves [17] Q' and ~ equal to L1 # 0,
S~ 0 and ipl ~(90� - cp ) is an ellipse, while that at Q'~ 0, c~ < 0 =
and ipl )(90�.- cp ) is a hyperbola. The rays of the P waves will be
_ described by ellipses for earthquakes with epicentral distances of L~ > 20�
and at ~p = 40-80�. 7.'he axes of the ellipses and the displacements of their _
centers with respect to the axes of coordinate system x'Oy' are expressed
by the formulas
Hpi tg tpi cos W
ap- �cos2cp-sin'-~tgz'tpl `
~Rp~ tg ir~ cos ~ (2 .19 )
bP = + ~
- Ycosz ~-sin2 ~ tga ipl _
sin ~Hpl tga iPl -
x0P Cos~ ~p-sin2~ tg~ tpi ~
For the PS wave, the equation of the line of intersection of their paths with
the daytime surface of a two-layered medium with sloping interface has the
_ ~
~ foscm
(xe)2 ~cos2 ~ sin2 ~ tgz i~l~ -I- ~Us)y -I'
2xe sin q~Hsi tgz iS1= (Hsi t8 isi)'� (2 . 20 )
In the case of a horizontal interface = 0), equation (2.20) assumes
the form
(xs)z-1- ~~ls)z = ~As~ tB iai)~~ (2 . 21)
i.e., the equation of the projection of the ray of the PS wave to the
- earth's surface is a circle of radius HS1tgiS1� '
Equation (2.20) for PS waves is an ellipse provided that 0; 0;
90� - ~ ~ iSl ~17~ �
_ Equation (2.20) is a hyperbola provided that 0; 0; (90� i51� -
_ The axes of the ellipses and the displacements along the x' axis for PS
waves are determined by the formulas ~
Hsi tg tsi cos ~ -
as cos~ cp-ainz ~ tgz tal '
42
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' 1~R1 tg i91 coe~ _
bg = � � '
cos~ ~p-sinz ~ tg iel (Z. 22)
~ ein~Hgl tgs te1
~os = -cosY q~-~ln' ~ tg t8i ~
Equations Q tpg_p at .0 < 10 � for a two-layered medium with sloping inter-
face can be written in the form
etP9_p_ g' _ g,
C08 tSiv91 CO9 iP1vP1 + ( 2. 23 )
~ g~ ~tg iP1'-tSigl~ 91II lPl~
vP9
or
- e:pg _ p= g" (xl ~os ~gl - ~og ~p~).
vpi (2.24)
Equa~ions of Hodographs and the Time Difference of the Arrival of Multiple
P and PS Waves and Single P Waves to the Surface of a 7.tao-Layered Three- _
Di.mensional Medium with Horizontal and Sloping Interface
If multiple waves of types P2Pir ~P2PlPlp1~ P2plPlPlPlP1 ~d so on), P2S~
and P2P~S~ (Figure 12, a) occur at some special geological conditions, t e
equations of their surface hodographs with horizontal exchange~boundary in
a two-layered medium can be written in the form
(~-i, ~1 Pl'~' P
tP~Pl pPi COSL t r (2.25)
tP.Sm =(m U 1~ Hl cos isi -I- tps, ' (2 . 26 )
1 . 91
nEl (m.-1) Ht
' ~ a m= cos iPl COS tgl "I'tP9~ ~2. 27 )
p~pi81 UP1 U81
where n is the number of segments of rays of the way included between the
surface of a two-layered medium and the multiplicity boundary (n = 1, 3, 5,
7 and so on) and m is the number of multiple reflections without the first _
single wave. There is the following relationship between the values of m
andn: n=landm=0, n=3atm=1, n=5atm=2, n=7atm= 3and
_ so on. At n= 1 and m= 1, equations (2.25)-(2.27) change to equations of
43 _
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� ~ - -
~ ~ FOR OFFICIAL USE ONLY
the surface hodographs of single transient P and PS waves. The equations -
of the surface hodographs of single transient P and PS waves for a two-
layerec~ mediuin with horizontal exchange boundary have the form
tp ~ B1vPS' ~ ~x~)~ tg tpi, ~ (2 . 28 )
1 tPS = 9 P2 2(~~y~)Z -I- (z")Z tg tsl ( 2. 29 )
With a sloping,interface, the equations of the surface hodograFhs of P2Pi,
P2Si and P2PiSi waves ~Figure 12, b) for a two-layered medium have the torm
t~ R= T~ t~ n+ _
p~pl p'pl (2.30)
tp,Sl Te-~-tP.si' (2.31)
tP~PrsSm - P~Prt'I' tP:Sm~ ( 2. 32 )
1 1 1 1
where T1 arid T2 are the transit times of multiple P and PS waves from point
A to point N and tp pn and t"P Sm are the equations of the surface hodographs
2 1 2 1
_ of single longitudinal or composite PS waves whose wave fronts comprise
angles ipl -(n - 1)q~ and igl -(m - 1) cP , respectidely, with boundary R.
- Ttie time difference of recording multiple P2Pi, P2Si and P2PiSi waves and
single P waves can be written in the following form. -
A Yiorizontal interface ~
_ ~n_1, At
tP~Pi -~p - ~Pl cos iri . ( 2. 3 3)
- t~'_tP= ~m-1)~i cosisl-~ (Ki-1) C1~- i cosaePl~, (2.34)
P~gi v31 ~Pl ZKl
tp,pngm - tp vPi COS LPl v91 A1 COS L91 _
1 1
N' (Ki-4)~~1~- 21c cos~epl). (2.35) -
P1 1
A~sloping interface
. ~ hl
tP'pn - tp = vPl COS LP3 -I"' Tle (2 . 36 ~ _
1
tPsSi tp sl cos isl Tz� (2. 37) _
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s ~
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n
Q .
~ PzP~ oopP PP~PPPP ~
_ -x
~ I ~I
/ tP~ ~ I I % -
/ / H~ L~' I ~ I
~
, ~
9 dPz
PZ
!
Li PZPPP ~PFPPF ~
- 0 P P y
i tiP~ ~ Z~ Pt 4~ LP~"~"~ ~ '
i
I` ~ j h I v~
R i A N U~
~ ~ ~ ~ -
f~
t
~
Figure 12. Diagram of Pat:~of Multipie P Wave Rays in a
- Two-Layered Medium with Horizontal (a) and _
Sloping (b) Interface ~
The equations of the lines of intersection of a series of rays of multiple -
- P and PS waves with tne surface of a two-lay~red medium will, as for single
P and PS waves, be ellipses or hyperbolas as a function of the ratio of~the
invariants of these lines and angles of inclination of the multiplicity
boundaries. At L~ ~ 0, S~ < a~ which is possible at ncf ) ipl, we find a
hyperbola. At S~ 0, which is possible at n~~ ipl, we find an ellipse.
The axes of the ellipses xpp can be calculated by the method, as for single ~
transient P and PS waves, outlined in detail in [112]. _
Equations of the Arrival Times of Single P and PS Waves in Multilayered
Three-Dimensional Media with Sloping Parallel Interfaces
A three-layered three-dimensional medium. The time difference of recording
PS and P waves at point F(Figure 13) is determined by the formula
~tpg_p= gpa.~Ka-1) C1-{- 2Ka COSZgpal ~
pa ~
+ gpi ~Ki -1) C1-{- 2K1 cosz epl -
P1
. "pl ~Sl-1) (1-{- 2K1 cos~ epl) Xpsin (2.38)
45
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a - ~ ~ ~
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where Hpl and HP2 are the depths along the perpendiculars to the inter-
faces, epl~and eP2 are the angles of emergence of. seismic radiation (see
Figure 13) in the first and second media and Xp is the coordinate x' along
- the major axis of the ellipse.
Multilayered three-dimensional media. By analogy with (2.38), the equation
of the delay times of PS waves with respect to P waves for an n-layered
- medium with sloping and parallel interfaces has the form
n~.i
- ,tpg_p=~ Pt (Kt-1) C1-}- 2Kt cosaept)-I-
t-z
. gl (Ifl-1) C1-{- 1 cos2 epl) (2 . 39 )
vpl 2K1
1(Kl - 4) C1-}- 1 cos2 eP1) Xp sin
vPl 2K1
where
XP = A SiII xop. (2 . 40 )
Unlike (2.19), here the parameters A and xpp a~e determined by the formulas
~ n=i
. G+ ~gi tg tPt cos
A _ c-a
n-i ~
. ~ (cos~ ~--ain2 W tg iPt ~ . .
ti-a
R-1 . ' ~ (2.41)
~ (Bl sin ~ tg2 iPt )
' , i"a , ~ .
~~p ~ n~l
~ (cosa ~-sinz ~ tg'tP1 ~
t-z
Equations of Hodographs of Lateral P and PS Waves
Transient diffracted P waves. Let us consider the case when the interface ~
of two media is horizontal and diffraction of P waves is from the edge of
the bench (Figure 14). The equations of the surface hodographs of transient
diffracted (longitudinal P and composite PS) waves from edge AA' on ~he
surface of a two-layered medium can be written in the form
_ �pi { x2 Hi -f- I! P2K } ~ ( 2 . 42 )
P~~,- vsi { xa~-~i-~-y vPZx}~ ~ . (2.43)
46
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~ �
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- b
0 X
� 0 Xa f eai i'
_ -~Z'
_ IHp~ ~s~ Zp ~r~ ~'ri ~
I 4 vn t -
I H en ' ~st ~ r. n-3
. ~
y i v n-2
U Prt"
n-1
1 v] Hp ~Sn-1 v ~
. ~vn ~
P ~ ~~3 p .
P
P ~ P . ~
Figure 13. Diagram of Ray path of P and PS Waves in Three-
Layered (a) and Multilayered (b) Media with
Sloping Interfaces
The value of vP2K along the edge is determined by the formula
"ps (2.44)
vp2x Coe t~ ~
where vP2 is the velocity of longitudinal waves in the sec~nd layer and
~ cos ~ is the direction cosine for the incident ray of the P wave (see -
Figure 14) _
- ~ , cos ~ = sin iPa sin ~l. ~
(2.45)
-
-z =n 0
H~ lv~ Y
A I M
i
~'~rt i ~
I ,
tQ I -
I _
2' P
r
9
(1)y,F�'~A
,~o
Figure 14. Diagram of Ray Path of Transient Diffracted
P Waves
Key : -
1. Contact
, 46 a
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LPS,C
a _ b '10
h~' ~d`~ ~ 9A
t 70 ~ 5
.
- L 0 P p
0
~ Hi ~P~ H_h~~Pi~ ~KM' 10 5
~ ~P2 4~2Q S
~P1 ~ tPS-P~C
, Figure 15. Diagram of Rays of Transient P Waves Reflected
From a Sloping Contact (a), Hodographs of P and
- 5 Waves and the Time Profile tps_p at 10� (b)
Transient reflected P and PS waves from sloping contacts. Let us consider
- a two-layered m~dium with horizontal interface. The contact of the medium
- with different velocities is�included between two horizontal boundaries
(Figure 15, a) and is a plane sloping towzrd the horizon at angle ~p . The _
equations of the hedographs of transient reflected P and PS waves were de- -
' rived in a plane perpendicular to the strike of the contact. According to
= Figure 15, a, the equations of the recording times of the P and P5 waves -
reflected from the sloping contact have the form
t~,'P _ 1 h~ fll-h' -
P~Ps vpi {sin(:pl-~~+ sin~ipi~-~~~' (2.46) -
toTP = 1 fj-"~'1
P~Pi vSl { sin (isi-~~ sin (igl-~-~~}' (2.47) -
where vpl and vgl are the velocities of the P and S waves in the first layer, F
- h' is the depth along the vertical to the point of reflection in the first
layer, H1 is the depth to the interface in the twa-layered medittm, ipl and
igl are the angles of incidence of the reflected to the waves to the sloping -
contact for P and PS waves, respectively and Cp is the angle of inclination
of the contact.
The Effect of fihe Angle of Inclination of the Crustal Boundaries on the
Diffez�ence of the Delay Times of Single, Multiple and Lateral PS Waves
with Respect to Single P Waves
Single waves. Let us consider the case when the aggregates of the rays of
P and PS waves describe ellipses on the surface of a two-layered three-
- dimensional medium. The differences of the values of ~J tPS_P were calcu-
lated by formulas (2.2) and (2.12) for two models of the medium to analyze
47
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the time difference of recording the P and PS waves on the surface of a
two-layered medium with horizontal and sloping interfaces. Model I:
- Z= 5 km, vpl = 3.6 km/s, K1 = 2.1 and vP2 = 5.35 km/s. Model II;
Z= 33 km, vpl = 5.8 km/s, K1 = 1.8 and vP2 = 8.1 km/s. The value of
_ angle ~ varied from 0 to SO� every 10�. Angles iP2 (with the vertical to
the interface) comprised 40�55', 30636', 17�15' and 8�38' and corresponded
to equal to 10, 20, 70 and 140�; angles ~S' varied from 0 to 360� every
30�.
The dependence of the value of S Qtpg_p , which is the difference of ~tpS_p
for horizontal and sloping interfaces, on Q and is presented in
~ ~ Figure 16. The theoretical dependence of the relative error (S ~ tpS-P) on
~ along the dip and rise of the interface in percent is given in Figure 17.
~
~
_ ~'dt~-p'~ ~1) e
- 1,1 /
1,0
+ x
0,9
0,8 ~
0, 7 ~
0,6 X x
0,5 ix~ \ \
/
0,4 ~ x\
03 ~ ~
, -
p~
~
30 60 90 120 I50 =-==`=ii -
~ ~ ~ 180 Z10 240 270 ~00 ,~30~i,rpa,qyc -
-0,1 ~ ~i ~
~
-o,~
_43 ~ ~ 1 ~g 3
\S~~ ~Q
-0.4 ~$~2'x-x6 4
~
-QS r
a
-q6 (2) ~
-0,7 a�
Figure 16. Theoretical Graphs of the Dependence of s Q tpg-p _
on Azimuth for Two Models of Media:
1-3--model I for eQ = 10, 30 and 50�, respectively; Model II
- f~r 10�; a-- Q= 70�; b-- Q= 20�; c-- 10�
Key:
~ 1. Dip 3. Degree
2. Rise =
. 48
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Analysis of~the graphs of Figure 16 made it possible to reach the follow-
_ ing conclusions. At equal to 0, 180 and 360�, which corresponds to
the condition of the strike of the boundary K= 0), there is no differ- =
ence in L~tpg-p for sloping and horizontal bour.3aries at Hpl dependent on
C~ K. The maximum differences between ~ tpg_p for sloping and horizontal
intexfaces are observed at equal to 90 and 270�, which corresponds 4a -
the rise and dip o� the boundary (CP K� ~ max~� Thus, at Q= 10� and
cp = 70�, they reach +0.75 second along the dip with a total value of _
~t~s_p of 1.61 and +8.5 seconds for a horizontal interface and 5.25 seconds .
at ~ tpg_p for a horizontal interface. The values of ~ QtpS_p are approx-
imately of the same order along the rise as along the dip, but are negative.
This corresponds to the fact that the values of Q tpg-p for a horizontal
boundary is greater than those of ~,tpg_p for a sloping boundary. Z'he
- ratio between Q tpg-p for horizontal and sloping boundaries changes to the
opposite along the dip: Q tpg_p for a slopinq boundary is greater than for
a horizontal boundary.
Accordi.ng to the graph of Figure 17, the difference in ~ tpg-p for sloping
- and horizontal interfaces at CP = 10-80� may reach 20-100 percent or more
~ of Q tpg_p for a horizontal interface. This circumstance requires that
the angles of inclination of the interfaces be considered when constructing
, the profile at c~ ~ 10� for Q' ~ 70� and at ~p ) 20-40� for L1, ~ 70��
Multiple P and PS waves. In the case of a horizontal interface of two-
layered media, multiple P2Pi and P2Si waves are distinguished from each
other by values equal to tp pn - tp, determined by the type of wave and the
- parameters of the medium. 2 1 The dependence of the difference of arrival
times of~multiple waves Q t on the angle of incidence of P waves to the inter-
face ipl for four variants of models of the media is presented in Figure 18.
The parameters of the models were as follows. Model I: vpl = 3 km/s,. H1 =
= 3.5 km, K1 = 2.2 and vP2 = 4.5 ]an/s. Model II: vpl = 3.6 km/s, H1 = 5]cm,
K1 = 2.1 and vP2 = 5.35 km/s. Model III: Vpl = 4.73 km/s, H1 = 14 km,
- K1 = 1.96 and vP2 = 6.4 km/s. Model IV: Vpl = 5.8 km/s, H1 = 33 km, K1 =
= 1.86 and vp2 = 8.1 km/s.
:~s can be seen from Figure 18, the interval ,Qt betweer. the multiple waves
is reduced with an increase of the angle of incidence iP1 to the interface.
The distribution ~t of multiple waves is subordinated to the same principles
as single P and PS waves in the presence of a sloping interface.
Lateral P and PS waves. Transient diffracted P and PS waves on the surface _
- of a two-layered medium have the shape of hodographs varying from a hyperbola
(y' = 0) to a straight line (x' = 0) (Figure 19) as a function of the approach
azimuth of the front or rays of the P and PS wave to the dislocation line (see
Figure 14). The time profiles [ L~ tpg_p = f(R)] are either almost horizontal
straight lines (x' = 0) or second-order curves intersecting the universal co- -
- phasal axes at large angles of inclination, corresponding to crustal inter-
faces from the basement surtace to the interfaces in the mantle on compara-
tively small (up to 30 km) tracking intervals of the PS wave.
49 -
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d'et a-~o'
12D PS-P -
110
100 _
90 _
80
ZO
7Q
60
~ 10
40 ~ '
- 30
70
~ 70
- 10 140
~ l d=14Q`
_ 0 ~ . _ 3
~
~ \ ~ ` ~ 40 50 60 ;70 }o, rpa,qy~
-lp �b o~ _~~--~---�d~1~i0
_ ZO G=10 ~ ~ ~ ~ p?0_ ~ ~40
~ ~o` �~p 70 -
-~0 _
~g' 6 2 .
- Figure 17. Theoretical Graphs of the Dependence cS.L1 tpg_p
on the Angle of Inclination of the Boundary E
Upon Approach of the P Wave to the Interface -
Along its Dip and Rise for Two Models of Media:
- 1--curves for model I; 2--curves for model II; a--along the
dip of the boundary; b--along the rise of the boundary
- Transient reflected P and PS waves have the shape of hodographs which are _
straight lines with different angular coefficients dependent on the param-
eters of the studied medium and the angle of inclination of the reflecting
contact. The hodographs of transient reflected P and PS waves and the time
profile [ d tps_p = f(x)] are presented in Figure 15, b. As can be seen -
from the time profile, the transient-reflected PS waves at a short distance
f,up to 5 km) from the cont.act may intersect all the time profiles (from 1 to
~ 5.5 seconds) related to tYie interfaces of the entire earth's crust.
Displacement Vector Components of Single Transient P and PS Waves and
Their Azimuths in a Two-Layered Three-Dimensional Medium with Sloping
Interface _
Calculating Formulas
- The displacement vector components of P(UP) and PS(UPS) waves for the right-
handed coordinate system xyz located on the surface of a two-layered
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- dt,C ~
~
- 1~ __.~---o. --o_ 9_ 9 3 n=5
-o~ -
Y'Y-YXYYY 9
~ ~~~._Y~ ~7 -YYyYyyy3
_ 7
__OS
'~~~_s_~~ - - S
5 �~9 5 ~ -
o---o- - -o---o- 5 ' -
_ ~ -0-3
----------3
. 3 3
- ;p i i i i -
10 20 30 ~ 40 50 iP~,rpa�yc
~6? YYY 63 ~ 6~
Figure 18. Graphs of Dependence of ~ t on ipl for
Di�ference Models of Media:
1-4--graphs for models I-IV, respectively; a--for mul- -
n
tiple P waves; b--for multiple PS waves
three-dimensional medium with sloping interface (Figure 20) can; be calculated ~
by formulas similar to those presented in [90).
~ For P waves
UP,L = UP9P COS ~~i -
UPy - -UPQP 31II 1~1 w~+
UpZ = -UpW p. (2 . 48 ) -
For PS waves
rlrsx = Urs [cos r~qs cos 1-E- w) - 2 sin r~ sin (~1-}- w)1+
UPSy = UP9 ~2 s1II T+ COS ~'I~1 til~ -f - QS C08 91II ~'1~1-}- W~] ~ ( 2. 49 )
UP9Z = UPS COS 1~ Wg,
' S1
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P5 E C PS
~
~ ZD '
. ' 18 y'-o
~s ~
- P ~ P
1Z
- 10 0 .
~p2~
- x
0
6 /X/"~x 1o i G
- ~x-X- 70 '
~40
SD 40 30 20 10 0 10 ZO JO 40 50 R, KM~
+-+-+-+T+- a-i4o -
Z x'=0
4
6
~Z 8
~ 3 10 ~ ~
~4 ~
~ ~ ~p ~ x~'7I !0
~ ~ u ~u . G1 ~ ~40 ~
dt~_p,C
Figure 19. Theoretical Hodographs of Transient Diffracted
Longitudinal P and Composite PS Waves for the
Model of Figure 14: -
1 and 2--hodographs of transient diffracted P and PS waves
for the plane x'Oz'; 3 and 4--hodographs of transient dif- _
fracted P and PS waves for the plane y'Oz'; 5--time profile
Q tpg-p af transient diffracted PS wave for the plane x'Oz';
, 6--time profile of 0 tpg_p of transient diffracted PS wave
~ for the plane y'Oz'
where UpX, UpY, UpZ, UpgX, UpsY, UpgZ are the displacement vector components -
_ of P and S waves on the axis of a rectangular coordinate system, qP, qs, WP
, and Wg are the horizontal and vertical components of the conversion coeffi-
cients determined by the formulas of [28], c~J.i and yl 1 are the ray azimuths ~
of refracted P and PS waves, t~ is the angle between the direction of dip-
~ � rise of the interface and the axes in coordinates xOy and ~ is the angle be-
tween the vertical and normal planes passinq through the ray of the PS wave.
52
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~
~ -~J
` ' J~ ~oy ~ vs
~oo ~r I _ ~p
~1 ~ + ' ' ~ z
~ p Usps~' 11=vs I
' ~ \ ~
~ ~si ~ �
~ I Uvi
i'vi I
\ \ \ I e~c~0y`P~2 ~
~
~ P
PS I \
~ \ ~ /
i
s
~ ~ / l~ ~
p
. - ' ~ ~
R ~ ~'P
~
-Figure 20. Diagram of Ray Path of P and PS Waves and -
Distribution of their Displacement Vector
Components in a Three-Dimensional Medium
with Sloping Interface R
Key :
1. 'Dip 2. Rise
- The vaTues of j~2 and w 1 are determined by the formula [90]
K'sin tPZ sin ~z (2. 50)
31II'1~1= sin i' ~
`where ~J �1 = ~ pl or ~ 1� ~ S1? K'', = vpl/vP2 or K' = vSl/~P2 ~ i' = iPl
or i'. =.iS1 as a function of for which wave the calculations are made--P or
- PS, 'is the a'ziiriuth o~ the ray of the P wave impinging.on the interface
_ and`
pl arid_i:sl are the angles between the rays of the P and FS waves in
the first "iriedium and the vertical to the interface.
`Arigle i' is calculated by the formula -
cos i" = C sin ~-I- a~g ~ B- Ce' ( 2. 51)
~where
53
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_ C= K" (cos i' sin si n i' cos cos
B =1- (K' )2 sin~ i' sin'
The Effect of the Angle of Inclination of the Interface on the Horizontal
- Components of the Displacement Vectors and Ray Azimuths of P and PS Waves
The theoretical curves of the ratio of the horizontal components of PS ~
waves (UpcY/UpgX) and the angles between the ray azimuths of PS waves and
their P waves formed as a function of p( , determi.ned by formulas of seis-
mology at differen~ values of ~ and ~ were calculated to determine the
effect of the angles of inclination of the interfaces on the displacement _
vector components of PS waves and the ray azimuths of P and PS waves. _
~
I ~~y ~
I .
I D1
I '
_ `s ~ ~z
, \ � ~-q
: � _L �-nJ
~ .
~ ~ . 180 � 27 -
..r{ ~~c~rPaAYc'' .
~ _S ~ i (1.) . 1 .
I ~
- I -
. ~ ~ .
~ �10
Figure 21. Ratios of Horizontal Displacement Vector Components
of PS Waves ApsX/ApsY and OPSY/UPSX as a Function
- of OC :
- 1--experimental values of ApSX/Apg~ for regions of the North
German Depression; 2 and 3--theoretical curves of Upgy/UpsX
- for horizontal and sloping interface, respectively, at
= 20�; a--along t
he dip ~ f the interface; b--along the rise
of the interface
Key :
1. Degree
The graph of the theoretical value of UPSY/UpsX is presented in Figure 21
as a function of the approa~ch azimuth o~ of P waves to the recording2s~t~ation
[136] at angles of inclination of the interface of 0 and 20� ~
iP2 = 30�36' and K= 0.32). Since the coordinate system selected during
field investigations differs from the theoretical system (see Figure 20),
54
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~ . .
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then the Y components of the theoretical displacement vectors of P and PS
waves correspond to the X components of the displacement vectors determined
by the amplitudes of experimental PS waves, while the X components corre-
spond to the Y components. At ~P = 0, the value of i~pgy/Upgg varies by
*_he law of the tangent. At 20�, the curve UpgY/UpgX is located to the
left and right of the curve UpgY/UpgX plotted for 0 as a function of
the slope of the interface.
2 ~
(1) ~C ) dW,rpa~lYc 50 � , _
dW,~paAy~ Y o �a BO ~
. 60 ~'S0 d-l0~ E gp 10 d-70�
~ IO ~ 4D � 5
S TO
10 9D 80 270 360 wZ,rpaAyc
180 270 J6 0
0
_1p � r -20
-40 ~ e t4, -40 y -
~3~ u
-6V � ~ PS
- � y,
d -
s dW, rpepyc ~ z
, dW, rpa,4yc 90 w
~ 3D ~x 80 1p t
1U co ~ ~ ~ ~ P
60 ~0 d~10 ~ S d'~
~ -9
2o s 20
~o eo r~o 3so o so ~so ~o J 0 w,rpBAyc
� 0 '
-20 -20 �
-40 ,
-60 . ~
.
~ Figure 22. Dependence of ~ and t~ 2 at Different Values
of tp and . .
Key:
1. Degree 3. Rise
2. Strike 4. Dip
Th~oretical graphs of variation of the angles between the ray azimuths of
PS waves and the P waves forming them ( are presented in Figure 22 as
a furiction of ~ 2. The calculations were made for a model of a medium with _
vP2 = 5.3 km/s, vpl = 3'.b km/s, vgl = 1.71 km/s, K= 0.32, cp equal to 5,
10, 20, 30 and 50� and ,Q equal to 10, 20, 30 and 140�. As can be seen
from Figure 22, the value of Q yi is sign-variable. It is equal to zero at .
angles of ~/i2 equal to 0, 180 and 360�, reaching maximum values at 2
equal to 90 and 270�. In other words, the.ray azimuths of PS waves lie in
_ the verti:cal pl:ane in the plane of the dip and rise of the interface, coin-
ciding with the azimuths,of the P waves impinging on the interface. The
-
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- maximum deviations of the ray azimuths of refracted PS waves from ray azi- _
muths of P waves impinging on the interface are observed along the strike
of the interface. The values of these deviations will reach 70-85� with
angle of inclination of the interface of CP = 50�. The values of Q.cv
increase with an increase of the angle of inclination of the interface and
of the epicentral distance.
56
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~ . . .
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PART 2
THE "ZEMLYA" DEVICE, METHOD OF OBSERVATION AND
INTERPRETATION OF MATERIALS
THE "ZEMI,YA" DEVICE
Moscow SEYSMICHESKIYE ISSLEDOVANIYA S APPARATUROY "ZEMLYA" in Russian
1977 signed to press 31 Jan 1977 pp 54-80
[Chapter 3 from the book "Seysmicheskiye issledovaniya s apparaturoy
'Zemlya "'by I. V. Pomerantseva and A. N: Mozzhenko, Izdatel'stvo Nedra,
1,400 copies, 256 pages] �
[Text] The Main Characteristics of the Optimum Design of a Device for
Continuous Recording of Seisznic Signals :
Continuous recording of seismic signals arriving at the reception point at
any time of day requires a special design of recording apparatus opera*ing =
for a long time without maintenance personnel. It should have sufficiently
wide frequenty and dynamic ranges and have the capability of recording sig- -
nals for a long time and maintaining given parameters.
These problems are being solved either by discrete recording of the useful -
informati.on or by continuous recording of all seismic signals arriving at
the reception point. Discrete recording of signals is accomplished either
_ on a magnetic ~rum or on a magnetic tape loop, where the signals recorded on _
the magnetic carriers are erased at the end of a single revolution of the
_ drum or magnetic tape loop and new information is recorded on the erased
track. The useful signals are read and sent to the non-volatile storage
unit befi~re erasure. This recording system makes it possa.ble to carry out
prolonged`~sampling of useful information, limited only by capacity of the
storage unit. One of the main disadvantages of the discrete method of re-
cording is the difficulty of identifying the moment of arrival of signals
with useful information. The known method of separating signals by ampli-
tude-frequency features sharply limits the capabilities of this method of
= recording since the signals of miGroseism background are frequently compar-
able to useful signals in both frequency and amplitude. More complex sys-
tems of separating the useful information result in complication of the de-
sign and an increase of power supply consumption, which significantly worsens
the technical-economic indicators as a whole. -
Continuous recording of all seismic signals arriving at-the observation
point is technically simpler but r2quires continuous supplementation of the
57
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information carrier. In the case when the information carrier can be re-
stored and used again after laboratory sampling of the useful information,
the continuous method of recording seismic signals is sufficiently effective.
Seismic signals are recorded continuously on magnetic tape for 100 hours or
more in the "Zemlya" apparatus complex. Frequency recording in the band of
0.5-15 Hz is provided at magnetic tape speed of 1 mm/s. Accelerated speed
of the magnetic tape is used during reproduction of the recorded signals
" [84]. In this case the emf and frequency of the reproduced signal are in-
creased in proportion to this acceleration.
The use of this phenomenon made it possible to use d.irect magnetic record-
ing to record infralow frequencies without introduction of any modulation
methods. Tlze use of some type of modulation is based on the use of an aux-
iliary high-frequency signal which varies its parameters as a function of
variation of the frequency of the recorded low-frequency signal. The aux-
iliary signal should have a frequency tens of times higher than the recorded
frequency in all types of modulation recordings. If the recorded signal is
- limited by a frequency of 20Hz, the auxiliary signal will be within the
range of 400-800 Hz. In this case signal recording will be provided at a
magnetic tape speed of 10-12~mm/s when using magnetic heads with working
gap width of 10 microns. This magnetic head provides direct signal record-
ings at magnetic tape speed of 0.25-0.3 mm/s. Variation of the frequency
of the reproduced signal (frequency transformation) permits conversion of
the superlow frequencies of the recorded signals to the seismic prospecting
frequericy band of reflected waves. This makes it possible to utilize stan-
dard seismic prospecting apparatus for subsequent information processing
both in e~naing and in discrete variants.
Block-Diagram of Apparatus for Continuous Recording of Seismic Oscillations
A block-diagram of a device having all the necessary components for contin-
- usou recording of seismic oscillations for a long time is presented in
Figure 23. A group of seismic receivers 1 is connected by a calibration
- device 2 to the inputs of seismic signal amplifiers 3. The calibration
device 2 transmits a series of signals to the seismic detectors anc3 ampli-
fier inputs at given time intervals, which makes it possible to determine
the parameters of the recording channels during reproduction.
, Z'he outputs of amplifiers 3 are loaded by magnetic recording heads 4, the
number of which is determined as a function of the number of working channels
and required two auxiliary magnetic heads which record time signals taken
from the output of the radio receiver 8 and quartz frequency standard 5.
The radio receiver receives time signals transmitted by a special ratio
station 18ri~.r by some other radio station. Time signals from the internal
quartz frequency standard 5, which are individual for each recording station,
are recorded on the second magnetic head. T'he time signals received by the
radio receivers turned to a sinqle transmitting radio station are reference
signals for the entire recording network and are usually tied to world time
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J 8 p /8 ;9
9
1 2 ~ k 10 11 12 i3
15
� 5 14 17
7 6 16
O
9
r r q ~ Y~ a ' ~ ~'n~~'' . 9 rk',~ m ~Ly ~s . ti
W .Yy"~{Yl,i~~t~~+~(z.{n+i`., '~~.s~.~,'
~ y~~ya ~ ~ ~ ~ ~ ~%c; , t�v,~',~~~u.~'S~. ~ ~ ~ ~.uo-~~ i ~ .
k a � `~z~ ~'3,s~",> ``K
! .~'~a ~H ~ y~,~ I~' ~'"~i
~~~~~~~I x~ ~ ,`y1 ~i~, i ~t
f . xr ~ P
~j'3 a ' y ~ i
~k f ~ a`' s'~5~~'
a~ k~t
K ; ~ , ~ �~d~
_ ~ ` r
~ ~ k'' ~ ' i^ L. 5. UY { . . .C ^Q'~a
( s s~,~ r'.,~,~.xr::.,,~.�.,.~'`'r~':e~.f~s~,~"k~~'""" ru~� asci-wra.�^~ ~ 3 `j -
~re~~ ~
~k ~
~qy,,
~,'t- SX't.~` ,j~" �t S, .i ~i'~~ ~ ~ ~ ~ I~II;N
o-+ y.. . ~ i
~
. L... . t
~ �~~i., :~,x~vll~,~'~~IIN~'~llti ~vw~i1,'~'
^~y~ ti~~ti-
P .
ti~~ ~ ,~,.~li
1 ~ t y~ i. y' 'v li ~
` ~~a; ;~'J, '1.~'VU ~'~W ~~tUl4l~~,J'J~M~'11~w
�~~iJ;~,~{`1~-,~ "ir ~'+~~1`~, i~~~~ak~v"~~a~~,.}~~ti~
~ _ . . Z~~;~`~~~y~'^+~1,~/~~414Y1:~L~~i~M~~'uL~Yi~4~Y4'~~~
~
, J~` ~ 5l.hV~S-L~L1Vti.N~~v11ti1M1~L\,~1~C'1Aw.n~Ltiyyw
~t
Fi:gure 52. Seismogram from Aftershock of Tashkent Earthquake
of 26 April 1966 with Disappearing Low Microseism
Background Prior to Arrival of P Waves -
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1~~ o
_ ~ ~
- N
- ' ~n
- - w
_ ~
- A ~
- ~
b
~ ~
a~
~
x
, ~
~
0
~
_ v
~
_ w
0
a ,
0
a~
_ a _
~
x
a
�rl N
f. ~1'
O
�rl r-I
. N
O 11
dr ~ ~
~ 0 ~
~ 4-1 X
~ a/ ~ N
~ ~ ~ O ~
a
N II
a ~ a
ri
v~ _
~ X N y
N
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Separ,ation Qf PS waves on recordings of earthquakes and explosions and
identificatiQn of them with P waves is accomplished by the following criteria
I~, 18, 20, 108]: recordinq of PS waves on the horizontal components of the
recording, identity of the shapes of recordings of PS waves and the genera-
trix of their P wave, the proximity of the recording times of P and PS waves,
the nature of polarization of PS waves and the distributi~n of their arrival -
polarity (at 10�) mainly by quadrants as in P waves and usually reduced
- intensity of PS waves by a factor of 2-5 compared to the intensity of P waves. -
The reliabil.ity of determining PS waves on recordings depends on the shape of
oscillations of the generatrices of their P waves. PS waves are clearly de- -
termined on recordings of those earthquakes for which only a single P wave
or packet of P waves having amplitude 3-5 times or more greater than the
amplitude of the preceding microseism background and subsequent P waves
(Figure 55) is recorded on the Z components. In these cases the first com-
posite wave is clearly determined on all the earthquake recordings. The
first P wave must be time-limit~d (1-3 periods) ~o determine the subsequent
PS waves outside the interference zone.
The characteristics of P waves fornu.ng composite PS waves. All earthquake
recordings with = 1.5-10�, hoah = 100 m and ~ 10� can be divided into
four groups by the nature and shape of P wave oscillations.
Group I includes recordings with a single clearly defined P wave in amplitude,
r~ecorded in the region of the first arrivals and having 1-3 phases (see
Figure 55). The epicenters of these earthquakes are located within Kamchatka, ~
the Kuriles-Kamchatka arc, Japan, in the Pamirs and in the Aeg~an Sea. The
foci o,f th.ese earthquakes are located in the upper mantle and ~their average
depths are 200 km. Some of the epicenters are located within the Tonga and
Kermadec Islands 140� ) and in the regions of the Aegean Sea ~ 2p
also with foci in the upper mantle (Figure 56). The P waves are, by their
nature., trans.ient waves refracted in the crust (P) and man~le (PK~). The
- nature of P waves which form clear composite PS waves at the crusta]. interfaces
outside their interference zone were determined in the following manner. The
time differences T-Tp of recording the first phases of P waves from earthquakes
(T) and the times at the foci (Tp) were applied to the Jeffries -Bullen hodo-
graph. As can be seen from Figure 57, the arrival times of the first phases
- of P waves recorded by "Zemlya" stations with errors caused by the structural
characteristics of the earth's crust and upper mantle under the.observation
points coincide with the arrival times of longitudinal waves refracted in the i
crust and mantle (P) and which passed through the earth's core (PKP). ~
' Group II includes recording in which a packet of intensive P waves rather
_ than a sir~gle wave is recorded on the Z component (Figure 58, II). These are
PKP waves by their nature. The epicenters of these earthquakes are located -
within the Kermadec Depression and Tonga Islands (Q N 140�). The depths of -
earthauake foci varv from 120 to 450 km.
* -
The values. of the epicentral distances are given for recording stations
. operating in the region of the Azov-Kuban' and North German Depressions.
111
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o , I
1/V~ ~ v~ ~ .4'M l~!~~
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[Caption on following page]
112
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~ � r ~
~
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z n
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~ 113
FOR OFFICIAL USE ONLY
;
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- Group III includes recordings in which two clear P waves separated by a time
interval up to 8-15 seconds are recorded on the Z components (Figure 58, III).
The epicenters of these earthquakes are located within the Kuriles-Kamchatka
arc (0 ~ 66-86�) and the depths of the foci are appxoimately 80-100 km.
- The first P wave is one refracted in the crust and mantle by its nature (see
~igure 57) and the second P wave, according to seismological data [65], is
a composite-reflected sP wave.
1c
2
PS~~ pPR�A pSM
r~
~
PS OC
~
PSPR� PS
~
~N '
- p ,
. Mw+n~nnrovwvvwu?w
Figure 55. Seismogram with Clear Recording of First P Wave
From Earthquake in the Region of the North German
' Depression: ,
- T= 2305, 11 Aug 1969, L~. = 75.8� and o( = 30.8�
Group IV may include recordings on which a large number of P waves comparable
in intensities and continuously following each other is recorded (Figure 58,
IV). The epicenters of these earthquakes are located within the Mediterranean
Sea and transasiatic belt of seismisity, in western Europe and within the
Atlantic Ridge. The depths of the foci vary from 20 to 185 km.
The distribution of the total number of earthquakes recorded by the "Zemlya"
device by groups of P waves is as follows. If all the clear recordings reg-
istered by "Zemlya" stations from remote earthquakes are taken as 100 percent,
the number of earthquakes related to group 2 comprises 15-50 percent in
aseismic regions. The maximum number of remote earthquakes (a ~ 10�) of
this type comprised 30-40 percent in seismically active regions (Tashkent).
Their number increases to 60 percent with regard to recordings from near
earthquakes (Q = 1-10�). The number of earthquakes of groups II and III
is also low and varies from 10 to 15 percent and from 10 to 30 percent,
respectively.
114
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� v~
~ . a
i � �~,ss ~ ~
ti , ~ . ~
.
~ � ~
� o~
. ~ ' ~ U ~
~ ~ ~
-r s,, b ~
i ~
; ~ $ i ~ ~
~
i ~ ~
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_
. ~
~ ~
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.
~4 ~ � ro ro
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W
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115
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Group IV of earthquakes is the most numerous and comprises 50-60 percent,
and sometimes 30 percent of the total number of recorded earthquakes. Re-
cordings of most catastrophic earthquakes are related to this group.
Analysis ot material obtained from the "Zemlya" stations permits one to as-
sume that the shape of the P-wave recording is apparently determined by
processes occurring at the foci at the moment the earthquakes occur and is
determined only at zones of large disturbances by seismogeological condi-
tions of the region of investigation and is essentially independent of .
The greatest length of recording P waves is observed for focal deptk~s up to
50 ]un, i.e., for foci located in the crust, and th~ shortest length is noted
for foci with H~ 200 km (regions of the Kurile arc, Kamchatka, the Pacific
Ocean, the Aegean Sea, Hindu-Kush and the Pamirs) and with H= 20-60 km
(regions of the Japanese Depression, the Aegean Sea and the Pacific Ocean).
The earthquake foci are mainly located in the mantle in both cases. No clear
- dependence of the length of rPCOrding P waves on ~ is observed for the same
earthquakes. A similar dependence of the length of recording P waves on the
Z component on the depth of the focus is dstermined upon comparison of re-
cordings from earthquakes obtained at significantly different values of
- but with shallow depths of foci [110].
T'bMNN l
~ ~5Q
5
~
32
18 ~ ~h 5~~~~~~ ~
y ~ SKS ~
24 PKS
. - SnP t � Q~Y
20 QQQ o
~ PSP ~ PNP
is 5 e~ e
.
?z . C,
p O
8 ~ Z
� O 3
: ~
4 Q
4
b
~ ?D 40 60 BO ~QO ~0 /40d,r c
P~Y (2~
Figure 57. Comparison of the Values of T-Tp for P Waves Recorded
by "Zemlya" Stations within the North German (1) and
Azov-Kuban' (2) Depressions and in the City of Tashkent
(3) to Jeffries-Bullen Hodographs (4) at hoch =
Key:
1. Minutes ,
2. Degrees ~
116
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. � ~
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, ,
- -
_ 4 r, , � a
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+ + ~ ~ ~ #i R~ -ri h ~ ~ 0
~ � � ~ ~ ~ 3~-i ~ N i b ~ GU)
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117
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Analysis of recordings registered i~i different regions, but from the same
earthquakes, showed that the shape of the recording of the P wave on the
wideband channel (f = 0.5-10 Hz) does not vary siqnificantly upon variation
of the epicentral distance from 30 to 100� when operating in sections with
sufficiently thick sedimentary mass, excluding regions with ~al+--~iome tec-
tonics. A ccrtnplex shape of the P-wave recording ~.s observed"in regions with
salt-dome tectonics and outcrops of crysta~lline rock to t~:e earth's surface
for these same values of Q. Multiple P waves apparently appear over the
domes. An additionally large ntunber of longitudinal waves of rather large
amplitude which interfere with each other appears in regions with outcrops =
of crystalline rock. One may assume that complication of the nature of re-
cording of P waves is related to complication of the P-wave front due to
the inhomogeneities of the upper part of the crystalline crust and super- F
, position of additional lateral P waves and also due to the appearance of
intensive vertical components of PS waves [110].
" Characteristics of recording and determination of composite PS waves. Com-
~ posite PS waves in the presence of a sedimentary mantle with velocities up
to 5 km/s are recorded only on the horizontal components (see Figure 55).
Composite PS waves are separated on recordings of local, near and remote
earthquakes from explosions. However, confident separation of them and
tracking are possible on recordings from remote and partially from deep- -
- focus near earthquakes of the groups analyzed above. The complexity of
determining PS waves on recordings from explosions and local earthquakes is -
explained in the following manner. PS waves on a recording from explosions -
may be confidently separated at the same distances and times where there are
- not other waves of any kind and when a single wave or a packet of P waves is -
recorded on the Z component. A large number of waves: surface, reflected
and single and multiple refracted whose total length exceeds 10-20 seconds
(Figure 59) is usually registered in the initial part of the seismogram re-
, cording upon excitation of oscillations by explosions = 0-250 km
The angles of emergence of all these waves are close to 45�, as a result of
which the same complex wave pattern is observed on the X and Y com~onents as -
on the Z components. With a time difference of recording PS waves from dif- -
ferent crustal interfaces of 0.5-1 second, PS waves with length of 10-20 _
seconds will be complexly interpreted between each other from each of these
boundaries. It is impossible to visually separate and distinguish PS csaves
related to different boundaries in this zone. The existing program of V. N.
Troyan [44] does not operate under these conditions. A similar complex wave =
pattern is observed on recordings from local and near earthquakes with foci
at the crust [110J. Moreover, PS waves from explosions and near and local
earthquakes have visible frequencies from 3 to 10 Hz. Ordinary phase correla-
tion of composite waves cannot be carried out for these waves with spacing of
5-7 km between the recording stations and vk = 6-9 km/s. Therefore, record-
, ings from explosions and near and 'local earthquakes located in the crust can-
not be used as the main recordings for separation and tracking of PS waves
fz~om station to station.
118
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r ~
w M 'r n.1e:~~
Z'...r`""'_"'~�~'~4. + ~V~ ~v~M ~ M1
P 'V
X
~:w~..
' -
" ~~^vvWl/W"rVww~.~.-~-,~.�
S
~ ' ~ N~M'~/~~r~~
r J"'1~
--------~--~w ~~n., ,n,n,~,.~ ~
�3!' `,,.,.-.~`,~.~y~''w"
Z2~~~ ` J .i' ~y ~ ~ ' ^1~~~~L ~I~
J' -v~~~ M" ~q~h/'~
~ r lfu~ ~,^'~W'~'.,
,rti+'~`+~-~1~-,~+.~~.'~,'~,~,,, ~~.~~t,,~.,~,,r~,~^"~f"~1~V'~''~�~I
- Figure 59. Nature of P-Wave Recording Registered from Explosion -
in the Region of the Pre-Caspian Depression: -
T= 0219, 15 Sep 1965, 140�
The PS waves (f ~ 1-3 Hz) are separated more systematically and reliably
= on recordings of deep-focus near (p = 1-10�) (Figure 60) and remote ~
(L1 = 10-160�) earthquakes. The shape of the P-wave recording from these
earthquakes on the same recording station spacing (approximately 100 lcm) -
essentially does not vary (Figures 60 and 61). A correlation seismogram
obtained by means of SS-24-61M stations is presented in Figure 61; the
spacing.between recording stations is 5-6 km and the total length of the ~
installation is approximately 100 lQn, The reproduction recordings have
both tlie use of 100 p~rcent mixing of three channels with overlapping of
two channels and without the use of these channels. A recording of one of
the Z channels is presented for comparison of the shape of thP P and PS wave
recordings and the tie-ins of them in time over the groups,of channels X and Y.
P ~
~
Z ,~,"'~v~'; , ~I.~1~~~;
~
~ v~W1.wL.n...`�~~~ W~?`l ~ ~~~I n
P S PZ 1 nPS M V. ~..,.,.~,~,-..:-~,,.ti'~'.. ~~ti ~
A�~
~f~r\ KWV`~}1~~1L~.^/~/1,J ~~j ~`M1'tl n~ ~ ~ -
MY ~"'~'V` V 1~, ~l~
~~t~ 5 1; y'~'t;i ~ ~ ~ I ~.I1, ~
~ n ~ �L .,,r ^ ~~,,~,,~1 ' p '4~~~~?y
i ij,~~;~,~l~,l'; � I.' h~~ .
_ ~ ~"""""^",/~r~,M,- ~�~/~,n, ~ Ir , r ~qJG
n '^^'1/~/~~ yti~~/~
` m,V
r II 'r;l~
= Y "~"~`''`^iy~~y 1`'1j~v~~;^' `r/1,~~~ ~ /~,~,C~, ~I,r'~'",?n r~!,~j~: ~u (I~ 4~;1 ~
~ ~`^N ~\~i` ~ n~~.r~i~~-~n;!~I~il ]I v~ '~^'1/~i+l y J. ~i.;'~ - ~n,t'~,,~. ),~~j,
"~'�vtilv`'~"`r'~ lrV~'Y~~ w1~~1~ i, � i~~'
1""y'v'~^-.lV~..--y.~';`w'~r~vyv~. ~,~,'L ,JI/~,~..,~,~~i1; .
-1!~ !"1 y l: ~
ww-�-_�ww..h( /~~.~H,~
~~+~1 ~ . ~~~"ti' !I f ~ ~ I,,, ~ ,
.-Z ' 'N""~r, .`��`i~ " r�`ti,~~''~' ~ti"~1'~~~'~~~~,~;:~ l~ il ~
~ v" 'vd~t`~~~~"r~`.:~; ~ I' ' ~ l
` ~M. ~~l+r'~ v1M1~,.ti ~l ~ 1 ~,1~~:~
~W'1v"LJ~,d`1~/'W1nP1d1./`?_,1,~(y`1.M~'1nr1,J`4~11''Y--!''~r^1,?1.�I~W`1.+MrM~%,MJ`1ih,~`t~^'.M.J1,P1~!`It"W'!t
y I: a ~~y ~ r ~ ~ ~ .y. fd ~'I ~ r'~ ~I
.~a~na.~ ~a w
7 ' bo
n ~ S~I N N H~ ~ v1 ~~-i
~ ~
- A~d.~ ro ~~-~I p OP~OAF�~~~ -
,a~ ~ 2 N �m O ~ ~ 'O ~ u~) .
~ ~ ~ O N ~ ~ ~ ~ t~d 'A
N 4-i A~~ b U 4-t ~ i
D ~ A N~' U O~
�
~ ~ ~d a ~ rt i' 3
ri I I a-? 1
~ al M~ N' N R7 H~d
� a o 1-~ ~ ~ ~ ~ ~ ~ 3~ 2f ~ ~ b N ~d �3
N ~ ~ g i b~ ~ N~~-? + A ~ t~d ~p
C~ .-I 2 fA W~ U H,L~
124
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The essence of correlation of PS waves by the regions of common (deep)
points includes the following. Depth distribution diagrams to the inte.r- -
faces are constructed (see Chapter 7). As a result of the fact that the
- sources are located at different puints with respect to the stopovers of
- the recording stations,' one can obtain recordings of PS waves at several -
_ stations and from different earthquake foci from the same point or closely
located points of the interface. The condition of equivalent depths (with
error permissible for the composite wave method) obtained for the same region ~
of poincs, but at different stations and from different earthquakes, permits
one to relate the considered composite waves to the same interface. A chart
_ of the surface of the basaltic layer compiled for the region of Tashkent is
presented in Figure 64. The error of determi.ning the depths comprises ap-
proximately + 1 lan. The regions of various depths outlined in Figure 64 by
the thin closed lines were obtained during recording of PS waves at differ-
ent stations and from different earthquakes. A single region of common
points permits one to note the same exchange surface, but obtained on re-
cordings from different earthquakes on the time profile. Analysis of PS
waves obtained in these regions and combination of them on separate sections
of the time profile into a single boundary permit one to draw a single con-
tinuous boundary, selecting the common deep points of the overlapping sec-
tions of time profiles by regions. The coincidence of the obtained boundary
with that constructed during phase correlation of PS waves indicates the cor-
rectness of the constructions. This check is especially necessary upon trans-
ition through fault zones where phase correlation of PS waves.undergoe~
separation.
PS waves related to different crustal interfaces have a somewhat different
_ ainplitude expression which is determined by the structure of the interface,
the size of the jump of velocities and the angle of incidence of the P wave
on it. PS waves corresponding to the same interface in regions of their
common points are easily sustained by intensity for earthquakes with differ-
- ent values of (but A~ 10�) and oC . PS waves of the same type on recor.d-
ings from earthquakes with similar values of J~ and are easily sustained
in regions with complex salt-dome tectonics.
The sequence of recording reference PS waves on a recording of components of
the same type and their number on recordings of different stations, but from
the same earthquake, are usually maintained.
Additional composite waves traced between the main reference waves may appear
in some cases at some recording stations of the same stopover, but from dif-
ferent foci. However, they are usually l~ss intensive under simple platform
conditions and do not strongly interfere with recording of the main reference
- composite waves of the investigated region.
Polarization of PS waves exchanged at the same interface (if its slope does
not change to the opposite) and the polarity of their rivals with respect to -
P waves remain constant for each earthquake. If the angles of inclination
of the interfaces vary by even 10�, the azimuths of the polarization planes
125
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so~~20 ~ ~ s
l9,~
h ~
~ ~ S~i
_ i
i ~z ~
~ ~
- ~ ~~~e, _'~s ~e 19
~ y ~~"'1j.~ 7 ~19,4 T4` ~n.~
/ ~.19,1 ie~8.5 ~ ros-~y tA,9 ~I I7,6
; ~y ~ ~p l7 ~ ~1 . .
~ .s- b~ ~e
~ ~ ~ zo,e ~ ~ ~ .
s
~ - - ny ~,n,a ~4 r
cq~ ~ n,s ~ ~s~~'~ n .
' ~s n 4 R ~s,a ,c,i ~ ,
~ S ~6r
n ~s z ~
~ n 1~$~~z a `5'~ ~~a-~ ,~~i
a~
~44 ~s,q ~ ~
~ ~az
/z1
~ 4
_ ~ , ~ s Q6
,~~~`,s �
L~qs ~ ~e
~ 1Q1
- a~ 119,7,1$3
,1~9 ,l$I ~r ~ Z
Figure 64. Diagram of Depths to Surface of Basaltic Layer in
the Region of Tashkent from Data of "Zemlya" Stations:
1--regions of conunon depths (km) with direction of
arrival or waves from earthquakes to the recording
stations; 2--confident (a) and doubtful (b) isolines
of depths.
of PS waves may deviate from the azimuths of the polarization planes of P
waves impinging on the interface up to 60�. As a result, PS waves may ap-
proach from quadrants different from those for P waves and the polarity of
their arrivals with respect to P waves will differ from that of the arrivals
of PS waves.recorded at adjacent stations with different orientation of the
interfaces.
The Wave Pattern on ReGOrdings from Local Earthquakes (Q = 0-40km)
Tremors of the soil surface from the aftershocks of the Tashkent earthquake
of 26 April 1966 during the summer season were recorded in Tashkent itself
126
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at intervals from 3 minutes to several hours. Adjacent tremors frequently
followed within fractions of a second, as a result of which several P and
_ S waves were seemingly registered from the same aftershock on the recordings
(Figure 65). Clear packets of direct P and S waves (see Figures 51 and 65)
were recorded and PS and SP waves were sparadically recorded on recordir~gs
from the aftershocks of the Tashkent of 26 April 1966. The time interval
between the arrival of P and S waves was short and varied from 0.8 to 1.5
second. The total length of recording all P and S waves reached 250 seconds
and dependent on the energy class K of the earthquake.* The length was in-
creased by an average from 10 to 250 seconds with an increase of K from 5.7
to 11.5. The magnitudes of the aftershocks of the Tashkent earthquake com-
- prised an average of 5.5 and the intensity was 4-7 units (from data of the
Tashkent Seismological Station). Microscopic earthquakes (with intensity
less than 2 units) apparently having foci in the sedimentary mantle were
also recorded by the "Zemlya" stations {Figure 66). The intensity of S
_ waves is 3-5 times higher than that of P waves on recordings from the after-
shocks (2-4 units), while the frequency is 2-4 times lower. The frequencies
of P waves varied from 8 to 10 Hz (Figures 67 and 68) and those of S waves
varied from 3 to 8 Hz.
_ ~_,~-t
_ ~
_ Z
P~ p
X
S, S'~
~ 1~
i~~vW~
' ~nn,,,w.
- zT .
- ic
Figure 65. Recordings of Weak Aftershocks of Tashkent Earthquake
- of 26 April 1966 with P and S Waves
*
The energy class of earthquakes is K= 1gE, where E is the seismic energy
of the earthquake focus in joules.
127
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The Wave Pattern on Recordings from Near Earthquakes 50-500 km)
Direct or refracted P and S waves are determined on recordings from near
earthquakes as a function of the relationship of Q and ho~h and clear PS
and SP waves are frequently present (see Figures 54 and 60). Direct waves
are recorded first on the recordings of P and S waves at A G hoch and re-
fracted waves are recorded at Q,~ hoch� P waves have frequencies of 3-5 Hz
- and S waves have frequencies of 1-2 Hz (see Figures 67 and 68). 2'he total
length of recording P and S waves is different and is greater by approximately
an order than that of S waves. The intensity of S waves is also approximately
an order greater than that of P waves (see Figure 54).
'a ~ b
_ y
~ ~---~-r-~v~..ti-~w~..v~.wu~'
~ y ~,_,,r
- Z~ , rwu~,.-w
P~
~--~X
~
_
~y �
.
~7~~ ~
~-w
1c
c .
~
~v~r V~
~ w,,.-wN..
/p
_ S
J~
- - - Y .
. ,
Figure 66. Recordings of Weak Aftershocks of Tashkent Earthquake
of 26 April 1966 (b and c) During the Interval Between
Recordings of Aftershocks with Intensity 2(a and d)
- The nature of the wave pattern on recordings from near earthquakes vari'es
- with variation of hoch and A. Deep-focus (hoch ti 200 km) earthquakes in
128
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the Pamirs and Tyan'-Shan' have the simplest shape of recording of P and S
waves and sharp arrivals. Waves from these earthquakes frequently have 2-3
periods (see Figure 60). Complication of the recording of P and S waves the
- same as for remote earthquakes is observed with a decrease of the focal depth,
_ especially when it is displaced into the crust: an increase of their length
and the appearance of various types of waves reflected from the crust and re-
fracted in the crust occur. '!'he clarity of P and S wave arrival and the
nature of i.nterference of P waves and ~specially of S waves vary with varia-
tion of Q. Arrivals of P wa�ies are more clearly noted at short epicentral
distances and those of S waves'are noted at long distances. This is related
to the fact that S waves are recorded on a background of intensive subsequent
P waves at small values of Q(0-70 km). P and S waves are already separated
by a time interval with an increase of epicentral distance and, beginning at
100-500 km, S waves are essentially recorded after attenuation of all
oscillations caused by P wayes (see Figure 54).
ISI ~
._x a
100 ~Z ~3
_ 80 ~ ~5 ~~a6~6~08
60 ~ ~
~
d / � ~
40 : ,
~ ~ ~
20 / br ~
. ~ ~ .
~ ~ ~ ~b ~ .
- p % IO ` ~O
f rq
0,1 ~ ,
Figure 67. Amplitude-Frequency Spectra. of P Waves Recorded by
Seismological Apparatus (1 and 2) from Earthquakes
and by "Zemlya" Stations from Earthquakes (3-6) and
Explosions i7):
1-- Q, < 10�; 2-- 0= 60�; a--hoch = 30-60 km; 6--hoch = 150 km;
b-- L~ = 1�; 4-- ,L~ = 20�; hoch = 0; 5-- L~ = 40�~ hoch = 30 km;
6-- 70�; a--hoch = 200 km; b--hoch = 100 km; c--hoch = 580 km;
. 7--P waves from explosions: a-- A= 50 km; b-- A= 60 km; 8--
frequency characteristics of "Zemlya" apparatus
- The general nature of variation of the wave field can be followed on the sum-
_ mary hodograph and the graph vk = f( Q) of the first P and S waves (Figure
69 and 70). The value of vk increased rapidly from 1.5 to 5.8-6.2 km/s for
longitudinal waves at distances from 0 to 10 km from the focus. At _
- = 10-45 km, the value of vk of P waves increases slightly =rom 5.8 to 6.4 km/s;
at 60-150 lan, the value of vk remains essentially constant and is equal
to 6.4-65. km/s; a decrease in the values of vk to 6 km/s is observed at
129
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= 150-180 km. A sharp jump of values from 6 to 8 km/s is observed at
l~ = 180-200 km. Some decrease of velocities to 7.6-7.8 km/s is then ob-
_ served at L~ = 180-300 km. Velocity vk increases from 7.6 to 9 km/s at
_ distances from 300 to 600 km. A jump of velocities to 10-15 km,/s is ob-
ser~ed at distances from 450 to 500 km. This sharp increase of velocities ,
is difficult to explain; it is not excluded that it is caused by failure to
consider some factor and is an error caused by the effect of the focal depth.
The values of the velocities of S waves~ vary within the following range. The _
value of vk comprises 0.6-3.6 km/s at distances of L1 = 0-165 km. A jump of
vk from 3.6 to 4.65 km/s is observed at = 165-180 km. The value of vk
decreases to 4.3 km/s at distances of A= 260-370 km. The value of vk in-
creases to 5 km/s at = 370-500 km and is equal to 5-5.3 km/s at 4= 500-
~ 600 km. ,
The Wave Pattern on Recordings from Explosions = 0-700 km)
_ Longitudinal and transverse waves are determine3 and PS and SP composite waves
are sporadically determined on recordings from explosions (see Figure 53).
Clearn intensive surface R1 and R2 Rayleigh waves, 5-10 times more intensive
than P waves (see Figure 50), are determined in regions with the presence of -
~ a.low-velocity mass of sedimentary rock, for example, within the Azov-Kuban'
Depression and Tashkent, on recordings from explosions. The intensity of S
waves is either comparable or 2-3 times higher than that of l~.waves. S waves ,
- freqaently are not determined by intensity among subsequent osci'lations af
~ P waves. The frequencies of P waves depend on and vary from 5 to B Hz
(see Pigure~. 67 and 68) and the frequencies of S waves vary from 3 to 5 Hz.
The first phases of Rayleigh waves (f N 0.6-1.2 Hz) have the lowest fre-
quencies. The last phases have frequencies of 1-5 Hz. R1 and R2 waves have
a clearly marked dispersion. The length of the recordings of packets of in-
divic~ual P, S and R waves from explosions is different: it is maximum (5-25
phasES) for R waves and minimum (5-10 phases) for P waves.
Th~~ nature of the wave pattern on recordings from explosions can be followed
= on summary hodographs compiled for the regions of the Southeastern Russian
Platfor.n, the North German and Azov-Kuban' Depressions. R waves were not re- -
corded in the first two regions. They were clearly determined on the record-
_ ings in the third region (see Figure 50).
A summary hodograph of the Southeastern Russian Series (Figure 71) consists -
of two branches: a summary hodograph of explosions and subsurface earthqua.kes _
with focal depth of hoch ti 0 and a summary hodograph of earthquakes with
hoch = 30-50 km. The points of the hodograph at hoch x 0 are easily averaged
by straight lines along which five different values of vk can be determined.
The dips of the hodographs correspond to distances of 160, 200-220, 400 and
500 km from the point of the explosion,
130
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~
4-~ U
Ul O A
c: G dG r1 td ~ N
0 N td b' ~
v4'i ,ta �rl .'3 U rt3 U! �rl
~ ~ " ~ bi O 'd ~1 td
+ ro,[~ w ~
+ a m ~ ~ o o -
~ �
o~ ~ ~ b - v N w~ b
~ +~0�~++i ! a ~ o ~ ~ ~ro
O .
+ N~. ~ N~.~ 3 O b~
_ I 0 ( ~
_ *
I ~OO I O O O Ul a r N
I x s m~ I ~ ro y.~ ~ _ p~ R
1 z -
u
o ~ T 41 L: ~ L: e-~I N~ U
I fix ���'~,,I�Y���� o a 0 O~ ~~~U U.C
~ 4...~� _
I,~ ~ I V N~ I~ N Li �rl 3
~ ~Y I � ~ ^ ~U t~l~ M N 4-1 ~'U ~
~ q �f O N t~
~x ~ ao ~ - ~ - 1a =
+ ~ I ~ ~ r-'~I f~3 ~ (~d N ~-~I 1
y, N ~ ~ 'd r-1 ~ O
*x~ I w L�7.-.N ~ A N~
( y= r c O N=
~t t R rl tfl ~I �rl (d
� : ( A ~.�~ww Dw+~
r, �f~s s* # . ~ cn u-i ~ ~d -
- ` ~ # rNl cn td N O ul
� " � o^ � w.~~b 3 aNi a,c~i~ ~
~ ~ b u I ~ b�r'1 ~ ~
- . ~q N~~'~ ~ b b ~ S-I A
- I x + ~ 8 3 r~l ~ ro'Jr f~"d I A~ U .
x.� ~ ~ i ~ rts ~ r ao N v-~ cv
~ x-~ I ~ -O ~mc`~i~a -
+ o a
, ''i~'~~~ ro.~~~~o~~No
~ X~~ I~ ~ ~ ~ b~ O U N.Y, U1 �rl
Hrr + I ~ o ~n 1d .-~I O G~ G) ~ ~ b~ ~~-i -
I * I ' "~..a~ ~~N~~~~.~~o
( i f I ~ ou~�~~~a~+~a~a
* ~ ~ N ~ � a ~a u~i - ~ uR'i b ~ rd
* fn U1 I N bi N N N
I % i++ + I ~ _ _ ~ ~ ~ I ~ N ~I UI
I * t + � `S ~ D+ ~ ~ 0 4~-~ ~ ~ ~ 0a
i~* + ` ~ ~U'~l IA O O
~ d N' a~ rtf rOl r~-I ~~C' N 3 0;
i~ I ~ ~~Q U Ul Ul f-1 rl -
I o W U 41 �~i O~ rl '
~ ' N �O au~'i~~~w i
- ~ m ee~e--~ee I ~ a ~ ~ uNi t~i N ~ ~ C ~ ~ -
I e *e .
_ ~ ~ h ~3 tr'~~-~i ~ ~~ro ~
~ . ~ . , N ~a ~ w~'~ x
~ r, ~ #
,,~1~~ ~ ~ ~ ~ ~j
~ ~ v ~a`~i~�~~,~a~
d~N o o ~ 7' cv C�q O C' C~ C'~, o~O" . ~ r~f ~ rl ~ N rl
R1 ~I ~ N ~ .L' ~r 41
[~a ~w~n vA ~
~ 131 -
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_ T_, C ~ -
o~ ~u a~? ~ h ,
~
~ ~
2 � .
i ~
wh~ � .
_ =f ~
1 wp P ~5 6 9A
~ ~l~' ~ ~5 ~ ~ 99~
/ ~ ~ay
~ r
~ ' ~ _
.
- ~~,uc, ~ 9$~
8
~ ~x
. yjf ~6
~ ~
6 ~ .
i ~ ~ _
_ ~ 5 ~
0 ~
0,5 ~ 6 1 0 k
/ ~ 6 OZ 05 -
~ ~3 ?,4 6
~ 100 200 300 4C0 500 Q,KM
Figure 69. Summary Hodograph of P and S Waves Compiled by
Recordings from Near Earthquakes and Explosions -
for Tashkent (1-3) and Rayons Around Tashkent(4):
~ 1--hodographs of first arrivals of P and W waves from seismo-
logical data of Ye. M. Butovskaya; 2 and 3--hodographs of P
- and S waves from data of "Zemlya" stations compiled by explo-
- sions and local earthquakes, respectively; 4--hodographs of
first arrivals of P and S waves com'~iled from seismological
data of Ye. M. Butovskaya at hoch -,0; 5--averaging lines
for individual earthquakes; 6--values of apparent velocities
in km/s
A summary hodograph of the first arrivals of P and S waves of the North German
Depression was compiled from recordings from special explosions at known coor-
dinates and at the moment of the explosion (Figure 72).
Averaging of the points by the least squares method made it possible to ob-
tain linear hodographs of P and 6 waves with the values shown in Figure 72.
The points of the dips of the hodographs of P and S waves arrive at approximately
132
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~
~
I � ~w ~ ~ ~ -
Q ^
+ + ~ ~ ~
- . jI ~ ~ ~ . ~ ~o~ u -
- ~ i w o ~ o
I i : h ~ N
1 ~C 1 ~ ~ ~ ~ ~ O
~ ~ ~ b ro a~ b ~N
x~ o tr,~ 3 a~i
~ ~ ~ ro~~'~
b o ro a~
b x~,~~
~ d~ ~ ~ a v
~ tb 34.,w
v, ij ~ ob
I t7 p~
UI N I
o. ~ id ~ ~ ~ W d'
I t ~td ~b
. ~�I o x wab~r~ �
~ ; + r. w b
I j . ~p~ri
N ~ b'
~ I w t~~ H
+ ~ ~ xo i o ,
~ ~ N U
j ' . 40i 4-1 ,~t.' N ~1 ~
x N O
I b
_ . o
_ ~ o o, w s~
~ ~ i ~ro~ -
?,~r~ ~,~~ab
~~I
i ~ � -
I j ~ -
~ ~ ~ ~
- o o
. ~ ~ ~ ~ w
~ -
0
~ q ~ ,
~
- ~~-x-
Y ~ ~
p OO V N ~ ~ ~ ~
~Y
133
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9
/
. , ~ _
T-T ,C ~
/
ISO ~ �
i
/
~
~
d
r
. /
S
. ~c~~ _
. y
. �
!00
i ~ P
i p
i
d~. ~~i
.
, ~
~~6 ~ o~`~
? . 9 %~'O~
. ,
.
50 ~ 8q a0~t .
~6 ~
.
6;~
~59 ~ ~2 ~3
.
j ~5 6 S(Z 7 _
~ 100 1~ ~00 400 500 600 d,KM
Figure 71. Summary Hodograph of First Arrivals of P and S Waves
Compiled from Recordings from Explosions, Near and
Local Earthquakes for Regions of Southeastern Russian -
Series:
- 1--arrival times of P and S waves from explosions; 2 and 3--
arrival times of P and S waves from earthquakes at hoch = 20-50 km -
and hoch ~ 0; 4--theoretical hodographs of direct waves at hoch =
= 23 km; 5--certain sections of summary hodographs; 6--uncertain
sections of summary hodographs; 7--values of apparent velocities
in km/s
the same distances from the point of the explosion: 2.5, 18, 28, 62, 83, 126,
135.5 and 178 km. �
The following group waves: direct P waves related to the sedimentary mantle
. (vpk = 0.78 km/s), refracted P waves (vpk = 6.5 km/s) and refracted S waves
134
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. . ~
~ ~ ~ f Y Ul ~d
' a O b O
' ~ N o ~ ~
: . . . ~ ro ro
.
~ ~
.~s ~ ~i
~ ~
� i '.a ; �u' i
. 4' ~ ' ~
~
� M ~ O
j �
_ s. d 4~-I Jy N -
. � r-I Ry
~ ~ ~ o N ~ b~
�rl R1
.
tn�`'�~' ~ 3 U N
~ � � ~ � Ul LL t~C
. ; " o "i rn U1 1
- � ' ~ t U+ ~ [ro.' 5~~1 ~11
~ fd
. s a ~n
~ � N 4-1 > tad
' ~ 3 b,
i � �
r~-I U] ~ \
� ~ � N
'J ' 'L[7~! .r ~
~ ~ ~ ~ a 0 1Y ~
� ~ ~ ~ 'N a ~
tA N
� iN-1 W W tn
tr �rl N �rl -
+ ~ W A ~ ~ 0
~ ~ 4-i ~ O b~ ~-I
' � . iD O ~ �rl Rf N
_ . s. ,s"+ 1~1 b N ~
�u .w w~+~ D+~
� rd C7 N td ~
~ti ~ ~ ~
. ,
.�s ~ ~ >r ~ W
`
~ `v�s, x 2 ~ N
� ' N ~ _
q N N �ri 4-t
~ = O 0
. ~a+~w wN
~ ~~~o ~ t~ o i a~
~ ~w~~'ro
N
d~,, ~ � + N ~ 'I
r N 3~0
~ 9~ ~ roax
~ ~ ~ h ~ M N ~ ~ ~ R~ O ~ _
w ~ w a~
~
135
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~ (vgk = 3.6 km/s) related to the Paleozoic Basement and surface R2 (vk = 2 km/s)
and R1 (vk = 200-500 m/s) waves, are determined on the summary hodograph from
explosions obtained on the longitudinal profile within the Azov-Kuban'
Depression [59].
The Wave Pattern on Recordings from Remote Earthquakes (L~ = 10-160�)
P and PS waves are registered on recordings from remote earthquakes and S
waves are registered at L1 N 70�. The foci of the remote earthquakes recorded
- by "Zemlya" stations during 1962-1974 are presented in Figure 56. Most of
~ them are located in the Pacific Ocean seismically active zone and within the
Central Asian and Mediterranean Sea seismically active belts. The foci dis-
tribution of these earthquakes in depth are presented in Figure 58. The mag-
_ nitudes of the remote earthquakes determined by "Zemlya" recording stations
are presented in Figure 73 for five regions: the Pre-Caspian, North German
and Azov-Kuban' Depressions, the transition zone from the Southeastern Russian
Series to the Pre-Caspian and in the region of Tashkent. A similar nature of
the graphs was also found for other regions of the Soviet Union where inves-
tigations were carried out with the "Zemlya" device. Earthquakes with mag-
_ nitude from 4 to 7 have been recorded at all epicentral distances. The great- -
est number of earthquakes was found with magnitudes from 4.5 to 6.5.
A graph of the distribution of the number of earthquakes N from their epi-
central distance, recorded and accepted for processing in these regions, is
presented in Figure 74. The largest number of recorded earthquakes for all
the regior~s was found at epicentral distances of 50-76� from the foci located
in Japan, in the Kurile Islands and on Kamchatka. A rather high maximum dur-
ing reaording.s from earthquakes in the region of Tashkent is noted at L~ _
= 1.5-8� and corresponds to earthquakes with foci in the Tyan'-Shan' and
Pamir Mountains. The maximum values of N are noted at ,~(~,equal to 100, 130
and ].50�. They correspond mainly to earthquakes with foci in the Pacific
Ocean, the Kermadec Depressian, the Tonga Islands and so on. And finally,
a maximum of N at,(~ x 18-20� has been noted during observations within the
North German Depression. It corresponds to earthquakes with foci in the
Mediterranean and specifically in the Aegean Seas. The depths of the earth- _
quake foci within all the maximums determined in Figurp 74 are located in
the mantle.
The azimuths of the P wave approach from remote earthquakes o( for all re-
gions are presented in Figure 75. As can be seen, the waves from the earth-
quakes approach the recording stations from all directions. But their maxi-
mum number for all regions is observed at o( = 20-35� and corresponds to
earthquakes of the Pacific Ocean zone with epicenters in Japan, in the
Kurile Islands, on Kamchatka and so on. An additionally increased number
of recorded earthquakes with O( = 110-170�, corresponding to the seismically
active zones of the Tyan'-Shan' and the Pamirs, was observed for the rayons
of Tashkent.
136 -
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M
8
~ � e ~
1 ~ + o � � ,
o � �a* , , , �
,o b~~~ 8~ ~ 8~~~go 0
6 .o.~~oo~~BB,,444 o
. o ~.e ~ o � �o . Ib~ -
o ~ ~ o ~ �
5 ~ tg.r , �
d^ o 0 0 ~ o
~ � ~ ~e
~ M r + 1' otp
4 o .
/00 l50d,tpu8yo
p 50
' - OZ ~3 ~y ~S -
M . .
8
1
. .
6 + *
.
5
4
J Jp 40 SON
p !0 20
Figure 73. Graphs of th~ Dependence of Magnitude M of Remote
Earthquakes on p and N:
- 1--Pre-Caspian Depression; 2--transition zone from Southeastern -
Russian Series to Pre-Caspian Depression; 3--Azov-Kuban' Depres-
sion; 4--rayons of Tashkent; 5--North German Depressian;
2'he wave fields on recordings from remote earthquakes can be represented in
the form of statistical time profiles--time models of the crust for Tashkent
- and the North German Depression (see Figure 63). Maximum numbers of PS ~
waves corresponding to the main velocity boundaries of the earth's crust are
- o~served on these profiles for both regions. The nature of the maximums,
their distribution and the number N of PS waves with an increase of Qtps-p
and H vary for each region in their own way. The maximums for the regions
of the North German Depression (a yound series) are clear and narrow. Their
- values decrease only for the intermediate interfaces of the earth's crust
with an iz~crease o� L~. tpg-p and H. They remain comparable for th~ basement
surface and the Mo horovicic discontinuity. The maximum PS waves with an in-
crease of tpg_p and H become indistinct and their amplitude decreases for
the region of Tashkent located in the transition zone to the mountains. This
is especially evident for the transition zone from the crust to the mantle.
These factors may qualitatively indicate the different structure of the crust
and the transition zone from the crust to the mantle within the series of
�ormations and the geosinclinal zones.
137
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N
- ~
SO
40
_ '
30 1=J2
3
~4
20
10 + -
+
- ~
a
+
~ 50 ~ 100 150d,rpaAyc
_ Figure 74. Graph of Distribution of Number of Earthquakes N
Recorded from Foci with Different Values of
1--Pre-Caspian Depression; 2--Azov-Kuban' Depression;� 3-- -
rayons of Tashkent; 4--North German Depression
138
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x
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~
.
.
~ \ ~
_ p~ ~ `
~
o /
� o -
270~----__ ~ ~a - --gp�
- � s ~
_ o~
.,~Z
-Q3
lgp�
- Figure 75. Graphs of Approach Azimuth Distribution o( of P _
Waves to Recording Stations from the Number of `
Earthquakes N:
1--North German Depression; 2--rayons of Tashkent; 3--Pre-
Caspian Depression; 4--Azov-Kuban' Depression
- The Nature of the Wave Field in Fault Zones and in the Presence of Subvertical
Contaczs of Media of Different Petrographic Composition -
Clear separation of the fault zones and subvertical contacts is a complex
problem which requires consideration o� alI the factors outlined above for
all types of P, S, PS, R and other waves. The fa~lt zone and media contacts
have the greatest effect on transient composite PS waves, which are not formed
upon disappearance of the boundary in the fault zone. Lateral PS waves may
appear in the presence of a sloping contact. Transient P and S waves and
- also R waves may only be attenuated somewhat in intensity, while their arrival
times are deflec~ed from the normal hodographs of these waves.
139
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~ a P
Z,
I PS
T
X
PS
Y n~w
P ~
Z
~,M
J''?,i
W'~J~,I"W"W"~J'W'W'W"U'~,f'
Ic
. b p
z,
x
y
- P
ZZ
- ~
= Figure 76. Seismograms Obtained A,bove Sections of Normal (a)
and Disturbed (b) Structure of the Earth's Crust
in the Rayons of Tashkent:
T= 0819, 15 Oct 1969, L1 = 170.5� and a( = 318.2�
140
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. P~y ~
~ -----v i P ~
i ~ ~
~1
Z J' - u~ n~ `~~l11~
~ _
u~n ~
-
~
P P .
Z ~ '
~
, ,
X ~
~J
- ~ ~ . , _
' Pg~~ ~ oc PS PI,
PS au
_ , z p~~~~ au P, z 3,n PS
. ~
_ ~ ~ -
,
_ Y --------~--%N` 1/~
� . _'~-'_"'~v~V~~ ~J V ~ '
r ~
.,----_~pgp~ `~^~-----PS~~ ~
" , tc ' ps 61 ~
Figure 77. Correlation Seismogram Obtained by Using SS-24-61M
Stations in the Region of the North German Depres-
~ sion. The cross-hatching denotes the location of
the main North German Fault -
_ 141
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Analysis of P, S, PS and R waves showed that the fault zones are determined
by the following features: a) by sharp decrease of the PS wave amplitude
until total disappearance baove the fault zone* (Figure 76); b) by the com-
plexity of shape of the recording of composite and sometimes of longitudinal
waves (by the appearance of a"broken," higher frequency recording); c) by
the presence of a shift in the recording times of PS waves on the X and Y
components; d) by the appearance of lateral PS waves which are transient dif-
fracted and transient reflected PS waves from conta~cts of rock different in
petrographic and physical composition upon re-recording on tha SS-24-61M
station (see Figure 62, a and Figure 77); e) by the presence of a time jump
of Q tpg_p upon transition through the fault zone; f) by variation of the
polarity of arrival of PS waves; g).by the presence of a large number of PS
_ waves which fill the entire ti.me space; h) by attenuation of the P and S
wave intensity during passage through the fault zone; i) by deviation of the
recording times of P, S and R waves from the normal hodograph and k) by the
presence of foci of current movements ~f the earth's crust.
*
Disappearance of PS waves may be caused not only by the fault zone, but also
by a larger angle oF inclination of the interface.
142
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THE DYNAMIC CHARACTERISTICS OF EXPERIMENTAL P AND PS WAVES AND THEIR
COMPARISON TO THEORETICAL DATA
Moscow SEISMICHESKIYE ISSLIDOVANIYA S APPARATUROY "ZEMLYA" in Russian
1977 signed to press 31 Jan 1977 pp 134-160
[Chapter 6 from the book "Seismicheskiye issledovaniya s apparaturoy
~ 'Zemlya' by I. V. Pomerantseva and A. N. Mozzhenko, Izdatel'stvo Nedra,
1,400 copies, 256 pagesl
[Text] The dynamic characteristics of P and PS waves for earthquakes with _
1.5-160� include the shape of the recording, the ratio of the PS to P
wave intensity and its dependence on the parameters of the medium, the visible ~
per?ods, the frequency spectra and the polarization of PS waves. Based on
study of experimental data on the dynamics of P and PS waves and comparison
of them to theoretical calculations, the criteria for determination of P and
PS waves on earthquake recordings have been formulated.
- Most dynamic graphs were constructed for P and PS waves for two regions: the
North German Depression (600 earthquakes) and the rayons of Tashkent (400 ~
earthquakes), since the channels of the "Zemlya" recording stations were re-
liably calibra~ed by their sensitivity in these very two regions (see Chapter
3). The erros of channel calibration by sensitivity did not exceed 10 per-
cent, while the phase shifts did not exceed 1/20 of the perifld (0.05 second). _
The amplitudes of P and PS waves were masured by phases not distorted by
interference phenomena for construction of the dynamic graphs. Seismograms _
with the presence of remodulated P and PS waves were eliminated from processing.
The Shape of Recording of P and PS Waves
- It was noted during experimental studies with the "Zemlya" device in the pres-
ence of clean, noninterference recordings that the shape of the PS wave re-
cording easily repeats the shape of the P wave recording (Figure 78). `
- The values of the coefficients of the cross-correlation function between ampli-
tudes of the same type of P and PS waves were determined to determine the degree ~
of similarity of the shape of P and PS wave recordings. Wave recordings outside
the interference zones and usually in the reqion of the first arrivals were used
in this case. The cross-correlation function coefficients were determined by _
143
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a P
_ ,
_
Zt
~
/ ~ PS~
x 'Vw.~.,.,-n -
� PS
,
MN~
Y
P
Zp
.~.....~...r.,... -
_ 1JV Vf~~l~~~ .
iC � �
_ b P I -
~
_ ~ Z~ 1 V1/w~/~- -
PS
. v~
X -Jv
~.~.~./W"L?1^^.~^. -
~ ti ~~,~?.^~/w"~V1N
PS'
/1 ~ -
z
- NY
+.NN-~M~'~MV Wy."""vww,^.�ti1n,PM�,/U .
P
Z ~I -
~~Lv~h'~/l~l~
^.~Nw1h
ic � , '
Figure 78. Shape of PS Wave Recording from Near and Remote
Earthquakes Recorded in the REgions of Tashkent (a-c)
and the North German Depression (d and e): _
a--T = 0113, 23 Sep 1967, Q= 4.6� and o( = 158.6�; b--T = 0408,
24 Sep 1967, 64.5� and o( = 107.4�; c--T = 2032, 18 Dec 1967,
= 4.5� and d( = 103.5~; d--T = 0203, 3 Oct 1969, 71.5�
and D( = 23�; e--1220, 10 Jan 1970, ,Q = 98.5� and = 66.4�
[Figure continued on following page] .
144
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[Continued from preceding page]
C p ~
_ � \
Z~
X
PS
_ ~ f ~
Y-
_ P
8
!
ZZ v~N~
; ',~~r~~?^ -
_ .
~ a
,
~
PS
r
~
PS
VV~J~ ~
P
PS �.i.i..~�~.n~
Z
P
7t
- Figure 78 (Continued)
[Figure continued on followix~g page]
. 145
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[Continued from preceding page]
e
_ ? J 4 n
PS
_ ~
! o r 2 ~ n
PS �
' ~
- . PS
, z , .
P �
1c
Figure 78 (Continued)
- by ordinary formulas of mathematicalstatistics [71]. The dependence between ~
the amplitudes of phases of the same type of P and PS waves was linear for
the greater part of the material, while the correlation coefficient was in-
cluded in the range of 0.8-1. Similar values of the cross-correlation func-
tion coefficients were found upon analysis of the shapes of P and PS wave
recordings, theoretically calculated for different models of the interfaces
of the crust and the transi~ion zones between its layers (see Table 4). 2'his -
permits one to assume that a similar shape of P and PS waves recordings is a -
sufficiently stable and reliable criterion for determining PS waves on the
recordings. -
~
Ratios of the Amplitudes of PS to P Waves and Their Dependence on the Param-
- eters of the Dledium
The ratios of the amplitudes of experimental PS to P waves (Apgq/Apw), the
first of which (Apq) were recorded on the horizontal components and the second -
of which (Apw) were recorded on the vertical components for the regions of the
North German Depression, vay from 0.1 to 0.7, sometimes reaching unity (Figure
79). Values of Apgq/Apw which exceed 1.5-2 are rarely encountered.
Graphs of Apgq/Apw were analyzed for each crustal interface as a function of -
the epicentral distance Q, the azimuth of the P wave approach to the record-
ing stations o( determined b~ the formulas of [136], the angle of incidence of
the P wave to the interface i, the angle of inclination of the boundary cP at
values up to 15� and depth H and structural shapes of the; interfaces (Figures
79-81). A wide variation of the values of A
pgq/Apw is ob~~rved on all the
- graphs Apgq/Apw = f( Q, a, i, , H), An irre ularit is `
~ 5 y poorly determined,
146
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~ U ~ '
�
� ~
� ~h~� ~ 10
. � � � L. ~ I
- � ~ II d ~rdM O tr~
~ a~i ~ ~ ~i a ~ -
� ~I t~n ui o~~a N
I~ ~bb,~ama~n~ _
~ ~r~~+~ o~ ~w~
' , 0 ~ U ~ ,Nq ~p?., O
I $~.1 ~ td > N Ul b
' � p$ ~ao ro~ a~ 3 u�,.~+~i
_ . II ~tr+ ~ ~ b cn a~i s~ -
~ 4 [n r-+ A O 3 ~n ul
~ a td m~~ rd b
� � � ' ~ ~ I~ V .1-~
� � ~ � ~i/ � ' �I~ 4~ rd t~ rd ~ R3 ~1 N
p A C'. a+ 1-1 O b~
� � �
� U ~ U W ~ N'd ~W
,I ~ ~ ~ ~ i~ ro ~ ro ~
~ N~ ~j~N _
~o
- .a.�. ~ a~i ~o~a~',,~~.~
. ' � � w ro a~ w ~ ~ -
~ Q~a~ a~x3ow
� .~I oo~w~~~o~+~
- , . � dMa I ~ ~ 3
A ' ~ a~ N,�~ro o;;,.
. bbw~+~~~~~.:,,
- 01'~ A ~ c~.7 ~ a~ p~3 W~.~
v~ ro o
Q Q~N ~ ro dI N N~"~ O�D ~
~ N � i, ~ ~ O ~ ~ I~ N ~ O
~ ~~i~ ~ � ~C ~ G1 I �ri ~ CT W ~d �rl 4-1
~ . ..r~~:.�. ~ oro~vw?S~o~
~ ~ .
� � ~ia ~..ro~'oc~'dowo
- ~ ~f ~n zso~a~~~w~~
II ~ rt ~
b ~ � u~ b
� ~d N ~d ~ ~
~ ~a~~a~wws~~, ~n
� I td rl I U~~I ~ R1 N b
' ~ ~ o ~ ~~a,~ww ~�n � a ~ a
- . . o m~ ~
_ � � ~ II ~ U N U w
.
- ~ ; . w~ ~H o ~ ~ ws~ r�+
~ ~ d ~ ~ i ~r~ � I ~ ~3 tn rd ~ 3 ~ N ~ O
w
� ~ N PO H O~.~' ~
I ~ ( Q 4-I 'd ~~D G+ O
� ~ ~ ~ � I I r R7 ~ U ~ b ~ ~ ~ 'd
. o~v a~ ~ s~ ro~ a a~
.
' ~ I tn ~ ~ ~ U `n`n 3 ~
- . ~F . ~ ~ I ~ ~ H ~
~~~rtc`~iro`"ay ~ -
. "
. . . O � ~ ~ ~ ~ U ~ ~ la cn a~i ~
~ a o ~S w cr
o,, �1 ix~~+~~a`~i w
~aN ^ a ~A~~?3~dbs~ ~
Q Q
147
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~
'~Q,.~~~~ ~
t d r ~ ~
. ' v
~I
_ ' ~I
~ ' I
� � ~ o
� o
~
~ ~i
- ~ ' . ~~tf
, 1~ I
~ ~I
. ~ yl~'
� �
I ~ .
~ ~
� � ~ ~i~Iu ({~i ~I ~
� ~
~
� i w~~If(~,p~~ ~ y
� � N~ � � M ' I ~
~ I ~
a 9
Q Q ~ N ^ ~ U
~
~
N
' ~ ~
i ' ~ w
�e ��i~~ ~
- a -
~ ~I
II
d, ~ � + ~I o
w ~I � ro
. �
� . ~ a
~ . ~
. � . .
_ TJ M~~� ~ � � � I {~y .
~ � � ~r ~ � ~ I ~O
Q) � ~ ~ I
~ I ~
a ~
I~o p
_ ~ ~ I ~ _
~ � io . ~ o
. . . ~
~ ~
~ . . ~ ~
~ . . . . � � ! ~ ~
� � O ~ � i~
U U ~
" a~ ~ u
. ,Z Q N p
- 148
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A~ -
e
2
;
- ~
4
~ � .
. . � .
� ~ . .
. �y . `ti�� o. .r
M'J j ~ ~ ~ '
. ~ ~ _ ~ - � � �
� � S ~0.
~ ~ � ~ � ~ Si
j ryryry~~~ 111 � �
� - �s . ~ : : . .
- ~ ~ ~ ,
~ Sp t00 4,rpaAyc I
Figure 79 (Continued)
although a slight decrease in the value of Apgq/Apw is noted with an in~rease -
of the epicentral distance and depth of deposition of the interface. This
may be related both to the absence of any common regularities and to the fact
that a large amount of material obtained under similar, but still different
geological conditions was used in the analysis. ~
The corresponding theoretical curves calculated both with and without regard
to the absorbing properties of the medium were plotted on the experimental
graphs. The values of the absorption coefficients for P and S waves were
assumed equal to D(p = o(S and o( p= 2 ~C S� The derived experimental values
of Apgq/Apw on the graphs of the dependence on (see Figure 79, a-e) and i
_ (see Figure 81) ar~ mainly located between the theorietical curves of Apgq/Apw
calculated for thick-walled media with interfaaes of first kind at o( p=
= p( S= 0 and p= 2 0( S� the theoretical values of Apsq/Apw = f( A), also -
calculated for thick-walled media but for the zones between the crustal layers
represented by benches of thin layers (see Figure 6), even without regard to
the absorbing properties ot the medium, are located above the experimental
values of APSQ/Apw. The derived data permit one to assume that good agreement
between the theoretical and experimental values of Apgq/Apw is observed. This
, coincidence may be the result of ~khe effect of two factors~ the absorbing
properties of the medium and the structure of the boundary (zone) between the
crustal layers. Each of the factors can be reduced to a significant divergence
of the experimental values of Apsq/APW.
_ 149
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� � o 00 �o b pp~o~�~ � ~ -
. 000 ~ O Oe~O~ ~S ~ jti
~ O O �~O� 00 O c[ �rl
� O � a U~ N ~
~ a ~ a~+~+~
0 0 0 0 o d~ c~ Q o Z3 ya
o~ d� oo~� oo~~~ t5~ 0 Gl W rtf 0
0 0 00 ~ ~ U
T1 N
~ ~ ~ ~ U3 N ~ ~ ro
� 0 O a o O O~ 0 0 i o O~ � ~ z ~ W�~-1
O O~OOOD O O � � ~ ~ �~-1 O U �
N �rl
�
~ pooo~~'t~9},~jba, O N~ v O
~ + � a
~--~cP~i~~s ;ao.o.~ N 4-~ '-~I b O
o x o row.[
o ~ N U ~ p
~~p~, ~ ~ ` ~ ~ -
~ � S d � ~i ~~`J~~1 Oai ~u~
� uvi,~~
N A �.~1 O
o M O ~ 3~ .1~
� 3 ~ D b
~ a ~ ~ ~
~ a' ~ ~
, ~ a ~ w o ~
_ ~ . o .o .8 ~ r~ o o w ~ -
w v~ ~n ~
~ o�o b.o� o ro U) N b
~ ~ � CP~-~i ~oo ao~ W U~l tUd b tN0 ~
- � o o ~~co o~ u~o ~ N A ~ tn N
� o~ �~ed�~~~8Q4~9 p� ~ v1 p~ ~
ooooc ~�'Q~"~OOOiO~ a 0 ~ O W
~o oorttb~~oo~?� o~ a) ~ ~ 4I1 O
~ QP ~db ooti o� A(Z ~ N I N
� o = ~ ~ ~ ~�~00~�i~~9 O O ~ ~ N b
O ~o 0 0~~o�'~G o~i W rl 4a
� � oo~ fo00 o o p~ N~~~ t~n
, oo ~ o 0 0~~ o ro~ a N N
� o�~~� ~'~'oo �Q ? o~ .a C~7 3 A ~ ~ _
� o o � � � ~ b� � g rt '1,
0 0 � ~ ~ �'Z. : ~ ' ~ a ~1 ~
- � o 0o c~� o ao
O ~m ~ ~o~ ~ � 'p� i~ ~ ~ W
, ~ p `'lp o~ 0 ~ ~ } ~ ~O ~1 ~ _
_ ~ a~�~, ; ~ ; ~ ~
~ �p ��O~~.o � ~ w ~ U U
0
. ooo.
Q ~a 1 ~ ~ O
150
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APSq. ' ~
A Pw . -
_ 1 ~ ~
� 1
, ~ x__v 8 Z -
� � .
�
. ' ~X ~3
~ ~ ~
. X .
� � �
. � . ~ ~ ~ : . . ~
~ ~ ~ ~ .
~ v ~ e ~ � X -
�
� ~ ~2 ~ �
~ ~ � ~ � ~ ti -
� � ~
� � _ �~~~~~'y~ ~ � � ~ . ~
~ s tiS"w"~': �i~ 1i~N � _ . �
� � M~ � ~
�
~ ti~ ~ ~ 13p7 i ~ � ~ ~ � ~
. t~ . . J~K � �
~N � ~S~' ~i � �
~ ~ !er~~ � � ~ ~N C' � ~ -
C~ ~~s N
~ � .a.,.r':~~ sti � � s ~
~ � ,F f . � :wM ~ � � �
~ i y `-jo ti ~i ~ � _ � . �
� < ~ lp � ~ �
� ~ ~ f~ ~0~~~ � 70~~ � ~ ~
- ~.~ft " ~,i ~ ti .1 ~ ~ � -
� J~~ . q~ _ �
~ ~ ~n~~`~� ~ �hd' ~ ~ ~..V
g~ ~
~ Y !t ~ ~ _
'+1'~':' '.'"~w.�,.~~:~:~ :�1.4.. ~ : : � � ar~~ -.'v
' f~~~ � ' � ~ ~S~-vy'~ ~ -~'1f'
p~ ,y} J~ ,�~j~ ~ ~ ~
r~�~'~V- -
~ x
V~~ ~
x~. y~~ ~
~ ~ 20 " 40 60 ~,rpaAyc
Fiqure 81. Graphs of Dependence of ApSq/APW on the Angle of -
Incidence of the P Wave on the Interface i for
the Regions of the North German Depression:
1--experimental data for PS waves related to all the interfaces _
of the earth's crust; 2 and 3--theoretical curves of Apsq/Apgw =
calculated for different epicentral distances with and without
regard to absorption of P and S waves of the real medium; a--
20�; b-- d= 72�; c-- L~ = 140�
Visible Periods and Frequency Spectra of P and PS Waves
The visible periods� of P and PS waves for earthquakes with different epicentral
distances vary at A~ 1.5� from 0.3 to 1.1 and sometimes to 1.5 seconds at
Q = 160�. The average value of the visible period of P and PS waves on re-
cordings from remote earthquakes (A ~ 10�) is equal to unity. The difference
in the periods of P and PS waves is observed very rarely and mainly for re-
cordings from near earthquakes with low values of ~(up to 1.5-2�).
~ 151
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The frequency spectra of P and PS waves were analyzed by experimental ma-
terials obtained during seismological investigations with standard seismo-
logical apparatus [11, 66, 136] and with the "Zemlya" device. The frequency
spectra of P and PS waves recorded by "Zemlya" stati~ns were determined at
the CDC-3300 processing center installed at Leipzig and at the Sigma-5 pro-
cessing center at Kiev by using the standard programs of these centers. 'I'he
- determination was made for the channel with bandpass of 0.5-10 Hz. Several
- maximums are determined on the amplitude-frequency spectra of P waves (see
Figure 67) from remote earthquakes: the first highest in value at frequencies
less than 0.048 Hz, the second at frequencies of 0.157-0.180 Hz and the third,
minimum in value, at a frequency of 1.025 Hz. The maximum frequency spectra
of P waves from seismological materials with variation of ,L~ from 0 to 140�
- are shifted from frequencies of 5-10 Hz to frequencies of 0.05-0.3 Hz (see
Figure 68, a and b). According to data of "Zemlya" stations, the maximum
frequency spectra for these same values of change from frequencies of
8-10 Hz to frequencies of 0.6-2 Hz. The coincidence of the maximum frequency
spectra of P waves recorded by the "Zemlya" device and by seismological ap-
paratus is observed in the range of A= 0-8�. The maximum frequency spectra
of P waves begin to diverge gradually with a further increase of .,L~ , reaching
the highest value at l.~ = 20-140�. This is related to the difference of the
frequency characteristics of the "Zemlya" device and seismological stations, .
the first of which cut off frequencies below 0.5 Hz. It is interesting to
note that, beginning at Q~.2-4�, the maximum frequency spectra of P waves
cease to vary with an increase of epicentral distance.
The same pattern is observed for S waves as for P waves: the frequencies of
S waves recorded by seismological apparatus are lower than those of S waves
- recorded by the "Zemlya" device. The maximum frequency spectra of PS waves
at d= 2-140� are located at the same frequencies as the maximum ~requency
spectra o� P waves.
- Polarization of PS Waves
Graphs of the displacement of soil particles in the horizontal plane were
� constructed to determine the polarization properties cf PS waves from approx-
imately 15,000 recordings of waves of remote earthquakes for regions of the
North German Depression and the Tashkent Depression.
The graphs of the motion of soil particles in the horizontal plane at one of
the "Zemlya" recording stations for earthquakes with different recording
times T: 1) 2316, 28 Feb 1970; 2) 1700, 3 Mar 1970; 3) 0510, 10 Mar 1970;
4) 1105, 10 Mar 1970; 5) 1303, 14 Mar 1970; 6) 0033, 23 Mar 1970; 7) 0203,
23 Mar 1970; 8) 1227, 23 Mar 1970; 9) 2106, 23 Mar 1970; 10) 1912, 26 Ma;.
1970; 11) 1436, 31 Mar 1970; 12) 1546, 31 Mar 1970; and 13) 0024, 1 A,pr 1970,
are presented in Figure 82.
Seismograms with P and PS waves and graphs of displacement of soil particles -
after the arrival of P5 waves are presented in Figure 83. In all cases the
plots were made for PS waves registered first on the recordings. Analysis
152 _
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,S;VV"- .
- x
y a
x
a~~ ~ ~ ''R~ Y ~ ,
~ X `
a
~ ~ ~ ~ y~ a ~ ~
~ ~ h~,~~ 1 : a, ~ 11~/~.!
� ~'ll x "'a ~ ~S~ ~ , i
- '~y~~2J ~ ,~a~^~~~ -
1 ,14
~
7 Zv 3qrw y
/ ~j`~
/ ~ -
/ _
?iy .~.`y /
~ ~+iy -
0 ~ / ~
6 : . ~ . .
" y
x
_ ~Z ~3 1~1J 4 ~
i~s ~6
Figure 82. Graphs of Displacement of Soil Particles and Shapes
of Recordings of P and PS Waves from Different
Boundaries for Earthquakes Recorded at the Same
- Recording Station:
1-3--graphs of displacement of soil particles and shape of PS
wave recording re~ated to surfaces of Variscian and Caledonian ~
Basements, respectively, and by sections of interference zones; -
4--approach azimuths of P waves to recording station, calculated
by formulas [136] with earthqtYake recording times; 5--shape of
P wave recording on the Z comIaonent and PS wave recording on the
X and Y components; 6 and 7--depth isolines (in km) along sur-
faces of Variscian and Caledonian Basement, respectively
Key: 2, Minutes
1. Hour
of the seismograms, similar to those presented in Figures 83 and 84, and
_ the graphs of displacement of soil particles in the horizontal plane permit
one to note the following principles. If the P5 waves were determined outside -
the interference zone, they had linear polarization both upon exchange at the
- horizons in the sedimentary level and at tlne interfaces in the crystalline
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mass of the crust: the surfaces of the basement and Conrad and Mo horovicic
discontinuities (see Figure 83). If the PS waves were registered in the in-
- terference zone, the polarization of PS waves usually became elliptical ~
(Figure 84, a) or even circular (Figure 84, b). Elliptical polarization is
also observed when the time displacement by the X~nd Y components comprises _
0.05 secor3, i.e., is located within the range of accuracy of taking the
times L1tps_p from the seismograms (see Figure 82). Moreover, clear ellip-
_ tical polarization is observed in the case when a PS wave is recorded on one
component and the low-frequency background is recorded on the other and when
~ waves frequently called P5p and PSg actually formed at different boundaries
of the crust and registered on di�ferent horizontal components of the record--
_ ing, are related to the same boundary. For example, a PS wave with .L1tps_p =
= 2.15 second was recorded on the X component and a PS wave with ~tpg-P =
- = 1.6 second was recorded on the Y component for the same recording stations
on earthquake seismograms with T= 1436 and Q ti76.8� (see Figure 82).
These waves [52J could be related to PSV and PSH waves from the same interface.
At the same time, linearly polarized PS waves with L~,tPS_P = 1.6-1.75 seconds
were determined on earthquake recordings with T equal to 2106, 2316, 2100 and
0203 and 18�, while linearly polarized PS waves with tpg_p = 2;1
seconds were determined on earthquake recordings with T= 1912, 1105 and 1700
with Q~ 50-86�. The wave pattern obtained for all the earthquakes cannot be
explained by the presence of PSV and PSg waves with time delays of 1.75 and
' 2.1 seconds, as was possible in the presence of only a single earthquake re-
cordi.ng at 1436.
The only possible version of explanation in thi.s case which makes it possible
to relate the simultaneously linear and apparent elliptical polarization of
PS waves includes the following. In all cases PS waves with ~.tps_p equal
to 1.6-1.75 and 2.1 seconds are linearly polarized, but are related to differ-
- ent boundaries. These int~rfaces are oriented differently in space. As a
result, PS waves whose polarization planes do not coincide with the vertical
plane passing through the station-epicenter (see Chaper 2) are formed upon
_ approach of the P waves to the interface. In this case deviations of the
azimuth of the polarization plane of PS waves for the upper boundary occur
counterclockwise and those for the lower boundary occur clockwise, as a re-
sult of which PS waves from the upper boundary are recorded on the X component .
and those from the lower boundary are recorded on the Y component. Theoretical
calculations of the deviation of the azimuths of displacement vectors of PS
_ waves from the upper boundary for earthquakes with T= 0510 and 1303 yielded
valiies of 60-70�, which is in good agreement with the given experimental
material. The analyzed example is not the only one. Graphs were constructed _
_ (Figures 35-88) for statistical evaluation and analysis of the dynamic char-
acteristics of PS waves.
Only those seismograms where the PS waves were registered simultaneously on
the Z and Y components were used to plot these graphs. 2'his comprises approx-
. imately 50-60 percent of all the PS wave recordings used to construct the deep
profiles of the crust. The PS waves related to one boundary are recorded
either on the X or on the Y component on the remaininq 40-50 percent of the _
~ 154 -
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~ ~ ~ ~ ~~~~~~r~1~ilu.'~~ ~U~1'~ 1 1 r~~l.'~ ~q~�~ .p1 ~ .
Q ~~rr~, . ; . .
'av .t , ~ ,r..
nr ~ ~ ~I ~I ' ~ '
nv,.v � ' ' ~`Y2 ~ '
~`Ih,:V'~tit a~' I.'~~ ~ iul~~ i
I ~ ~
~I , ~
" � ~ ' -----~.n.,,, N i ~ ~ ~
~ 1~~,dj, v, ~ �,r~, 4 ~ -y y
. ,VS~i I t ~
~ ; ~ I ~ i r
~ ~ I~ ~ ~ I ~ .
'~.i~i~ s ~ I I ~ ~yt ~ , I \
: tlJ~yl x ~ ~ i ~ \
_ . � N') f V " - I ,
, ; ~ Psp~i , ~ ' ~ ~y~l
, ,
. , I i fl~~j, ~
~'k~-tj~"S z , r ~'i I
~'~~:r.K�~t ~ ~~i, ~ ~:1 i �
_ � , P . V ~ ~ ~
_.....,px~,,,
~~~{,~{,~^~�,.~r'�tin^',,."'�~.~
~i-^-'~f`1,d~{'?d,�f~ , '
b M. x .
J'?V~MJ~~ w
=y, .
~,~Vvv~1~. ' -y y
~x
PSnc
^nr,, P.~q ~
^ ~
J 2 ~ .
~ic~',P' `~'~''~.'r{'' ~{,~~t~wl,~
t..~.....~.~-~~n"+~'~"~"~ . ~~L~].=~'7 ~t.. _ _ '
,~w~rrr.', ~.t~. _ ":I...... ' .t...~.. i.... ~ ' i.._
~ ':.,.�A ~ ~ f........~..~ x I
- ' ~ , ,~,/~,,~,,,,,,nr. , .d'
~`vw.n.~ 14 �r , II ' /
� ~
~�r, : : ~ PS oc~ ~ ,1 / ~ � ^ r ~ P ~ ~ .
Ytiy�ti1 ~ ~ A /
�tn(1~~y ~~r,. y ~ r / '
'vvJV ] v
9
~f?. r 1-y ~
,
y;
i~, 'W`~,~
f,H
~ ,
~ ~ f, ~~--------X r ~I I, f~ r
~ ~ ~ ~ ~
~J~:~..l., 7.r^i'^'r V ~ ~ . ~ ~ V ' .
~y4 ~,~~/t h,4�
N ~j~ ~ � -.Z
VJ'J. c~ P~~~v ~ ~IJ I ~ I . / .
`~~'nl`�`Wy~'Ir:rrt',~`~nY~"M~ o, . I I. . . . . . . ~ Z
~
' Figure 83. Seismograms and Graphs of Displacements of Soil Particles
Under Seismographs for PS Waves Registered in the Range
of the First Arrivals and Formed on the Surfaces of t~e
Variscian (a) and Pre-Cambrian (b) Basements and the
M o horovicic Discontinuity (c) :
1--azim+~ths of displacement vect.~rs of P5 waves determined by their.
amplitudes; 2--approach azimuths of P waves from earthquakes calcu-
~ lated by the formulas of [136]
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Q ~ � S
~ ,
r. ~
r
~ ~ i
- r .
PsPZ -y . ~
Y
- i
-s ~
X . .
I �
P~ 2 ~
~
b psPZ PSPR~AFi /
1 ~
_ ~ y
-
i9 2.15 . i ~ ~
y r' i y
Y~ ~ �
1.9 2.15 ~ ~
~ i ~
I ~1
X ~
,
?.9 ~ ~
-x
P ~ ~ ~ ~
?c ~2 ~4 ,
Figure 84. Seismograms and Graphs of Displacement of Soil Particles
Under Seismographs for PS Waves Recorded in the Interfer-
ence Zone:
1--graphs of soil particle displacement from first phases of PS waves
related to surface of the Caledonian basement; 2--approach azimuths
of P waves re,^orded by formulas of [136] to the stations; 3-~inter-
ference zone; 4--section of soil particle displacement from subsequent ~
pi~~ases of PS waves related to surface of the Pre-Cambrian basement
seismograms. This is explained both by the approach of the PS waves only in
the corresponding (X and Y) directions or by deviation of the azimuth of the
displacement vector of PS waves due to the angle of inclination of the inter-
face. The total number of PS waves for each of the boundaries used to
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. . . . . . , . . _ . . . . . . . . . L
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d tPSZ ~c .
75 a Q~
D ~d~
`,a~~.
~
50
.
25
a D~ ~ - ~2
r
~,~~c Q ~ ~ SO d ~
~ 1 . ~ ~I t'As P'
it ~
0 9 ~
s B
~ N Ql` ~ ~ b~ I~;r o~1 ~�I
b o ~ I ~
� ~ ~p y~,~ ~'bb~ F'iiy~~ ~9 i~~i~i~j
ii ~ i
, '�d;~ ~ ~ ~t
S " ~ ~
,b ~
~p0 8 .
Q zs ~0 d t~~ P,C
~
Figure 85. Graphs of Dependence of Recording Times of PS Waves
on X Components tpsX_P on their Recording Times
on the Y companents ptpgy_p (a) and Distribution of
the Number of PS Waves as a Function of the Shift of
Recording Times (Dephasing) on the X and Y components
(b) and Recording Time of /~tpg_p (c):
1--values of ~?tpSX~Y_p and N for PS waves without dephasing on
- the X and Y components; 2--values of ~ tpgY~y_p and N for PS
waves with dephasing on the X and Y components
construct the graphs of Figures 85 and 86 vary from 160 to 400. The following
principle can be tr.aced in Figures 85 and 86. The time shift of recording PS
waves on the X and'~Y components varies from 0 to 0.4 seconds. However, the
majority of PS waves (approximately 96 percent) has shifts on the X and Y
components of + 0.1 second, 4 percent of PS waves have shifts up to + 0.2
~ second and less than 1 percent of PS waves have shifts of +(0.3-04) second.
On the whole the experimental points of the graph of the function ~tPSX-P -
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_ . � dt~. P~y`
a ~ b -
_ 4~ ~ _
p,2 ~ -.a~nr +h, Kci-~ .
~4.. ^ +4
0,1 *rwcw .?+e'
N 900 500 ~+~1,',.~.,~.,.� n.. w -
- , ~ ~ a ,tA'~l7~p as PS-P'~ -
_(1 J a ~Mti#IW!NVIrrt1 ~+ri..
5
"'~+4 M" ~
-0~2 M M a
^7 M
- . 'u" ~ _
_0~~{
- _O's
- Figure 86. Graphs of Dependence of ~ tpsX_psY on the Number ~
of Composite Waves N and L~ tpg-p for Regions of ~
the North German Depression: _
a--curve L~ tpgg-pgY = f(N); b--values of L~ tpgX-pSY =
= f( A tpS_p) for waves related to the interfaces of the earth's
crust in the presence (plateaus) and absence (circles) of their
dephasing on the X and Y channels, respectively
= f(L~ tpgy_p) are grouped (see Figure 85) with standard deviation of + 0.1-
- 0.15 second around a straight line drawn from the origin of the coordinates -
at an angle of 45� and which is the theoretical straight line of this graph
- for linearly polarized PS waves [52,54]. Analysis of the distribution of
shifts equal to 0.2-0.4 second, jointly with geological materials for the
_ rayons of Tashkent, the North Gerir~an and the Azov-Kuban' Depressions, showed
that they are confined to regions of deep faults of the earth's crust.
A graph of the dependence of the ratio of the major axis a of th~ figure (in
some cases of ellipses) to its minor axis b on the time shift between the
components of PS waves registered on the Y. and Y components of the recording -
and the m:mber of waves and also graphs of displacement of the soil particles
_ in tY:e horizontal plane, obtained for PS waves on three stopovers of the -
recording stations is presented in Figure 87. Those waves in which a/b ~ 3
can be taken as linearly polarized waves with re ard to the ~ ~
g possible phase -
shifts by the X and Y components determined by the apparatus (up to 0.05
158
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- U/B
a 20 s
' ~ ---y � -
. ~
~
- ~s -
I I
~ ~o ~
~
~ , o - ~
~ - - - f ~ ~
_ x ~ ~ _ ~ b
. - ~ i -
i - - ~
~ o o ~ x g
-y o 0 0 _ ~ t_+ ~ Z -
I ~O o o~o� + t - - �
o o+ � t ~ '
~
qs o,s i,oec~~,c ,
dtP~ Ps~c x ~S .
SO
o 0
f00 "
. 5
+
aoo+ o~w M
- 15~ Q~ Z QJ o ~+~:#ii.M.~.~.��w.w.�~�+
y- --4 ~ l0 20 N
j N ~
_ Figure 87. Graphs of the Dependenae of Ratios (a/b) on the
Value of Dephasing of PS Waves on the X and Y
Components (a) and the Number N of PS Waves (b)
' Compiled for Regions of the Nortn German Depression:
1 and 2--PS waves determined on the X and Y components and re-
lated to one or different boundaries, respectively; 3--~5 waves -
separated either on the X or on the Y component; 4--nature of
displacement of soil particles in the horizontal plane with di- _
rection of approach azimuth of P waves from earthquakes
second) and a.Zso by the error of dynamic constructions. The number of these _
PS waves for a cry~stalline crust (Figure 87, b) is small, since they are
traced mainly in the region of subsequent arrivals. The graphs a/b = f(N) -
are interesting by their contradictory nature: displacements of the record-
ing times of PS waves by the X and Y components do not exist, while the soil
, 159
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particles describe oscillations close to an'ellipse or even to a circle. -
This phenomenon can be explained by differerit factors, mainly from those by
which the times tps-p of PS waves mainly having 3-5 phases or more were
recorded by the central, least di~torted interference phase while the graphs
of.::he motion of soil particles were constructed by the phases nf PS waves
distorted by superposition of adjacent oscillations.
The dependence of the angle of polarization S on the values of L~.tpS-P for
regions of the North German Depression are presented in Figure 88. As can
be seen from Figure 8S, the value of s varies from 0 to 360� regardless of -
the value 4.tpg_p. A similar curve from [52] is plotted in Figure 88. The _
, small number of data from which this curve is constructed (30-40 determina-
tions) permits one to assume that its nature is random.
The data obtained in Figures 82-88 permit one to assume that polarization of
PS waves related to the interfaces of the earth's crust is linear or ellip-
tical with time signals on the X and Y components no greater than + 0.1 sec-
ond and rarely, + 0.2 second. An exception is fault zones where the values
of the time shifts of PS waves on the X and Y components may reach 0.3-
0.4 second. -
It was determined for PS waves with time shifts on the X and Y components
up to 0.1-0.2 second that their approach azimuths to thQ recording stations,
aetermined by the amplitudes of PS waves and formulas used in seismology for
horizontally layered media [136], do not coincide with each other. Graphs _
(Figure 89) were constructed for statistical analysis of the values of these
deviations Qo( and to determine their dependence on p( and the number N of
" recorded PS waves. As can be seen from 89, a, L~oC does not depend on oC .
- The nature of the graphs ~C1oC = f(N) themselves was rather unique (Figure 89,
b). It is identical for interfaces of the crystalline mass of the earth's
crust. A maximum number of PS waves is noted at ~o( = 0. The number of PS
waves decreases to zero with an increase of /~p( from 0 to 100�. Additional
maximum numbers of PS waves are observed on a background of a gradual decrease
~ of N at specific values of Qo( . The graph A 0( = f(N) is seemingly subor-
dinate to normal distribution law of /ao( with maximum at o( = 0. On the
whole, these distributions of the data of /~p( indicate that PS waves are
polarized in the plane of the ray (PSp) although significant deviations of
the polarization plane of PSp waves from the vertical plane passing through
- tl:e recording station-epicenter are also observed. Maximum values near
+ 90� should have been observed in Figure 88 with the presence of pSH waves.
The values of the phase shifts of PS waves register on the X and Y components -
and the ratios of their displacement vectors for these same components of
composite PS waves with horizontal and sloping interface were compared to
determine the degree of similarity of the theoretical and experimental data
on the polarization characteristics of PS waves.
Comparison of the values of ~tpgX=pgY showed that the theoretical and ex-
perimental data are in good agreement with ~ach other: the values of
tpgg-pgy for platform conditions (CQ ~ 10�) do not exceed + 0.15 second
in both cases.
- 160
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a b � -
100 Z00 300 ~:~paAyc
Na
~T~ 5 0 D _
0~ ~ � �
M
�
N ~
� � �
t ~
1 ~ ~M
. � ~ . .
j �
MY � � = M f f � _ � �
_ ~w'~ ~ : � ~ .
z u ' _
, ~
. Y � .
. � . � � ~ . .
.o. . ,f . .
i : : ~ :
- L ;g...
3 . . tit':. . .
.
~ r. . .
� .
. ~
~ � �
. . r
~ � " f t �
4 � ~ � � r�. -
�~N~~~ ~ � M -
~ ' J j ~
�
~f~~ ~ � � -
~p~. ~ ~ � . � ti
.
5 Ziti .
~ . :s~.
. ~ ~ ~
~s . . . � � -
o .
~ ~ ~ M ~ ~ � j
~ � � -
dtPS_P,C
~Z
Figure 88. Graphs of Dependence of Polarization Angle ~ of
PS Waves on L1 tpS-P and Their Distribution on
the Number N a' from Regions of the North German
Depression: ~
1--experimental data for approximately 600 earthquakes; 2--
- curve from [52] _
The experimental values af the ratios of the displacement vectors of PS
waves registered on the X and Y compon~nts (see Figure 21) are included
among the theoretical curves of UpgY/UpgX for interfaces with anqles of -
inclination from 0 to 20� and L~. = 20�.
The derived theoretical and experimental data on the polarization character-
- istics of PS waves make it possible to explain a number of phenomena observed
during registration of them on recordings from remote earthquakes. The first
phenomenon includes the �act that PS waves from different boundaries are
registered on different horizontal components of the recording. This char-
acteristic was explained [52] by the anisotropy of the medium which
161
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~ -
~d
~
m
. G ~ U ~ ~
. ~ 1~i ~ ~ rt ~
i
W 3-1 N ~
N �
_ jl ~ ~~a
LJ o b o
- ~ a~i ~ � ~
^ a ~ a~
_ a ~
~
ro a~i
A V A t~~t
? �~-I O
2 ~
O
T ~ N ~ ~
~ �ri �rl N -
d � ~N ~iQ~~ O b fI) ~ ~
~o v g � ~ P o " ~ N~
~ i
g ~ -
~ 4 ~ ~ ~ a~
o�p dPo ai ~o~�a�~o o~ o0 0 � ~ o r-I ~
oo~o r~?o aooG~b ~ c o a N~
~ ~ o0 o N U
~ ~ . � Op p � . .Q.~ p � ~ ~ 'N ~ -
O~ Q~p ~ O O ~ W~ II?Ir~~~ i~ ~ ~ O O~1 ~ fO
� ~ � � ~ ~tll N i~ N
_ o o�~'~' . . � ~ ~ N N ~-~1 A -
c
~ro ~ N ~ ~ ~
. . . ~a � p, A ~ aNi w
o
. d�ao 0 oc~~b ,'b eo,p �o ' o o a� A t~d 2S t~d � r
� � O~ ~ ~O ~ ~ a M ~Q~ ~A ~ ~ P � � N N
p ~ � ~ � ~ � ~ ~ o a~ a � � . ~ ~ e--I a 4-I
00 b O ON O ~ 00 O N ~ ~
. .
O~bp .i'~' ~ H S~ U]
~ ~ ~o ; . o ~ ~
~ . o a
~ � p . f o � 4d 0..~ ~~o o ~ f"~ ~ ~ N
o ~ . . o � ~ ~ ~ 1 .C
~�~�w b b ~ b c~ a~
~ o o �4.~00 ..o . 3 ~
~ p o o o a�'o w.~ ~
a o h , ~ ~ ~u
~ ~ 4~~1 G~1 N
1 rt1 ~
W ~ A U
~ 162
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determines the presence of PSV and PSg waves. However, as the study pre-
sented above showed, this fact can be regarded linked to the deviation of
polarization planes of PSV waves formed at the interfaces of the earth's
crust with different spatial position in different directions. The second
phenomenon observed on recordings of PS waves from earthquakes includes
the fact that in some cases the PS waves, judqing by the very typical
shape of the recording, have polarity distinguished from that which should
be observed at a given azimuth determined by formulas [136] (Figure 90).
Construction of the motion trajectories of soil partYCles in the horizontal
plane for PS waves shows in these cases that the azimuths of the displace-
ment vectors of PS waves are located in a different quadrant that the ap-
- proach azimuth of P waves and accordingly of PS waves, determined by the
formulas of [136]. Hence, it foll~ws that the polarity of the PS wave
arrival can be distinguished from that of the P wave arrival and does not
ccrrespond to the traditional sei~mological distribution of the polarity
of arrivals of P wave components by quadrants.* It is more correct in _
these cases to determine the quadrant from which the PS wave came, con-
structing the graph of soil particle motion in the horizontal plane. Strict
consideration of the motion trajectories of soil particles and the polarity
of PS wave arrivals affects to a significant degree the results of inter-
pretation. Specifically, it may be that composite waves determined with a
time shift on the X and Y components and related either to a single boun-
dary (PSV and PSg) or to different boundaries, may be the camponents of a
- single wave without phase shifts upon variation of the polarity of one of
~ the components.
The Nature of PS Waves of Different Groups and the Criteria~for Separating
Them on Recordings
The following groups of PS and P waves may exist on recordings from earth-
quakes at Q= 5-180� and T= 0-11 seconds after the arrival of P waves:
a) PS waves passing horizontal or near-horizontal (~Q ~ 10�) interfaces of
the earth's crust; b) PS waves passing through sloping (~Q = 10-80�)
interfaces of the earth's crust; c) lateral PS waves--transient refracted
and transient diffracted; d) the horizontal components of P waves; e) in-
complete (under some special conditions) P and PS waves in the sedimentary -
mantle.
= Separation of PS waves into these groups by the shape of their recording
and by the frequency spectrum is essentially impossible at the modern level
of development of studies. The most optimum approach may apparently by
separation of PS waves into groups according to the aggregate of their
kinematic and dynamic characteristics.
PS waves which pass through the horizontal interfaces of the crust may be _
distinguished among the surroundinq PS waves by the following features.
- *
- Deviation of polarity from the traditional may also be caused by exchange
of P and S waves on the top of the waveguide.
- 163
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~
- .nnn~v~~. -^~-~?~,..~vw~:'1rn,ti, ~~/~!v\~ti~
~r'~'~r+~ 1..; ~y~ ~ ~
v YY11~/
. 4 ~M/~'~~/~! "1' �
~
� PS PR ~ AR
' n~~~n ~i
w~-~w
. l'~~, ,
J r~
~ �~y1 1
~ /"~/~/~/'J 7 J V
~ PSpR+AR
^?'?~n '^vJ_^L._.~.,~,n_. ^ ~ ~n ~ ~n
~ ~ ! V~'~~~N l~`~ ~ V V ~ ' ~N
:/~nnn 'x ~"W~~,'L'~f~,_
- ~ ~
- . wttiv-""" V ~M .
r. ~,l,/~/V~ -j l~`~""~ ,
,/W~ 1 3
-e P
1C W"W'W"~~~u~vf1rf"I~J' .
Figure 90. Seismogram with Clear lteverse Polarity of PS
Wave on Y Component for Region of North German
Depression: -
T= 0229, 27 Jun 1969, Q= 76.3� and DC = 34.3�
1. ~1~Y1@ azimuth of the PS wave displacement vector (the major axis of an
_ ellipse or a straight line) should coincide with the approach azimuths of
P waves from earthquakes calculated by the formulas of [136]. According
to theoretical calculations, the errors in determining the azimuths of the
displacement vectors by their amplitudes with dynamic calibration error of
10-15� should not exceed + 6� at any approach azimuths.
2. The angle of emergence of the seismic radiation of PS waves coincides
with the theoretical angle calculated for a horizontally layered profile
under the recording station.
3. The delay times of PS waves with respect to P waves from earthquaices
with different approach azimuths, are registered by a single recording sta-
tion and corresponding to the same interface of the crust up to the M dis-
continuity, should not have a spread of more than + 0.1-0.15 second (if
this is not a fault zone). As a result of this, clear maximums correspond- _
ing to tne main interfaces of the earth's crust are determined on the sta-
tistical time profiles Qtpg_p = f(N). PS waves related to different inter-
faces of the earth's crust are easily separated in time between each other
tpS-P on time profiles L~ tpg-p = f(R).
PS waves passing through sloping interfaces can be separated by the follow-
ing features.
' 164
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1. The azimuths of the PS wave displacement vectors (t~e major axis of an
_ ellipse or a straiqht line) us~ually do not coincide with the approach azi-
muth of P waves from an earthquake calculated by the formulas of [136].
The discrepancies should be greater than 6 percent with dynamic channel
calibration error of + 10-15 percent. � _
- 2. The angle of emergence of seismic radiation may not coincide with the
angle of emergence calculated for a horizontally layered profile under the
recording station. `
3. The delay times of PS waves with respect to P waves, corresponding to
� the same interface at a single recording station, from earthnuakes with
different approach azimuths yield a spread of 10 to 100 percent or more.
As a result, the maximums on the statistical time profiles are indistinct
or white noise is observed instead of them for all the interfaces of the
crust with sufficiently large number of earthquake recordings with different
approach azimuths and with an increase of Otps_p (Figure 91).
- ~ ~ 20 N
- 2 _
4 -
6
8
10
_ - `
_ dtPS P,C ~2m3~4
Figure 91. Statistical Time Profile of the Crust of a Mountainous ;
- Region Compared to Theoretical Times tpS_p for _
Transient and Lateral PS Waves: ~
1--time profile; intervals of Atps-P; 2--for PS waves formed
on sloping interfaces of the earth's crust; 3--for transient dif- -
fracted PS waves; 4--for transient reflected PS waves
Lateral PS waves are distinguished from transient PS waves by the following
features.
165 ~
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1. The cophasality axes on correlation seismograms with location of the
profi].e transverse to the disturbance or contact have smaller values of
vk than the vk of transient PS waves and intersect all the remaining axes -
_ (see Figure 62, a and b). 7."he time profiles Q,tps_p for these same waves
intersect all the time profiles compiled for P waves for horizontal inter-
faces at large angles of inclination.
2. 2'he angles of emergence of seismic radiation determined by PS waves -
_ differ from similar anqles for PS waves calculated for a horizontally
layered structure of the crust under the recording station.
3. The azimuths of the PS wave displacement vectors may differ from the
approach azimuths of P waves to the recording stations, determined by the
forr,iulas of [136] for any values .
The horizontal components of P waves are distinguished among PS waves by
the angles of emerqence of seismic radiation e. In this case the waves
registered on the horizontal component of the recording are initially
assumed to be composite waves and then components of P waves. In the case
of recording PS waves on the X and Y components, angle e is determined by
- the formula (Figure 92).
e = arctg Aps$ . -
`4P92
In the case of recording P waves on the Z, X and Y components, angle e is _
determined by the formula (see Figure 92j.
e = azctg A pZ ~ . -
Pg
Thus, for example, the following data were found for the regions of the
Pre-Caspian Depression and for Tashkent. Based on the assumption that the
waves on the X and Y components can be either horizontal components of P -
waves or PS waves, angles of e equal to 10-15 and 60-80�, respectively, were
found. The theoretically calculated angles of e for PS waves registered on
the X and Y components in these regions were equal to 70-80�. This made it
possible to relate most experimental waves recorded on the X and Y components
in these regions to composite PS waves.
Multiple waves approaching the earth's surface as P waves are determined
on the recordings as the horizontal components of these waves (according to
- angle e). Complete and incomplete PS waves, if they exist, can be separated
from single P waves by the following features.
- l. A wave is assumed single if no other waves of any kind are noted on re-
cordings of all registered earthquakes with similar values of earlier than -
this PS wave on the horizontal component (see Figure 83, c).
- 16G
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a 1 ~Iipurracnu~c
aA , ~r~Qy~ �tTawKeNm
e,rpa~yc ~ ) 8naa~Na
90 ~ 90
gp _ 80~ .~t
70 ~ 70 ' t
. ~
60 A 60 � ?
SO ~ SO �
~ 10 ?0 d0 k0 SO * 70 �90 100 d; pa,qyc + 25 SO ~ 75 d,rpepyC
~ $ yp
10 . ~ 10 =
0 ~t ~
a ~ a? ~3 ~4 ~5 _
b B01itib ~P BOAH
5 ~P$ '
APx y APSx, e '
i e A � PS~
~ Pz ~-e ~ _
~ ~
Figure 92. Graphs of Dependence of e on Q(a) and Diagram of
Ray Path of PS and P Waves in the Plane of the Ray
Used When Determining Angle e(b):
1--angles e determined by the ratios of the P wave amplitude com- ~
ponents (ApZ/ApX); 2--angles e determined by the waves registered
on the X and Y components of the recording, assuming they are com-
posite waves; 3--angles e determined by the waves registered on
the X and Y components, assuming that they are components of P
waves; 4--the curve e= f(L, ) according to S. D: Kogan at hoch =
= 700 km; 5--the curve e= f( Q) according to S. D. Kogan at
hoch = ~
,
Key: '
1. Degree 4. P waves
2. Pre-Caspian Depression 5. PS waves _
3. Tashkent
- 2. All ~the determined PS waves may be asstuned single in regions with the
absence of a broken sedimentary layer. This is based on the fact that the
layer in which the occurrence of intensive multiple wav~s is ,possible is
absent. Waves multipla in the crystalline layers of the crust, as was demon- ~
strated above, even without regard to the absorbing properties of the medium,
~ have extremely low intensity and are actually not distinguished on the
recordings.
167
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3. The nonconformity of the delay times ,L~tps_p of subsequent PS waves to
the theoretical times of existence of multiple waves for the region of the -
investigation. -
A specific dependence between the recarding time on the horizontal components
of recording the first composite PS wave and epicentral distance was observed
in many regions during work with "Zemlya" stations (Figure 93). Waves related
to the deeper interfaces of the earth's crust are registered first.on the .
recording of horizontal components with an increase of . Thus, waves re-
lated to the Conrad or Mohorovicic discontinuity and having a value of
tpg_p = 3-5 seconds (see Figure 93) were registered first on recordings in
many regions at L~ = 140-160�. The dependence of 4 tpS_p of these waves
on was explained by means of theoretical calculations of the intensities
of the first PS waves on the X and Y components. Theoretical calculations
were made for one a~ the models of the media of the North German Depression
at absorption coefficients of a p= 2 aCS. The overall nature of the theo-
retical and experimental graphs is in good agreement. These data and also
analysis of the experimental material of five regions permit one to assume
that multiple PS waves are either absent on the recordings or their intensity
is so small that they cannot have a significant effect on the wave pattern _
created by remote earthquakes in the initial part of the seismogram recording.
This conclusion is similar to that with respect to multiple waves during GSZ
[75J � -
dt~~,c
4 ` ~ /
/ s~ �
: p~/'
w ~ ~~i -r J=-TT ~
Z � . _t ~ ~ �
. �
- _ ~ .
, .
.
x
~ ZO 40 60 Bll 100 120 ~40 d.rpa,qyc -
� � 1 ~2 ~3 ~4 ~S ~6 ~7 ~8 ~9 -
Figure 93. Graphs of Dependence of Arrival Times L~tps_p of
First PS Waves on Recordings of the X and Y Com- ~
. ponents on L1 :
1--Azov-Kuban' Depression; 2--Pre-Caspian Depression; 3--Rayons
of Tashkent; 4--North German Depression; 5-8--averaging c~ves
for the Azov-Kuban', Pre-Caspian and North German Depressions
and rayons of Tashkent, respectively; 9--theoretical curves for
model of the crust of the North German Depression presented in
Figure 3.
168 -
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Proof of the absence of multiple PS waves may be the presence of clear maxi-
mums on the curves L1.tpS-p = f(N) and Aps = f(N) plotted for different plat-
form regions [113] and their persistence on large areas. Moreover, the
times 4tpg-p of the first PS waves registered at large values of L~ on
the recordings of horizontal components correspond well to the maximum waves
AtPS-P = f(N). The persistence of the graphs ,~tps-p = f(N) within indi-
vidual regions and even upon transition from region to region cannot occur
in the presence of multiple PS waves on the recordings. The absence of in-
tensive multiple waves on recordings from earthquakes and rheir existence on
MOV seisn:ograms from explosions are determined by the presence of P, S and
PS waves dt the angles of incidence to the interfaces and possibly at the
frequencies from these two different types of seismic sources. Wh~rea.s the
angles of incidence to the upper horizons of the sedimentary mantle do not
exceed 2-8� for PS waves reom remote earthquakes, they are close to 45� for
reflected waves in the regions of their initial points. As a result, the
product of the reflection coefficients for multiple PS waves fro~m earthquakes
rapidly approaches zero and this product hardly differs from unity for P
and S waves from explosions since the angle of incidence of the ray is 5imi-
lar to the critical angle in this case. Thus, the reflection coefficient of
S waves will be approximately equal to 0.3 for the first layer of the model
of the crust presented in Figure 3. The product of the reflection coefficients
will be equal to 0.09 for a multiply reflected PSSS wave in the first layer
and it will be equal to 0.0081 for a triply reflected PSSSSS wave.
_ 169
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METHOD OF INTERPRETING TRANSIENT COMPOSITE PS WAVES ON RECORDINGS FRON NEAR
AND REMOTE EARTH~UAKES
Moscow SEYSMICHESKIYE ISSLEDOVANIYA S APPARATUROY "ZEMLYA" in Russian
1977 signed to press 31 Jan 1977 pp 160-183
[Chapter 7 from the book "Seysmicheskiye issledovaniya s apparaturoy
- 'Zemlya"'by I. V. Pomerantseva and A. N. Mozzhenko, Izdatel'stvo Nedra,
1,400 copies, 256 pages]
[Text] The method of interpreting PS waves on recordings from near and
remote earthquakes includes separation and correlation of P and PS waves,
- construction of the time profile, determination of the velocity parameters
of the meditun required to transform the time profile to a depth profile,
- stratification of the time profiles by deep drilling data and explosions,
calculation of the depths to interfaces and seismic deflections, construc-
tion of depth charts and profiles and analysis of their accuracy. Analysis
of wave fields, methods of calculating depths, seismic deflection and con-
struction of depth pr.ofiles differ somewhat from each other for regions
with subhorizontal (i~ ~ 10�) and subvertical ~ 10�) interfaces.
'i Compilation of Time Profiles
. Time profiles are compiled for the purpose of statistical accumulation of
material from different earthqu~ikes. They are the difference of arrival
times of PS and P waves L1 tpg_p to the recording stations along the pro-
file lines (F'igure 94) or concentrated in one place. In the first case the
distances between the recording stations R is plotted along the horizontal
and in the second case the number of distinguished composite waves N. Direct
accumulation of recordings from earthquakes at the observation points is
' impossible without preliminary conversion of signals due to the significant
difference in the shape of the P and PS wave recordings from different
earthquakes.
9 The value of A tpg-p 3epends, according to formulas (2.5) and (2.7) on the
angle of incidence of the P wave downward to the interface i, which in turn
is determined by Q. With large differences in Q, , the times ,LS.tps_p,
especially for deep interfaces of the crust, may differ significantly from
each other. Thus, ~or the Mohorovicic Discontinuity, if tpS-P = 6 seconds
at = 70-140�, then ~,tps_p N 7 seconds at A= 3-5�. This
170
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- circumstance forces one to construct the time profiles of the earth's crust
from near = 3-5�) and remote (A = 10-160�) earthquakes separately or
to introduce the corresponding correctior~s following from formulas (2.5)
and~l(2.7) into the values of A tpS-P of near earthquakes.
- Formulas for Determining Depths to the Interfaces H of Seismic Deflections
{L), P,pproach Azimuths (p~ Epicentral Distances ( L~) and Angles of
Etnergence of Seismic Radiation (e) for Horizontally Layered Media
Analysis of the formulas A tPS-P = f(H , ip2, v), derived for horizontally
layered media, showed ithat they may also be used with permissible errors~
for slightly sloping interfaces at 10� and Q~ 2 G� ~d at ~Q L 20
and A > 70�.
, The depth ( along the vertical) to th,e interface for a two-layered medium at
L~ = 0-140� is determined by the formula.* _
Otpg_p~p~~, (7.1) ~
~i - K~pCOS igl-COS tpl ~ -
Seismic deflections arr~determined by the form~xlas
Lg =Hl tg isi, (7. 2 )
- Lp = H~tg ip~�
At ~,5 10�, formula (7.1) can be reduced to a Hasegawa formula (see
Chapter 2)
. AtpQ _ p~ P~P
~j1= ~ 3~
(gcn-1) {1-~- Z~p sina i
2'}
or after slight transformations
*
*For the first layer in a two-layered medium, the values of vpl and K1 are
equal to the mean velocity vpgR and to the mean value of KgR, respectively, _
to the interface. Therefore, let us use vpgR and KSR instead of vp1 and
- K1 everywhere in the formulas. -
- 171
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A tpS _ pUp~D ~ 4~
H1= i_-..
y (K~p-1) i!-}- LK~p cos? epl~ .
l
- Seismic deflection at Q~ 10� is determined by the same formulas (7.2). r
_ The values of p( and ~ are determined by the following formulas [136]:
~os o- ~~S a,P S~n e S~n ee cos 6 cos 8~;
sin a= sin 1~P sin Oe. ~ � _
sin 0
(7.5)
cosa- ~~ss~-~ose~o9~, ~
~;n e S~n n .
where 8 is the complez~entary angle to the station latitude (90� - ~f 8 e ~
is the comp~ementary angle to the epicenter latitude (90� e); e? is the
epicentral distance, ~ is the azimuth to the epicenter, ~ p is the differ-
ence of station and epicenter longitudes e), [P is the latitude of
_ the recording station and ~ e is the latitude of the epicentex.
The error of calculating and on a compufer by formulas (7.5) com-
prises + 0. Ol An error in deternu.nation of ' L~ and o( of +(1-2 is -
- frequently permissible in practice. A Vul'f;,grid [136] is used in this case.
Angle epl is determine.d by recalculation of'angles eK = f(,Q ) presented in
[64~ by the for~mula -
- v "
cos eP1= U`p cos eH, ~
� x (7.6)
where vK and eK are the velocity and angle of emergence of the seismic radia-
tion for the earth with average parameters [64].
~anstruction of Depth Charts and.Profiles for Horizontally Layered Media
When working with',the '�Zemlya" device, unlike other seismic methods of in-
- vestigating the earth's crvst (GSZ, KMPV and MOV),,depth charts are initially
constructed, from which depth profiles are then cumpiled. This,anique produc-
tion of resulting materials is determined by the approach of wa~~es from earth-
quakes from different directions to the recording stations, as a result of
which the derived data indicate the structure of the boundary in space rather
- than in the plane of the profile. To convert a three-dimensional image to a
- two-dimensional image (in profile), its image is constructed on a chart and
then on the profile.
The entire process of ccnstructing depth charts and profiles include the
following steps.
~ 172
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\
~ S� � ~ i ~I ~ ~ _
.
.
~ ~ ~~1~
+
. . ~ \kl.b+ , ~ -
~itt ~ I \
t+,b~, * I \ ,
~ D
_ I� fi~' ~
~ ~ ~ I~ '
= 8$ I
: :
- ti~.. ~
_ . y ; o _
y . ; -
. ` \ \ x
~ ~ -
N . \ ~ ~ � . . ~ ( a
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~ i l I~
w : ~ ~ � ~ I
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S~ ~ . ~,~Y ~ ~e ~
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xxx ~ ~t I
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[Caption for Figure 94 on following paqe]
173 -
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173 a
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- 1. Selection of the velocity parameters of the medium and calculation of
the curves vpsr = f(H) and ICsr = f(H) under each recording station or for
- individual regions of investigation necessary to convert the time profile to
a depth profile. _
2. Calculation of the theoretical values of ~ tpg_p using the derived curves
~Psr - f(H) and Ksr = f(H). ~
3. Construction of graph paper of Q tps-p and determination from them of
depths H1, mean velocities vpsr and mean values of Ksr to the interfaces.
4. Determination of seismic deflections by P and S waves.
5. Construction of depth charts and profiles.
The velocity parameters of the medium vpsr = f(H) and ICSr = f(H) are selected :
either for each recording station or for a series of them with an error of not
more than + 5-10 percent. The curves vpsr = f(H) are compiled from seismic
_ logging, MOV and ICNI~'V data, special and inci.dental explosions and from near
- earthquakes registered by the "Zemlya" device. Seismic logging and MOV data
are used as the initial materials for compilation of the curve vpgR = f(H) to ~
construct the surface of the arystalline base with high accuracy, especially '
- at shallow depths of deposition (from 0.7 to 2 km). Data on coefficient K -
are usually absent in the region of the investigation. They are calculated
by using S wave recordings from explosions and earthquakes registezad by the
"Zemlya" device. Methods of calculatinu vpsr = f(H) and Ksr = f(H) are pre-
sented in Chapter 9.
The theoretical values of ptpg-p are calculated by formula (7.4). The
~ values of vpSr and Ksr are calculated for each recording station with strongly
variable seismological conditions by area. They are calculated for a series
of stations in regions of graclual variation of. these parameters. The values
of Atps-p are accordingly calculated for each station or series of stations.
The value of ~.tpg-p is calculated on a computer for a series of stations.
Special graph paper is compiled if necessary to calct~late L~tpg-p for each .
recording station.
The value of ,L~ tpg-p is calculated by a computer program in two steps. The
value of H is first determined by the simplified Hasegawa formula H=
= vPsr 0 tPS-P/(Ksr - 1) in the presence of curves vpsr = f(H) and I~r = f(H) i
and the derived values of H are then refined by formu.la (7.4) by introduction
of angle epl. The theoretical values of Atps-P = f~H],, Ksr, vPsr and epl) -
are derived as a result of calculates for the given curves vpsr = f(H) and
,
Ksr = f (H) � -
Theoretical graph papers can be calculated on the computer or by hand. They
_ pern~it or~e to take into account with far fewer volumes of calculations all the
~
possible variants of curves vpsr = f(H) and Ksr = f(H) compiled for each re-
cording station. Theoretical graph papers (Figure 95) consist of three series ~
_
~ 174
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~
.c
. , , , ~ , . . . . . . ,i~
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of the following curves: a) vpsr = f(H); b) ICsr = f(H); and c) ~ tps_p =
= f(H) at different values of eK. Specifically, for reg~ons of the North
~ German Depression, the values of eK dependent on L~ of the earthquaices
- registered here were selected as equal to 55, 65 and 82�, which correspond
approximately to the values of L~ equal to 18, 76 and 140�. The curves
_ Q tpg_p = f(H1) and the corresponding curves vpsr = f(H1) are denoted by
identical numbers. One theoretical graph paper corresponds to one interface.
Since the curves Q tps-p = f(H1? ~psr~ Ksr and eK are calculated by formula
(7.4) which includes cos epl, dependent an vpsr according to (7,6), when it
is considered for each boundary and station, the corresponding number of
graph papers would have to be constructed. With a large number of observations ~
(this comprised 650 points in the North German Depression), these constructions
bec~me unfeasible. To reduce the number of graph papers and to reduce them to
a single paper for each interface, the values of cos epl, different for each _
recording station and each earthquake, were replaced by the average value of
cos epl corresponding, according to (7.6) to the mean value vpsr to each
interface of the entire region. The effect of vpsr on the value of cos epl
was first analyzed prior to this substitution. It turned out that even for =
a surface of the Caledonian Basement (the North German Depression), where
the greatest variation of vpsr was observed (from 3.2 to 4.1 km/s), the use
of the averaged value of vpsr = 3.7 km/s leads to errors in determination of
_ angle epl from 12 to 4� and ,L1tpg-p = 0.005-O.Ol second, which is within ~
the bounds of accuracy of reading the times L~tpg_p from the seismograms. -
For the.remaining interfaces of the crust, replacement of interval vpsr'by -
the mean value vpsr leads to even smaller errors in determination of ~ tp~-p~ ~
The method of construction and use of graph papers includes the following. -
The values of vOPsrr KOsr and Hpl at any boundary in the sedimentary mantle,
below which the values of vpppo and Kppl are known to us, are initially de- _
termined for all recording stazions by the curves vpsr = f(H) and i~r = f(H).
For the derived values of vppsr~ KOsr and Hpl at the boundary in the sedimen-
tary mantle to depths somewhat greater (by apprnximately 5 km) than the depth
to the next determined interface calculated approximately by L1 tpg-p, the
curves vpSr = f(H) and ICsr = f(H) are calculated by the formulas
U Hoi-f-DH ( 7 . 7 )
p~P aH '
t0i -
. �OPnn
where Fip~ is the depth to the boundary in the sedimentary mantle, Tpl is the
travel time of the P wave along the v~rtical to this boundary, H is the
- increment of depth under the boundary in the sedimentary mantle and vpp~l is
the stratal velocity under the boundary in sedimentary deposits.
The following is then calculated
.175 `
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a ~ b c '
3 4 v~~CM/c ~,9 1.IK~P/2 1,2 !,2 I,1 12 1,2 I,2 1,2 l,2 1,2 1,2 dt _,C
~
4 4 ~i U~
~2 Cu
5 S S
6 6 6
~ 1 y ~ 7
2 8
3 g
8 ,10 8 8 -
5 � '
9 g y y eK ~o
65
1 , A7 10 55
11 11 11
- ' \
~ I ~ 12 12
H KM H,KM H~KM 1 2 3 4 S 6 7 8 9. 10 ~l
Figure 95. Theoretical Graphs For Determ.ination of Depth to
Surface of Varisican Basement for Regions of the -
Nort~i German Depression: ,
a--curves of inean velocities; b--curves I~r = f(H) for the upper
part of the crust; c--strictly theoretical graphs of LL tpg-P = :
= f(H1. ~pf~ ~r and eK) calculated for each curve of graph a.
AN
Ko cp L.a
01 Ko nn voP
~p nn ~ ~7.8)
K~a = Ha + AH
i'OP~p ~OP~p -
where KpSr and vppsr are the mean value of K and the velQCity of the longi-
tudinal waves to the boundary in the sedimentary mantle and Kpp1 is the
stratal value of K under the interface in the sedimentary mantle. ~
The set of curves A tpg_p is calculated simultaneously with curves ~psr
- = f(H) and Ksr = f~:?). The values of H1, vpsr and I~r to the first interface
are then determined by the experimental values of L~tpg_p and epl from the
graphs of Figure 95, c. The depth charts are constructed by the values of
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H1 and deflections L, by which the depth profile is compiled. The values
of vpSr and Ksr are determined to find the values of H1 under each recording
station on the depth profile, beginning from which the curves vpsr = f(H)
and Ksr = f(H) and ~tps_p are calculated for the next, deeper.interface.
The entire process of calculating the graphs and determining the values of
H, vpsr and Ksr from them is then repeated. With complex tectonics of the
sedimentary mantle (of the salt-dome type), the value of H1 must be determined
with regard to the deflection and approach azimuth of the waves from earth-
quakes at the corresponding distance and azimuth from the recording station
rather than under the recording station.
Seismic deflections by P and S waves are determined either directly by formulas
(7.2) or in the presence of extensive experimental material with strongly vari- -
able seismological conditions--by graphs (Figure 96). As can be seen from
formula (7�2), the tangents of angles ipl and ipgl are considerably dependent
on the velocities of the P and S waves in the first medium. On the whole, the
extent of deflection depends on H1 and on tgipl and tgigl. Therefore, formula
(7.2) can be divided into two parts, each of which can be depicted in the form
of a graph. Graph II (see Figure 96) is the graph of the dependence of tgipl -
and tgigl on vpsr in the covering medium for angles eK from 50 to 83�. Graph I
is the graph of the dependence of tgipl and tgigl on.Hl. Both graphs have a
common scale of tgipl and tgigl. The values of tgipl and tgigl are determined
by a single tangent scale, but with different scales of vpsr. The tangent of
angle ipl is determined by means of the external scale and the tangent of iSl
is determined by the internal scale. 7.'he process of determining Lp and Lg
includes the following. By knowing the value of vpsr to the point of exchange
and eK, the graph tgipl and tgigl on the right side is determined. The point -
- with the given tangent and depth H1 to the interface is ttien determined along -
the corresponding tangent curve. The extent of deflection for this point is
taken from the scale LR,LS (Figure 96, I). The described sequence of determ-
ining deflections Lp and LS is shown in Figure 96 by the dashed lines.
]:f one proceeds strictly from derivation of formula (7.4), the depth to the
- interface should be plotted on the charts or diagrams on the approach azimuths
of P waves to the recording station in the range of distances from the record-
ing station to the point of separation of the P wave from the interface, i.e.,
in the range of seismic deflection of the P wave. The values of deflections
depend significantly on the depth of deposition of the boundary. If the de- -
flections do not exceed 100-200 m for the surface of a basement at deposition -
depth of 5 km, they may reach 10 km (Q 60-70�) for the M discontinuity at
a depth of 33 km. Therefore, it is more feasible, especially with regard to
the dynamic proper~ies of P and S waves determined in the region of their
separation from the interface, to plot the depth on the section between the
points of separation of the P and S waves from the interface rather than on -
_ the entire length of deflection of the P waves. This section will be a point
for shallow-lying boundaries and will be a line measuring 3-5 km for deeply
lying boundaries. Thus, the depths to the interfaces are related to the point
located on the approach azimuth uf P waves to the recording stations at distance
(Lp + Lg)/2 from it when constructing depth charts by the interfaces af the
earth's crust for theupper boundaries (from the surface of the basement and
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- . . ~9Lqs~ .
x4' ~e~ so �
~ . J,~
. . 1,2 . S~
. . 55
LP L5'"M 1,0
56 .
0,9 , � �
I ~
y~ 0,8 60
_ .
. � . 65
30 ~~6 67
~ QS 70
74
20 , 75
0~~ 76
80 �
~ ~
' .
s ~ j 11P~ H* M/C
~ ~O YO ~O ~fO H~~KM Z T, 4 S 6frPCpNM~C
Figure 96. Graphs for Determination of Seismic Deflections
Calculated for Boundaries from the Surface of the
Variscian Basement to the Surface of the Basaltic
- Layex
approximately to the surface of the basaltic layer). Beginning from the sur-
face of the basaltic layer and to the Mohorovicic Discontinuity, the depths
to the interfaces are related to the line segment of length Lp - LS, located
on the approach azimuth of the P wave to the recording station at distance LS
from it.
Depth charts are constructed sequentially from top to bottom from the surface
of the basement to the M discontinuity. Regions with similar values af depths
lying within the range of accuracy of their determination are distinguished
from the data plotted on the plotting boards. For example, the values of
depths 16.4-16.7, 17.5-18.7 and so on ~re similar with an error of + 0.1 km
- in determining the depths to the surface of the basaltic layer (see Figure 64).
Isolines are plotted through the centers of the regions with similar depths.
They do not have to be located at equal dept;i intervals. The derived values
of a11 depths to the interface alony the perpendicular or in directions parallel
to the isolines are projected onto the line of the profile as a fun~tion of the
completeness of the derived data and are ~lotted on the profile where they are
also averaged with regard to the accuracy of determining the depth to the inter-
face. The charts and profiles are averaged simultaneously.
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:
-
~ ~
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The Method of Comparing the Data of PS Waves to Materials of Explosions and
DQep Drilli;~g
The data of PS waves are tied into the materials of explosions and drilling
by the times Q tPS-P and time profiles using the tormulas and calculations
given below.
Comparison to ma~erials of explosions by time profiles is made in the pres-
ence of curves vpsr = f(H) and I~r = f(H) derived in processing the explosions -
by recalculating them to time profiles Q tPS-P by formula (7.4). The recal-
culated profiles of 0 tpg-p for their stratification are compared to the
graphs vppl and vspl, also derived by the curves vpsr = f(H) and I~r = f(H).
Comparison of the time profiles constructed from PS waves at Q~ 70� and
theoretically calculated by the curves vpsr = f(H) and Ksr = f(H) for one of
the profiles of the North German Depression is shown in Figure 94. As can be
seen from this figure, the boundaries for the PS waves correspond to the
velocity boundaries of P and,S waves registered by "Zemlya" stations from
explosions,with velocity of vppl equal to 5.3-5.4, 5.6-5.8, 6-6.2, 6.5-6.7,
7.8 and 8.4 km/s. '
The interfaces constructed by PS waves are compared on the depth pr.ofiles (see
Chapter 5) to the sections of refracting boundaries separated by P and S waves
from explosions. Good agreement of similar profiles for the entire region
indicates agreement of processing the materials by PS, P and S waves.
Comparison of Q tps-p to the times tpp and tps from explosions is accomplished
, by using the Visser-Berlage formula [185]: ~
.etPS-P= pi (Ki-1) f 1-F C ~ps 2K1 sinaipll. (7.9)
L .l
Formula (7.9) can be found by two methods. The first method is described in
[108]. The second method includes determination of the diff~rence tps -'~,,tpp,
~ where tpg and tpp are the times intercepted by the hodographs of refract~~d
S and P waves above the point of the explosions through the parameters of the
medium. If there is dispersion of the seismic velocities (or a low value of
it) or if the PS, P and S waves are recorded at the same frequencies and also
- for refracted P and S waves obtained close to their initial poants, the values
of tpg and tpp for refracted P and S waves can be expressed, as for the lead- -
- ing waves, in the form [67]. -
`~1 C09 isi ~ 2H1 C09 tpl
t03 = ~91 ~ tOP = vPl ~ ~7. ZO~ -
Hence,
~os ~op Nlcosi51 Hlcosipl -
2 2 u31 ~Pl ~ ~7.11~ ,t
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�
As a result of simple transformations of (7.11), we find
z
tos ~op _ Hl ~gl-1) r1-~" ~ upz ) 2K sin2 iPl � (7.12)
2 Z P1 ~ i
The equality of the right sides of equations (7.9) and (7.12) permits one
to write -
eap9 _ p = `�S _ top
2 2 ' (7.13)
- Thus, the refracting boundaries and interfaces can be compared by knowing
the delay times of the composite wave-- ~tpS-P and the times tp for P and
S waves.
The interfaces are compared to boundaries by seismic logging data us'ing the
formula -
Alpg_p= t23 - t2 �'~%tagC03Lgl-tppC08iP1 (7.14)
t~g and tpp are the travel times of ~ and P waves along the vertical.
Assuming cos igl cos ipl, we find
Atps_p ^ ~tos-taP~ cos ipt. (7.15)
_ Characteristics of Interpreting Composi;~e Transient PS Waves Formed on Sloping
Interfaces of the Earth's Crust
The difference of the method of interpreting PS waves for sloping interfaces
(~Q ~ 10�) includes the need for additional analysis of.wave fields by cor-
r~lation and ordinary seismograms and to use three-dimensional constructions -
- which take into account the larger angles of inclination of the interfaces.
The method of interpretinq lateral PS waves has essentially not been developed.
- However, taking into account the dynamic and kinematic characteristics of
lateral PS waves, one can use all the methods of interpretation for them valid _
for diffracted and planoreflected waves (methods of intersections, time fields
and so on) [45, 116, 131]. Interpretation of lateral waves permits one to find
dat~ about the propagation velocities of P and S waves directly fram composite
waves.
The method of interpreting transient PS waves formed on sloping interfaces
- includes separation of these waves on the recordings of earthquakes, construc-
tion of the time profile and grouping of the points on it by boundaries, con-
struction of the first deptti profile by the method for a horizontally layered
180
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medium, determination of the line of the strike and dip of the interface and
also the azimuths of the displacement vectors of the incident and refracted _
P and PS waves, construction of theoretical graphs, determination of the
angles of inclination of the interface and construction of the exchange sur-
faces in the profile and in space. .
Separation of PS waves formed on sloping interfaces of the crust among PS
waves occurring on the horizontal sections of the boundaries and also separ-
ation of transient ar_d lateral (transient reflected and transient diffracted)
PS waves is accomplished by using the criteria outlined in Chapter 6.
O S lO IS R,KM
dnMep cmm+quu (1)
_ ~ 1 ? 3 4 5 6 7
~ _ . - -C'~- .
.
Z ' --C~~
. �
:
. .
. ~
---�-Q
4 ~ � - � �
. ~
.
-a
. . .
6
: _ ~ ~ o
.
.
g � -
.
. .
10 ~
df~-F~~ ~1 2 ~J
Figure 97. Time Profile for Region with Projections of the
Paleozoic Basement onto the Earth's Surface:
- 1-- A tpg-p from different earthquakes; 2--regions in which
the values of L1tps-p related to the same interface can be
located; 3--assumed correlation of PS waves on the basis af
horizontally layered model of the medium
Key : ,
1. Number of stations
The time profile is constructed by the ordinary method described for a hori-
zontally layered medium. Despite the presence of a large dispersion of ex-
change points on the ti.me profiles, grouping of points with similar values
_ of Q tpg_p is observed (Figure 97). These regions of points are related in
~ the first approximation to the same interface. The values of the possible -
dispersions of 4tpg-p and accordingly the range of L~ tpS-P in which the
exchange ~oints related to the same interface can be found are determined for
the region of investigation by formulas (2.11) and (2.12). The maximum values
of dispersion of ~tpg_p, corresponding to the case of approach of P waves to
the interface along its dip-rise line, are usually determined. t
-
~ 181
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The preliminary depth profile is constructed by the method for a horizontally
layered medium. In this case the mean value of 0 tPS-F fr~.� th~ dispersion
of points related to the same boundary is used for each recording station and
for each interface.
The strike and dip of the interface are determined in the following manner.
Graphs of the displacement of soil particles along the horizontal components
of the PS wave recording are constructed with regard to calibration of the
channels. The graphs of displacement for the first interface are also con-
structed by the horizontal components of P~raves. 2`he graphs of oscillation _
of soil particles from PS waves registered at the same station~~and condition-
ally related to the same interface are plotted on the same plotting board
(Figure 98). The oscillations of the soil particles in the horizontal plane
from the P wave are plotted on this same board for the first interface. The _
- direction of the dip-rise of the boundary is deternu.ned whexe the azimuths of
the displacement vectors of PS waves determined by their amplitudes and ca1-
- culated by the formulas of [136] coincide. The direction of the strike of
- the bo:indary is characterized by the maximum difference between these azimuths.
The azimuths of the displacement vectors of the incident P wave and the P and
PS waves refracted on the boundary are understood as the directions in the
horizontal plane which comprise angles W 2, ~ i and fy 1 with axis Ox of
thry right~handed coordinate system xyzo (see Figure 2A)� The extent of devi-
ation of the azimuths of displacement vectors of the P wavesroachinlnthenre-
tY;e boundary P(~/2) and the P((y 1) and PS ( 4' 1) waves app g
cording stations (see Figure 20) can be determined either directly by the
- drawing of Figure 98 or by formulas (2.48) and (2.49).
Theoretical graphs of the dependence of 4/ 1 and ~'1 on w 2 at parameters
_ of (P , L1 and K' are calculated for each interf~ e constructed on the pre-
liminary depth profile. The graphs of ~ 1= f( 2), calculated for the
following parameters of the media: i~l = 16� (L~ = 60�), K' = 0.425 and
CP = 0.10, 20, 30 and 50� I qg, N?, which corresponds to angles of ipS up
to approximately 20�, are presented in Figure 99.~ The process of determinatio�~
of the angles of CP by the graphs of yJ 1 and ~ 1= f( ~ 2) includes the fol-
lowing. The directions of the dip and strike of the interface and the values
of ~ 2, ~ 1~d ~ 1 are determined by the aggregate o� points for a single
recording station, related to a single interface. The value of 4'~1 is de- _
= termined by the horizontal components of the PS waves and that of ~J1 is ,
deternuned by the horizontal components of the P waves.
Knowing the value of Q for earthquakes ( and accordingly of iP ; and also
of K' and KII by the values of y~l, and ~ 2, the angles o~ ~ in the
dip-rise direction of the interface are ldetermined.
The depth of deposition of the interface at Q~ 10� is determined by the
formulas which take into account angle
,
- H _ etpg-pvp~p (~.16~
~ ( 1 ~
(K~p-1) S ! -F- ZK~P cosa epl} -
t
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C (1? .
t
~ /
~
i ~ z -
o,~ 2 )
I /
wZ+~
_ ~3~3 y p ' 9 B ~4)
_ i ~ ~ w J
- I ~ ~
- i ~ .
I -
~ z \~c`'~~y~~6)
~ `5 ~ ~
~l ~2 ~3
Figure 98. Diagram which Illustrates Determination of the Line -
of Dip and Rise of the Interface and the Values of
~ 1, ~ 2 and by Oscillations of Soil Particles
from PS Waves in the Horizontal Plane:
1--displacement vectors of PS waves determined by their amplitudes;
2 and 3--dip-rise lines and lines of strike, respectively, of the
_ interface
Key :
1. North 4. East
- 2. pip 5. South
3. West 6. Rise
or
Atpg _ pvp~D
HPl = ! ` -F Xp 91II
_ (K~p--i) ii-~- 2K~P C08~tPlj (~.17)
At d~ 10�, the formula for calculating depth is written in the form
etp~-pvp~P
~ IC~p�COSigl-co9iP1 ~ (~.18)
- Formula (7.17) is most convenient for determinafi.ion of H. The values of the
seismic deflections for H' and H" are determined by the formulas
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Y'~,~Pa~Y~ -
180
150
920 ~
; ~
: 90 ,p
6o yp
~ 30 ~
~ S0~ ~
~ ' 1gp 170 ~
y?2 o a 90 I8D
~ so=so ~ ~'i.~
3
0 '
~ '
" 0 ~
~ -
150
180 .
~'~IP4~Y~
Figure 99. Theoretical Graphs of Dependence of ~ 1 on ~ 2
Hsin(~+tsi) ~ -
- L$ - cos tsi
Hsin + tpl) (7 .19 )
Lp - COS tP3 ~ -
- where H= H' at L~ ~ 10� or H" at 10�.
The seismic drift for Hpl is determined by the formula
Lp =~(asin ~'-~xop)"-f-ba sin2~': (7.20)
Recalculation of depths by the perpendicular to the interface (H' and H") to
depths along the vertical is accomplished by the formulas -
f[a H cos (y: + isi) ~ -
1 .;;'1 a - cos igl (7.21)
R� H COS (tQ + ~Pt~�
_ p COStPl
184
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~ ' 1978 _ ~ _ ~ ' e ~YR' ~ ~ ~r ~
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Having found the value of depth H by formulas (7.16)-(7.18), the entire
process of determination by gr.aphs c~ 2= f( ~ 1~ l~l) and H by formulas
(7.16)-(7.18) is again repe~ted. The cycles of determining c;p and H are
repeated until the discrepancies cf their values found in the last two cases
dc~ not exceed the error of determining them by the described method.
Sloping inter�aces are constructed in the plane and in space by PS waves in
the following manner. If the line of the profile coincides with the dip-rise ~
direction of the interface, the values of H, L and C.P calculated by formulas
(7.16)- (7.20) and by graphs ~ 2= f( lN 1, cY 1) are plotted in the plane of c
the profile. If the profile passes at angle Y rather than along the inter- _
' face dip-rise line, ~hen angles ~ k for this directiun are determined by ~
the foi-mula
sin q~K = sin cp cos y. ( 7. 2 2)
~ In this casP the values of ~ k calculated for the given direction of the
profile are substituted into fox~mulas (7.16)-(7.18) for calculation of H.
The values of H' and H" from the recording station are drawn at angle CP k to -
- the vertical. The boundary is drawn perpendicular to this straight line.
S7~oping sections are limited by the points of separa~ion of P and PS waves
- from the interface, determzned by f~rmulas (8.19?. The entire s~oping surface
_ is included between Lg ar,d Lp. Its length is equal to (Lp - Lg)/cos CP k.
The boundaries are constructed in space by me3ns of a sp~ci:l isometric scale--
a protractor (114]. The values of H are calculated for this purpose by form-
ulas (7.i6)-(7.18) at the corresponding values of ~ k and are plotted in
space on the approach azimuths of PS wave5 from earthquakes determined by
formulas of [136].
The results of processing PS waves for some observat.ion points by the method -
for horizontal and sloping interfaces are presented in Figure 100. The di- -
vergence of the results of processing, even for upper, shallow-l~,in g cioriaons
of the ~:rust, is si.gnificant. Shifting ~f the bnundaries in depth and in the
- plane comprises 30-100 percent of the real depth of deposition of the inter-
face. Moreover, separated plateaus or even entire sections of sloping boun-
daries when processing by the method with regard to the angle of inclination
of the interface instead of the isolated poir~ts or horizontal p~.ateaus when
using the method for horizontally layered media. For example, a composite
boundary with ~tpg_p = 0.2 second is d~termined at station 2 from recordings
of four earthquakes. The use of the method of interpretation for a horizontal
- interface yields a single point at a depth of approximately 1 km under the sta-
tion. When processing by the method for slopir.g boundaries, a curvilinear
boundary emerging in the region of station 3 to the daytime surface is found.
The horizontal plateau under station 3 with ~ tpg-p = 0.55 second is shifted
under station 4, being inclined at an angle of 60� to the horizon. The plateau
of this same station with ,~,tpg_p = 0.3 second is shifted under station 4 and
185 ~
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,
~ 5 6 R,KM -
0 1 2 �3 -
Z yoMe cr
~ P CmaNty~u (1) -
Z 3 y s 6 7 8
- 1 ~�Z ' , `/,ara25 -
~4~
"~i.~`5~~~2 ~ ~ � Q2
0?-~ Q3 0 p � ~i'-.s'
, ~ � _ ~ Q25
- Q,SS
1 ~ ~
455?-''* ~ ~ ~2 ~
H~KM
: Figure 100. Results of Processing Separate Exchanqe Points with
_ tpg_p = 0.2-0.55 Secon3 by the Me~.t~~d for Horizonta?
(1) and Sloping (2) BoundaritG� The icientical symbols
near the plateaus cor-espond to a single earthquake and _
the numbers correspond to L~.tpg-P in seconds.
Key:
- 1. Numbers of stations
is inclined at an angl~ of 45� toward thehorizon. And finally the seri~s
of points under stations 7 and 8 with Atpg-p = 0.2-0.25 second is trans;-
~ formed to sloping plateaus loca~ed between stations 7 and 8. The errors of _
- construction may increase significantly for deeper interfaces of the crust.
The described method of canstructing the interface in a two-layereme d aa~ I n
can also be used when constructing the boundaries in multilay~red
this case tPie most shallow-lying interface is initially constructed. The _
medium from the earth's surface to the next boundary is ~hen replaced by a
layer with mean parameters and all the processing for the deeper interface
is again carriec~ out as for a two-layered medium. Thus, the overlying medium
is replaced by a layer with mean values of all its parameters each tim~ when
constructing th~ next interface. The error of plots i~ 5-10 percent in this _
. case. If necessary f~o increase the accuracy of the plots for dQeper horizons, `
one should take into account the effect of refraction of rays of P and PS
waves on the ov~rlying sloping boundaries. ~
The Resolution and Accuracy of the Method of Composite Waves from Earthquakes -
Resolution of the Method
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Resolution of the composite wave method can be analyzed by a method known in
~rdinary seismic prospecting [10]. In this case the main parameter which `
characterizes the resolution of the method of investigation is the minimum
difference of the depths of the two interfaces at which waves corresponding
- to each of the boundaries can be traced separately outside their zone of inter- -
ference with each other and consequently can be used for further interpretati~n.
The nature of the zone of interference of adjacent PS waves and the deqree of
the reliability of determining them on the recordings depend on the value of
the ratio of useful signal to background, t1~e pulse length of the P wave from
which PS waves are formed, the structure of the interfaces, the frequency of -
the recorded signals and other factors. ~
As was shown above, the use of various methodical and apparatus procedures _
- permits one to obtain recordings of composite waves with high signal to noise
ratio (more than 5-10). Let us determine the minimum thickness of the layers, _
study of the boundaries between which causes no difficulties by means of com-
_ posite waves, as a function of the two main factors: a) the length of the
initial pulse of the P wave from wha.ch the composite PS waves are formed and
b) the frequencies of the recorded signals. ~
Let us make use of the following simplified formula to determine the minimum
thickness of the layers as a function of the lengtn of the P wave signal
Otpg_p- Pl,`Kl 11' (7.23)
For the two interfaces one may write
~ � gl ~ . -
~ et~ps-p~~=[Hl ~Kl-1)1 ~ ~t~ps-Pj:=[vp~ ~Kl-i la
Pl .11 .1 (7.24)
t '
Assuming the ray of the composite wave is close to the vertical and assuming -
in ~he first approximation that K1 and vpl for both boundaries are equal, let
- us write the difference
eHl K i
Ol~PS-P)~'-~t~PS-P),- ppl ~ 1 ~~.25~
The waves from the two inter.faces will be separated frar~l each other if
� ep 1 (Kl -1) ~ nt, ~
(7.26) _
where t is the period of oscillation and n is the number of periods which
comprise the pulse of the PS wave.
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The maximum value of ~.H1 at which separation of compo~ite waves fr.om the
two boundaries is possible if they are recorded on thE.~`same components and ,
if they have equal intensities, is determined by the fqrmula
- nt
~1 _ Kl-1 UPl� (7 . 27 )
- Estimates by this approximation forcnula yield the following values of H. The
sedimentary thickness is vlp = 2 km/s, n= 2, t= 0.5 and 1 second (f = 2 and
1 Hz), K1 = 2.7, H1 = 1.2 and 2.35 km. The crystalline crust is vlp -
- = 6 km/s, n= 2, t= 0.5 and 1 second, K1 = 2 and l~ H1 = 6 and 12 km.
;
Recording of PS waves from different interfaces on differen~t horizontal com- -
ponents, registration of PS waves first on recorclings of horizor.tal components
with an increase of ~ relatEd to the deep interfaces of the crust and the
- different intensity of PS waves formed at different interfaces contribute to
an increase of resolution of the camposite wave method. Moreover, the reso-
lution of the composite wave method is increased due tn the fact that earth-
and so on) may produce composite
quakes with different parameters (0( , ~ ,
waves at different interfaces. The aggregate of the given factors permits
one to separate interfaces in the sedimentary mantle located at intervals of
100-200 m by depths and those in the crystalline crust at 200-500 m.
PS waves from the surfaces of the Variscian ( A. = 18�) and Caledonian ( p = -
= 70�) basements, the time interval between which on the time profile ccimprised
0.1-0.2 second, while the value of 1S H1 on the de,pth profile.comprised 0.5 km,
were separated in the first arrivals due to different values of ,L~ (18 and 70�)
when working within tY~e North German Depression. Accumulation of experimental
material by P~ waves from earthquakes with different values of ~ made it
- possible to find PS waves in the region of the first arrivals which were ex- _
changed on the surfaces of the Variscian (,L~. tpg-p = 1.6-1.9 seconds),
= 1v7-2.2 seconds) and Pre-Cambrian (,L~ tpS-P = 2�1'2�5
Caledonian ( A tFS-P -
seconds) Basements in the transition zone from the granitic to the basaltic
layer (L1 tpg-p ti 2.9-3.2 seconds) at each of 650 observation points from
recordings of 1-3 earthquakes within the North German Depression. Waves ex-
changed a~c deeper interfaces of the earth's crust, including the Mohorovic~ox-
Discontinuity tpg-p = 4, 4.6, 5.0-5.4 seconds) were registered at app
imately half of the observation points on earthquake recordings with L~ = 140�.
P6 waves formed on the Mohorovicic Discontinuity were 2-10 times more intensive
than PS waves related to the shallower interfaces of the earth's crust'in some
- sections of the North German Depression. This provided confident separation
of them on the recordings uptin overlapping af signals up to 50 percent and good
correlation alonq the profiles.
The dependence of the resolution of the camposite PS wave method on the fre-
quency of the recorded signa].s can be manitested for sharp interfaces due to
- the large P_wavelengths,'as a result of which exchange of thsse waves for S
waves may occur in some zone near the interface rather than directly on it
and also due to the fact that the boundary is a transition zone or bench of
188
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,
L
. _ . , , , . _
. . _ : , .
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layers. In both cases the dependerce of tpg-p on the frequency of the
- recorded signals should be observed with a dip of P waves of different fre-
quency to the interface or exchange layer. To study this effect, we set up _
experimental studies near a deep borehole which exposed a Paleozoic Basement _
(Tashkent). Nine recordings of aftershocks of t~e Tashkent earthquake of
26 ApriZ 1966 with frequenc~ of P waves of 8-10 Hz, 10 recordings of near
earthquakes with frequency of P waves of 3-4 Hz and 12 recordings of remot'e
earthq~~akes with frequency of P waves of 1-2 Hz were registered. According
to the materials obtained, a graph of the dependence of L~ tpg-p on the
period of the P wave on which it was clearly obvious that L~.tpg-p is not -
dependent on the periods and accordingly on the frequencies of the P waves, ~
was constructed. This made it possibie to conclude that P waves are exchanged -
for S waves for sharp boundaries (of the tyne of the Paleozoic Basement) on
its surface and ~t not dependent on the P wavelength. Therefore, the use of
P and PS wave recordings from remote earthquakes with frequencies of approxi-
mately 1 Hz does not reduce the accuracy of constructing the surface of the
basement and consequently does not reduce the resolution of the composite
wave method.
With a dip of P waves to transition zones [121], Q,tpg_p will also not depend
on frequency if the structure and thickness of the bench of layers comprising
the transitiun zone remain unchanged. In the opposite case, variation of
~ tpg-p as a function of frequency will vary within the range of values
which comprise the difference of the travel time by P and S waves of the bench
of layers which form the transition zone. According to materials of remote
earthquakes with similar valuPs of frequencies (f ti 1-2Hz) for the boundary
" which is unchanged in thickness by the bench of layers, Q tpg-p should not
vary by more than 0.1 second for the same common point at the interface [121]
' (due to the possible effect of the anisotropy of the medium) and either the
roof or the bottom of the transition zone should be traced when tracking the
PS waves from station to station by recordings of remate earthquakes. Actually,
the values of A tpg_p correspond eithf%r to its,roof or bottom or they have -
- intermediate values between the room a_.:;d bottom upon correlation of deep PS .
waves from station to station for the transition zone from the crust to the
~ mantle. This indicates, first, that we are dealing with transitinn zones in
the crust and separation of them by individual earthquakes may lead to sig-
~ nificant errors. To avoid these ~rrors, F waves from the exchange zone of
not more than 5-7 earthquakes. 7.'his makes it possible to profile rather reli-
ably the exchange zone. Second, P waves are replaced by S waves in difierent
parts of the transition zone. Moreover, the resolution of the composite wave
method also remains independent of frequency in this case (since essentially
identical frequencies are observed from remote earthquakes) and is determined
mainly by the length of the P waves.
_The Accuracy of Constructing Interfaces by PS Waves
I The accuracy of constructing interfaces of the crust by PS waves is determine~ -
by the q,uantity and quality of the initial matzrial, by the correctness of
determining the nature of PS waves rp~istered on recordings, by their correla-
tion from station to station, by the validity of the formulas used to calculate
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depths and also by the errors in determining the parameters of the media
used to construct the depth profiles. 'Since two types of profiles: time
and depth, are used during investigations with "Zemlya" stations, let us
estimate the accuracy of constructing each of these profiles.
The time profile. The accuracy of constructing the time profile is determined
by the reliability of the correlation of PS waves and the dependability of
identifying phases of P and PS waves of the same type. The main errors of
separation and correlation t~f PS waves occur in those cases when PS waves
comparable in amplitude are separated and correlated in the subsequent inter-
~ ference part of the recording. In this case errors by 1/2 or a single phase
may occur when separating PS waves, which comprises 0.5 or 1 ~~cond, respec-
.tively, for recordings for remote earthquakes. Since the time profiles are _
compiled by a series of earthquakes (10-34)in investigations with "Zemlya"
stations, the errors by one and one-half phase in separation and correlation -
of PS waves by any 1-2 earthquakes are easily detected and eliminated from
subsequent constructions.
Let us estimate tre possible time confidence intervals of the existence of
interfaces of the earth's crust when they are constructed from PS waves.
Let us assume that the law of error distribution is normal, the probability
_ distribution density for which is c~etermined by the formula
(x-a)+
~~x)= 1 e zo= (7.28)
- v 1~2n
where"x is the observed value of ~ tpg_p, a is the selective mean value of
n
1 '
~tpg _ p = R ~ ~QtPS-P~+
� l~l -
and G 2 is the standard deviation of ~ tps_p determined by the formula
rt
Q2= n LII~tPS-P~l"~~EPS-P~~Z�
_ t-i ~
The confidence interval of the existence of L1tpg_p is calculated by the r
formula
E_ �t(1-~, n-1) ~~bn ~ -
where t(1 n- 1) is the Student t-distribution and n is the number of
- samples (earthquakes or PS waves) [71].
The estimate of parameters p( , G' and ~ was made for 1-30 earthquakes at -
values of probability P= 0.9, 0.95 and 0.99 for the following interfaces of
~ 190 .
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crust of the North German Depression and the rayons of Tashkent: the surfaee -
~f the Pre-Cambrian and Paleozoic Basements, the transition zone from the
granitic to the basaltic layer and from the crust to the mantle. The error -
reading the times on the seismogr_ams comprised 0.05 second, The initial
spread of times for the surface of the basements comprised +(0.05-0.1) second,
for the surface of the basaltic la~er it comprised + 0.2 second and for the
Mohorovicic Discontinuity it comprised 0.2 second. The time confidence in- ~
tervals of the exis~tence of the surfaces of the basements at P= 0.9 and _
n= 7-8 comprised +0.05 second (3-5 percent) and those for interfaces of the
earth's crust comprised + 0.1 second (1-3 percent) (see Figure 39). If errors -
by one-half phase or one phase remained upon construction of the time profile
for any earthquake,`this will increase the confidence interval of the existence
of the basement surface by only 0.1-0.2 second at n= 15 and P= 0.9.
The depth profile. The error of constructing the depth profile is caused by
the error in determining the nature of PS waves, by the time dispersion of
~ tpg_p observed on the time profiles, by the error caused by distinction
of real-from theoretical media and by the error of determining the different
parameters of the medium (vpsr and FCsr) used in constructing the depth profiles.
Incorrect determination of the nature of PS waves may lead to significant errors
in constructing the profiles and is the cause of the appearance of intermediate ~
- interfaces unrelated to anything. Processing the PS waves formed on sloping
interfaces by the method for a horizontally layered medium leads';to additional -
false boundaries--interfaces of the crust--due to the incorrect determination
of the polarity of PS waves by the quadrant system. Moreover, e~rors in the
arrangement of the boundaries in the plane and on the profile may reach 30-
100 percent (see Figure 100). Errors in determining the angles of inclination
of the interfaces may reach 45� or more. In platform regions where the angles
- oi inclination of interfaces do not exceed 10�, the use of accumulation of PS _
waves by receiving points, jointly with their dynamic analysis, permits one
- to sufficiently clearly separate transient composite PS waves. All remaining
types of waves yield dispezsion at depths which may comprise 100 percent or
more.
- The confidence intervals of the existence of deep interfaces of the earth's
- crust, dependent on the time dispersion A tpg_p, comprise +(100-200) m(Hf ~
N 5 km) at P= 0.9 and n= 7-8 and they comprise 400 m(H up to 33 lan) for
interfaces of the earth's crust.
The error caused by distinction of real from theoretical media includes the
error caused by failure to consider the effect of angles of inclination of the
interfaces of the crust, the error c3ue to the use of the simplified Hasegawa
formula and the error occurring upon approximation of multilayered media by
- two-layered media. Failure to consider the effect of the angle of i;nclination
of the interface for a two-layered medium at 0-10� and 10-140� can
be disregarded and the depth to the interfaces can be determined by formulas
for horizontally layered media. Formulas for horizontally layered media may
also be used at 0-30�, A= 70� and CQ = 0-60� and Q= 140�. At
- c`i 7 10�, Q~ 20:~ and 20-30� and L~, = 20-70�, the use of formulas for
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horizontally layered media may lead to errors in determinat~on of the depths
of interface deposition which comprise 10-100 percent or more.
Replacement of the complete Hasegawa formula by a simplified formula is pos-
sible ii the time difference in ~ tpg_p does not exceed + 0.1 second by the
two given formulas. This is possible at 30� for the basement surface*
at L~ ~ 40-50� for the surface of the basaltic layer and at L~ ~ 100� for
- the Dlohorovicic Discontinuity.
_ The following values of errors caused by replacement of multilayered media
by media with a smaller number of layers, were obtained for the model of the
crust in Figure 3. There are essentially no e~rc~rs in determination of
~j.tpg_~ when a three-layered model of the sedimentary mantle is replaced by
a single-layer for earthquakes with.4 = 140� and the error comprises 0.07
- second for earthquakes with L~ = 20� and 0.12 second for those with .A.= 1~��
The error in determining the depths of deposition of the basement surface for
r~ earthquakes with ,L~ = 10� comprises 0.3 km. RPplacemer.t of a nine-layered
model of the crust sequentially by a 4-, 3- and 2-layered model increases the
error of determination of Atpg-p and the depths of deposition of the Moho-
rovicic Discontinuity from 0.1 to 1 second and from 0.65 to 6.5 km, respec-�
tively, for earthquakes with .a 70�. ~e errors upon ~eplacement of a _
multilayered by a two-layered medium can be dis'regarded at LS. = 140�.
The rel~.tive error of determining tre depth of deposition of the interface
when using the simplified Hasegawa formula at separate points and by unit
- recordings can be calculated by the formula
aH ~(~~ps-p) �op~p~+ ex~p ~ _
a + v g~ .
H AtP~-P P~P P
The errors in determination of depth to the interface do not exceed 8-10 per- ,
cent with errors in determination of 4 tpg-p equal to 2-3 percent, ~Psr -
= 2-3 percent and I~r = 4-5 percent. The use of the aggregate uf recordings
of PS waves from many earthquakes at each observation point and the use of
statistical methods of processing the materials reduces the relative errar
in determining the depths to the interface of the earth's crust. As was
indicated above, the relative error of determining the.depth to the basement
surface will comprise 5 percent with the numbe.r of PS waves equal to 7.8 and
probability of P= 0.9, it will comprise 3'''percent to the surface of the
basaltic layer and 1 percent for the Mohorovicic Discontinuity.
*
Estimates of the confidence intervals and errors due to failure to consider
angle i were made from materials of the rayons of Tashkent and the North
German Depression.
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a '
METHOD OF DETERMINING THE COORDINATES OF THE FOCI OF EARTHQUt,KES AND =
INCIDENTAL EXPLOSIONS _
Moscow SEYSMICHESKIYE ISSLEDOVANIYA S APPARATUROY "ZEMLYA" in Russian
1977 signed to press 31 Jan 1977 pp 183-193
[Chapter 8 from the book "Seysmicheskiye issledovaniya s apparaturoy
'Zemlya"'by I. V. Pomerar~tseva and A. N. Mozzhenko, Izdatel'stvo Nedra, '
- 1,400 copies, 256 pages]
[Text] The method of determining the coordinates of focal zones is essentially
identical for explosions and earthquakes. It includes separation of the first
arrivals of P and S waves on the recordings, construction of the Vadati graphs
- from them, which are the dependence of the delay times of S waves with respect
to P waves ( L1 tg_p = Tg - Tp) on the absolute time of their recording (Tg
and Tp), isochronic charts, determination of the time of occurrence of earth-
quakes at the focus Tp and the location of the focus. The type of the source--
an explosion or earthquake--is also additionally determined under specific
conditions. Different methods of determining these values~are used as a fur~c-
- tion of the ratio of the depth of the focus hoch and the epicentral distance
p. Methods of intersectiizs, ~he Vadati method and methods of solving a
system of three-dimensional~,2quations of hyperbol�s are used in the relation
p L h~~h [70, 15]. Methods of intersections, hyperbolas, Golenet~kiy and
- others are used p~ H.
The method descri~ed below was tested upon determination of the coordinates .
of foci from recordings of 356 aftershocks of the Tashkerit earthquake, 125
special explosions, 650 incidental explosions and 200 near earthquakes within
Tashkent, the Azov-Kuban', Pre-Caspian and North German Depressions and on
the Southeastern Russian Series.
Determining the Moment of Occurrence of asi Explosion or Earthquake _
The moment of occurrence of an explosion ~r earthquake Tp is determined mainly
by two methods developed in the seismology for direct waves: by the Vadati
method [137-151] and by the arrival time of P and S waves. To determ.ine Tp
- by the Vadati method in the presence of n stations, n equations of the follow-
ing type are compiled and solved:
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T~-TY=~(K-1)(Tp-To), (8.1)
The system of equations (8.1) is solved by the graphical method. The absolute
arrival times of P and 5 waves to different recording stations Tp and TS are
plotted on the x-axis (Figure 101, a) and the difference of the arrival of P
and S waves to the recording stations (TS - TP = L~ts_p) is plotted on the
y-axis. The straight lines Tg = f( p tg-p) and Tp = f~ L1 tS-P) intersect
on the Tp and Tg axis at point Tp since at the moment of occurr~nn~e Pa he
explosion or earthquake TP = Tg = Tp. The value of K= v~/ S
from the focus to the observation station was detErmined simultaneously when
constructing the Vadati graphs. The times Tp for all the recording stations
were plotted along the x-axis and TS were plotted along the y-axis when dE-
termining Tp by the arrival ti.mes of P and S waves. The derived poin~s were
averaged by a straight line whose point of intersection with th~heisTs~eaxisX
of the coordinate angle yielded a value of Tp, read both along
and zhe Tg axis. Z'he second method with the presence of the value of K made I
it possible to determine the time Tp, having data only for one recording
- station. A straight line with angular coefficient K= vp/v5 was drawn from
the point with coordinates Tp and Tg and the point of intersection of ~es
straight line with the bissectrix of ang~e (B) yielded values of mp.
Vadati graphs and the graphs TS = f(TP) had a small time dispersion and were
averaged easily by straight lines wh~n direct waves approached the recording ~
stations. Breaks appeared on the Vadati graphs in the case of approach of _
zefracted (refracted in two- and three-layered media) waves to the recording
stations. The errors in ~he recording times of P andf~T averalhdfor differ-
tion of the points on the Vadati graphs and the TS p~ g p
ent values from the straiqht line. 2'he points on the Vadati graph and the
graph TS = f(TP) did not lie on a single straight line in the case of an
error in determining the arrivals of P ~r S waves. All the points could be
averaged only by means of a series of broken lines in the case of transition
during correlation from one type of P and S waves to another, for example,
.Q
~ r$;ats-P~~ -
9
i .
- 8 ~
8 -
. Z� ~p
~ . 6 � dt5-PJ ~tP~
3~ Z 8. 2 8
~ dts-Pf ~ts~.
. 6~q~ 7 10 7 6 ~p _
~ 3 3 9
�5
T ~
3 4 5 6 7 ~ 9 10 TP~TS,c
~6
194 ~
[Capti~on for Figure 100 on following page]
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x
U ~ -
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195
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from straight lines (by s'cations installed in the immediate vicinity to the
focus) for refracted waves (for stations installed far from the focus) on the
Vadati and Tg = f(Tp) graphs.
Determining the Location of the Focus of an Explosion and Earthquake
The position of the epicenter of an explosion or earthquake is determined by
ordinary methods outlined in seismology. When working with the "Zemlya" de- -
vice, the method of intersections, the Vadati method and ta a lesser extent
the average Golenetskiy lines and hyperbolas w~re most frequently used [151].
A method of determining the foci of local earthquakes by solving a system of
equations of three=dimensional hyperbolas was proposed in 1967 [70].
The method of intersections made it possible to determine the epicenter of
the ~arthquake and the depth of the focus simultaneously by the arrival times
of direct and refracted P and S waves or by the difference of the arrival
times of S and P waves to the recording stations. The number of observation
stations was not more ~than three when using t.his method. Theoretical or ex-
perimental hodographs compiled fcr the region of investigation at different
focal depths were necessary when determining the epicenter and depth of the
- focus by the method of intersections. The position of the epicenter was de-
termined at the point of intersection of ares of circles with centers at the
points of installation of the recordi~g stations. The depth of the focus was
taken as that, the theoretical or ex~erimental hodographs for which yielded
minimum triangles of lack of ~ie-i.ns for intersections made from the points
o� location of the recording stations. The most accurate results were obtained
by P waves fro earthquakes with low value of p(up to 100 km) since separation
of them on th.e recordings was more reliable. In the absence of Tp or inaccur-
ate determination of it, the radii of the intersections were determined by the
difference of the arrival ti~nes of longitudinal and transverse waves ( tS-P~
to the recording stations. To determine the explosion epicenter (hoch = ~
we suggested ~hat reflected and refracted P and S waves be used. The radii _
of intersec~ions for refracted waves in multilayered media were determined by
the formula*
! ~ (8 . 2 )
i 0= 1 tS tp -~(~0 SQ - ~ppQ~ U~. r. ~
~ ~
where tg and tp are the travel times of the P and S waves from the focus to
the recording station, vf.q is the imaginary boundary velocity
v v -
Pr S~,
I v~~ r . UgrvYr ~
I
i _
*
Formula (8.2) is strici.ly valid for leading waves.
196
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vpg and vgg are the boundary (or apparent) velocities of the transverse and
longitudinal waves.
For reflected waves propagated in a two-layered medium with horizontal inter-
face, the equation of the radius of intersections ) has the form
, ~~ts _tp~z v _4~ ~ (8.3)
~
where vf = ~peff -�Seff~~PeffvSeff:~d h is the depth of the reflecting _
boundary.
The Vadati method was used only for direct waves. It was used to determine
the,position of the epicenter ,3nd the depth of the focus of only the nearest
, earthquakes (but not explosion_;) for which the epicentral distances ~ ex-
- ceeded the depths of the foci by not more than a factor of 1.5. Z"he basis
of the Vadati method was the proportional dependence between the epicentral
distance and the time A tg-p. The advantage of the Vadati method is that
a knowledge of the wave propagation velocity in the medium is not necessary
and there is no need to be given the theoretical hodographs when determining -
the location of the focus by it [151]. !
~ ~
The method of average Golenetskiy lines was used in those cases when the
wave front approaching the observation stati.ons could be assumed flat. In
this case the linear isochrone was faund by three recording stations. The
average line which gave the direction to the epicenter was constructed for -
this isochrone. The same operation was repeated with the next station. In- -
tersection of two t~r more average lines yielded the location of the epicenter. _
The focal depth was not determined in this case.
The method of hyperbolas uses the main property of a hyperbola determined as
the aggregate of points for which the difference of distances from two points',
called the foci of the hyperbola, is a constant value (151]. The hyperbolas _
were constructed sequentially for a pair of stations. Moreover, the recording
stations are the foci of the hyperbola and the hyperbola itself is the geo-
metric locatcion of the possible epicenters. Intersection of several hyperbolas -
determines the location of the epicenter. The limitation of this method in- -
cluded the fact that vp was supposed to be constant, i.e., the recorded waves
at all the recording stations were supposed to be related to a single boundary,
for example, to the surface or basement, the Mohorovicic Discontinuity and so
on. No fewer than three stations must be used in the method of hyperbolas.
Satisfactory results were obtained with four or more stations. The properties
of the asymptote of the hyperbola rather than the hyperbola itself were fre-
quently used for remote earthquakes [17].
197
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U
- The location of the epicenter was determined by plotting* the isochrones of
direct P and S waves by the aftershocks of the Tashkent earthquake of 26 April
1966 (see Figure 101). The arrival times of the P and S waves were taken from
the seismograms with an error of 0.02 second. The isochrones were made every
0.1 second. The earthquake epicenters were located within the isolines with
- minimum time. This method also makes it possible to determine the propagation
velocities of P and S waves in the medium above the focus.
The method of solving three-dimensional hyperbolas was used to determine the
parameters of foci by the arrivals of P.and S waves without using theoretical
~ hodographs. An algorith~n was developed and a corresponding program was com-
piled [70]. ~ne entire process of determining the coordinates of the foci and
the velocity characteristic in the focal zones is divided into two steps. The
value of Tp is determined during the first step by solving equations of the
following form for a series of stations _
~ 7`sn-7'pnK-~T(K-1)=0~ ~8.4)
where Tpn and Tgn are the arrival times of P and S waves at the n-th recording
station as?_d K is the coefficient of the velocity ratio of longitudinal and
transverse waves in the medium covering the focus.
The parameters of the focus are determined in the second step by solving a
- system of equations of ~he following form for a minimum of four stations
7, 1+ _ 1 ~yrt _ x~2 (i/n - y)z -I-1toq + ( 8 . 5 ) -
pn�9n 0 �P,s
CD
where xn and yn are rectangular coordinates of the n-th recording station,
x and y are the rectangular coordinates of the earthquake focus and vp, Ssr
is the mean propagation velocity of longitudinal and transverse waves. -
The Accuracy df Determining the Focal Coordinates of Earthquakes and
Explosions
The accuracy of determining the focal coordinates of earthquakes and explo-
sions was estimated for the focal zone of the Tashkent earthquake of 26 April _
1966 from recordings of its aftershocks with A= 0-20 km and als~ for the
foci of local earthquakes and explosions with 0-500 km, determined during
studies on the Southeastern Russian Series, the Northern Pre-Caspian Depression
and within Tashkent. Accuracy was evaluated both by direct calculation of the
errors of time determination and construction of theoretical hodographs and
by comparison of the coordinates of epicenters and foci determined by different
methods.
*
This method was used in studies with the "Zem?ya~j' stations since high accur-
acy of reading the times from the seismograms i~.'necessary for it.
198
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- '('1~~ ncuur.t~c+y c+C ~lptpr?nlnlnu t.h~ C~~~:,al ~+n~~,-~~inar.~a c~f rt~d ~Ftd~ah~~~~:ke r~r the.
Tuehkent earthquake when using formu.Zae (~.4) and (~.5) was evaluate~l in Lhe
followi:~g snanner. Using different combinations of initial times of the first
P wave arrivals for the same earthc~uake by alternate exclusion of one or two
stations from the calculations, regions of the possible existence of earth-
quake foci ~aere estimated, i.e., the accuracy of determining the focal coord- -
= inates in the harizontal plane (x, y) and their depth was estimated, depending
on the location of the station and the focus, the distance from the focus to
the recording station and so on.
The regions of the possible location of the epicenters of the aftershocks of
- the Tashkent earthquake registered by different stations (Table 8) are ore-
sented in Figure 102. The regions of the possible existence of epicenters
vary from 0.8 X 0.5 to 2 X 2 km2 and depend mainly on two factors: the neu- ~
tral location of the recording stations and the focus and epicentral distances. _
- The region of the possible existence of the epicenter decreases to 100 X 100 =
or 200 X 200 m2 when using recording stations located around the focus at a
distance up to 7-8 km from it.
Table 8. Data on Aftershocks of Earthquake Used for Construction of Figure
102.
_ Hon~ep a~e~mo~ca t2~ ` Horep c3~-aau++9 m~4~
TAmHCHCtfOI'0 Bj1CMH jIQTACTp811HH 8~7'QpmOHOB BgIIACH 8~7C(lIDOHOH c -
8CY 7C'fpACCH1IA ~
79 2~s~6 a~u~ 2.XII. l966 r. i, 3, 8-10, i3
80 20 e 33 ~a, 2.XII. 1966 r. 3, 4. B-!3
81 20 q 37 rflm, 2.XII. f966 r. i, 3-13
' 83a 15 ~ 26 ~txa, 3.XI1. 1966 r. !-!0, 12, 13 a
836 15 q 26 ecxx, 3.XII. i966 r. i, 2-4, 6-l0, 12, !3
84 20 ~ 7~, 4.XII. l966 r. 2-6, 8-10, !2, i3
85 13 4 48 a~a, 6.XII. 1966 r. i-7, 9, !2
36 1~ 29 x~, 31.VII. 1966 r. 2, 3, 5, 6, 9, 10
37 23 anffi, 31.VII. 1966 r. 2, 3, 5, 9, !0
39 1~c 31 ~u~s, 3i.VII. l966 r. 2, 5, 6, 9, 10
42 23 07 MIIIi~ i.V[II. 1966 r. i-3, 5, 6, 8
47 - 3~ 14 at?~, f 2.V 1 t I. 1966 r. i, 3, 5, 6, 8, 10 b
- 48 5 q(~4 bnsa, l2.VII1. 1966 r. 3. 5, 5, 8
- 50 Z v U5 en+n, l6.VI11. 1966 r. ~-4, 6-10 `
51 � `Li ~ 44 sniN, i6.VIII. 1966 r. 2-5, 7, 8
5'? 4 v 33 11t1tIS~ i6.Vlli. l966 r. i-5, 7-9
53 20 y 27 a~~ui, 16.VIII. l966 r, i, 3, 5-9
54a 3~ 38 a~t~, l7.VI[I. i966 r. 3, 4-l0 -
546 , 3 s 38 asxa, f7.VII1. 1966 r. 3-l0
Key : -
1. Number of aftershock of Tashkent 4. Stopover
earthquake 5. Hours -
2. Time of recording aftershocks 6. Minutes
3. Numbex of.stations recording
- aftershocks _
. 199
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~
FOR OFFICIAL USE ONLY
~
_ , i _
~
~ ~
o a; ~ o =
s . ~ . ~ aUi
- ~ ~ ~
~ N
- . ' ~ H O
~ ~N W ~
W O O
. ~
O p c~~d
W ~ U U
- � . xAx~-~i
tA 'C~ N 1
0 E-~ ~ dl N
- �
W td W
p~ b.-.
~ ~
~ m fn UI ~
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~ I~d ~~ll ~ ~1
u a -
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, A N ~ ~ u1 -
A m N o ro~ -
. o m = a~
0 ?~N~~
- W 'A O ~-~-I ~
N y -
. 0
~ ~1 Gl ~r-I
N W r-1 ~1 N _
~ 0 N A ~ ~ ~
co w �ri �rl N
O ; b+b~N~OR7
~ ~~~w~
4-i O N
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H d v1
_ o ,b~ ~ ~ ~,,tT,
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b , .
2~~
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- The ~rror in d~termining the depths of the foci calculated by remote stations _
may vary from 2 to 4 km. If the atations are located around the focus and if
the epicentral distances are not more than 7-8 km, the error with which the
focal depth is determined decreases to +(500 meters-1 km). The best resulta
for the after~hocks of the Tashkent earthquake were found when the distances
to the foci were equal to 6-8 km at hoch = 3-9 km. Location of the stations
at greater distances and installation of them directly in the focal zone lead
to distortion of the results. To determine the focal coordinates, it is ne- .
cessary that the number of stations be no less than four. The optimum number
for processing is 8-9 stations.
Comparison of the locations of the epicenters of aftershocks of the Tashkent
earthquake of 26 A~ril 1966, determined by the method of intersections, the
method of three-dimensional hyperbolas and the method of isochrones showed
that all the epicenters generally depict the same zone. However, their lo- -
cation, 3etermined by methods of isochrones and three-dimensional hyperbolas,
is more compact than by the method of intersections (Figures 103 and 104). �
Moreover, epicenters determined by the method of three-dimensional hyperbolas
are located closely to the isochrone centers with minimum tim,e and have 3-4
times fewer triangles of lack of tie-ins than epicenters dc~termined by the
method of intersections for a theoretical hodograph (Figure 105).
Table 9. Values of hoch (in Kilom~ters) Determined by Different Methods .
. ~
Fiorep ~2~ Cna.o6~ Homep Cl' '~2~. ~ Cnoco6~ f3~ -
aeytnerpR- ~1 Cuoco6 upocxpaticz- aee~nerpe- I Caoco6 upocrpaHCT-
cetcxx aaceveK aexuaz cexNA ~~`~K ru�ep6on
(cr. pec. 104) rxuep6on (ca~. pHC. 104)
3 1 5.28 15 4,0 5.55
4 2 4,2 i8 4.77
- 7 2.6 4,7 22 2.0 6,78
8 7,5 6,4 23 3,0 4.59
9 6.0 4.2! ?~f6 3,5 6.15
ii 4,0 5.9 24s S,h 5.17
!3 7,0 8,6 25a 6,0 4,6
i4 3,0 6,86 256 4,0 4,0
_ Key s
1. Number of earthquake (see 3. Method of three-dimensional
Figure 104) hyperbolas
2. Method of intersections
The derived data permit one to assume that the most optimum and accurate
method is solution of three-dimensional hyperbolas (Table 9) when determining _
the location of the foci of aftershocks of the Tashkent earthquake of 26 April
1966.
' .
.
The accuracy of determining the focal coordinates of explosions; was also esti-
mated as a function of the location of the stations and focus. ~~A numb~r of
201
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,
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/i
-
:.r. ; -
_ r.~ ~
\ ~ ~ ~ - - ~
I j!:'.' ^
/ . 7
~ ~ ~ ` / / :
17 ' �'~e/ / /
-
_ / ` :1' ~ /
~ 1 ~
/ i ,
~
. ~ss \ ;a.;:~::,:~:~:`~:::...
~ ~ : ~ _
~ ~ B ~::;~::::~::~:::�;l::~~...
~
-1~::: .
~ ~ \ ~ 'y~0~ -6'7 ' .�'q':'.:.
(s' 9
~
- Q~~ J ~:~~~:o~~:`~:.Q~ .
~ - ~ .
:y~ . p. .
yt� C~'�Y:
~ Z ~ ~p~' �9'; ~9.;;: , -
G ::?~0:;
8 7 3 ~
_ ~4 ~ � .
~
Figure 103. Location of Epicenters of Aftershocks of Tashkent
Earthquake of 26 April 1966 Determined by Method
of Intersections (1) and Method of Three-Dimensional
Hyperbolas (2) with Isoseismal Lines of Destruction
in Units (3) and Fault Zones (4) Determined by A. G. _
Khvolovskiy and N. B. Vol'fson by Aeromagnetic Data
- Key:
- 1. Tashkent Fault 2. Almalyk Fault Zone
estimates was made from explosions with known coordinates and moments of the
explosions. The derived results showed that the error of determining the lo-
cation of the point of the explosion comprises 5-10 percent with the presence
of a sufficiently accurate of P and S waves the investigated region and with
the location of 4-9 recording stations in one direction from the point of the
- explosion at distances up to 200 km.
- 202
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N
b
- � ro o.$~ .
s~ ~
OD ~ 7�~/~ ~ N a~
_ N M ~ll O 'Jy ~ '
N -
_ ~ ~ : ~ ~ . ro ~ ~ ~
~
. . ~ ~ ','I {yr Q
~ ~ ~ Q O E
~w~~~~
~~A~~~ -
N 41 O N N N W -
' ~ E ~ 11 ~ ~ N
N.o ~ o~i ~ 3
O 4-I N O N~Ci CT' -
~ - ~ ~
. ~ ~ . ~�~~~;s.. � N H O ~ f-I
~ " ~ ~ U 4-1 ~ (~d .Ni"., ~ l
~ O 0 d ~ O
- ' N~d~ N+~ O
. ~ O N~ tvll N c
r ~ ,
. ~ I~i ~i ~t ~I ~ ~ -
. ~ �
' ~ ~ ~ ~ 'r'~ ~ .
r ' ' ~ N~ tl ~ ~J'1 ~ ~ ~ ~e'~
-~++~s.. . ~
�~n.~:�. d A i~f 3
u~ ~ a�� t: 'd O~ O~
~ ~iN 7 0~ ' U f~.'. ~ N~ r''~tl
tl ~a �'i � 0! N ~ 'J
M N 3n n ~i
`c ~ � ~ W
, ~ M ~O ~ d ~ ~ ~ N
N ~
= O ~
~ ~ W Q~N ~A N
. e ~ ~ Q ~ v ro . ~ ~
_ w ' "
~ ~~'�~'v,~o
N . s b u~i a+ a a? ,q
_ ` ` ~~rd~~+~w
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N .C:
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4 ~-1 N O
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203
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. ' yKM II~'2_il U~~ OL78?cM~~
- . h=~, O,SKM rrP2 2,8 rr~~
1,3i ?cm~c
' t,C .
JQ h~ ~,9KM UP'~~4 US`~~~ZKM~C
3 3
9 ~/P4 E,l US=3~4 KM~C ~ _
. ti
8
7
6 ~ ~
+
5 / ,
� . ~
4
~ P
3 _x~"
/ , _
1
- ITI~ ~Z ~3
1
-~+-~4'~5 ~6 . .
~ ~ Z 4 6 8 10 12 1~ 16 18 20 22 24~ d,~?+
- Figure 105. Theoretical Hodographs of P and S Waves for Region of
~ Tashkent at Different Values of hoch and Model for -
Which They Were Calculated:
- 1--hoch = 1 km; 2--hoch = 2 km; 3--hoch = 2.8 km; 4--hoch = 4 km;
= 5--hoch = 6 km; 6--hoch = 8 km
Key:
1. km/s ~ -
204
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~
METHOD OF DETERMINING THE VELOCITY PARAMETERS OF THE MEDIUM BY RECORDINGS
OF EARTHQUAKES AND EXPLOSIONS ( d = 10�)
Moscow SEYSMICHESKIYE ISSLIDOVANIYA S APPARAT[3ROY "ZEMLYA" in Russian 1977
signed to press 31 Jan 77 pp 194-201 ~
[Chapter 9 from the book "Seysmicheskiye issledovaniya s apparaturoy
'Zemlya by I. V. Pomerantseva and A. N. Mozzhenko, Izdatel'stvo Nedra,
- 1,400 copies, 256 pages] .
- [Text] The curves of variation of the velocities of longitudinal and trans-
verse waves with depth necess,ary to interpret PS waves and the curves of _
distribution of stratal velocities of P and S waves with depth, used for
stratification of the interfaces of the earth's crust and upper mantle, are ,
determined from recordings of the first arrivals of refractesi P and S waves
from earthquakes and explosions. 7.'he velocity characteristic of tYxe medium
at the focal zone is determined by direct P and S waves. The veloc,ities
found from them frequently differ significantly from the propagation velo-
cities of P and S waves outside the focal znnes and, therefore, cannot be
used to interpret PS.waves formed beyond these regions.
Calculatinq the Propagatxon Velocities of Longitudinal and Transverse Waves .
by Recordings from Explosions and Near Earthquakes
The propagation velocities of P and S waves in the earth's crust are deter-
mined by the first arrivals of the refracted waves propagated from explosions
and near earthquakes. The Wiechert-Herglotz-Chibisov method [147, 159, 186] _
is used as the main method of interpretation. Reflec.*.ed P and S waves from
the crustal interfaces are usually not employed to determine velocities due
to their poor correlation in subsequent arrivals with spacing of observations
of 5-6 km.
The method of determining velocities includes separation of the first arrivals
of P and S waves on the seismograms, construction of single or summary longi-
tudinal hodographs and graphs of the dependence of vk on Q by them, calcula-
tion of the curves of variation of the stratal velocities with depth at points _
of maximum penetration of P and S rays and mean stratal velocities and con- _
struction of vertical hodographs of P and 5 waves.
205
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t, _
q..r,':;:. . ~ _ . , . . . .
..v_ , . . . .
1
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The principles of determ:ning the fir~t arrivals of P and S waves on the seis-
mograms are described in Chapter 5.
Longitudinal hodographs of P and S waves are constructed along the linear pro-
files by ordinary methods used in I~iPV and GSZ [38, 67). Moreover, if there
~ is a small volume of material or if it is necessary to average small inhomo-
geneities of the medium, summary hodographs of P and S waves are constructed.
They are compiled from hodographs obtained both from special and incidental
explosions and from near earthquakes. For this purpose, all the hodographs
~ obtained in a region from special explosions and sections of hodographs from _
incidental explosions and earthquakes obtained at different values of A are
constructed in a unified time and distance scale. The epicentral distances
from the focus to each recording station are plotted along the horizontal and
the difference of the absolute time Tp~g of recording the P or S waves and
~ the times at the focus Tp, the method of determination of which is given in
Chapter 8, (Tp,g - Tp), is plotted along the vertical. A summary hodograph
of the first arrivals of P and S waves registered by "Zemlya" stations from
special explosions on twelve profiles* is presented in Figure 72. A summary
hodograph of P and S waves constructed by earthquakes is presented in Figure -
69. Each section of the hodograph corresponds to an individual earthquake -
- and does not coincide in time with surrounding hodographs. This is related -
to~the fact that earthquakes, unlike explosions, have different values of
Tp,g - Tp, determined by the different focal depth. To combine all segments
of the hodographs into a single summary hodograph, they are reduced to a uni-
fied focal depth. This summary hodograph of P and S waves, compiled by Ye. M.
Butovskaya for hoch = 0, is presented in Figure 69. When determining the
velocity distribution with depth by S. V. Chibisov's method, one does not
have to compile summary hodographs by earthquakes since one only needs to
know the distribution of the apparent velocities as a function of L~ .
The graphs of vpk = f(,A ) and vgk = f( Q) of Figure 70 were compiled by
- single and summary hodographs of the first arrivals of P and S waves. The
graphs of v}~ = f( Q) were averaged by two methods. The first method includes
averaging by the method of equal sums [17]. Z'his method permits one to ob-
tain a continuous curve of the true velocities at points of maximum penetra-
_ tion of rays as a function of depth as a result of processing by the Wiechert- -
Herglotz-Chibisov method. The second method includes averaging by a graduated
line with artificially given gradient + 50 m/s on the edges of the areas of
apparent velocities. The second method is no less convenient for calculations,
but corresponds more closely to experimerital data of a layered profile of the _
earth's crust. Z"he curves of stratal velocities calculated by both methods of
averaging the graphs vg = f(,d ) for a pro�ile of the crust (see Figure 3)
showed their good convergence. The difference in the curves does not exceed
3-8 percent. .
2'he velocity distribution function with depth v(Hpr) is determined by the
given hodograph of the refracted wave to calculate the greatest depth of
*
This hodograph was construct2d and processed by A. I. Minin.
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penetration of the ray tipr~ ~Psr~ ~Ssr and Ksr by the Wiechert-Herglotz-
Chibisov method. The dependence of HPr on vg is expressed by the integral
x~OH~P
1' S arcch vK(~~np) dOhnr, (9.1)
H�p = n
. � z~0
where L~ Hpr is the distance from the point,of the explosion to the point of =
emergence of the ray penetrating to depth HPr onto the surface of observations,
QH.pr is the distance from the point of explosion to the point of emergence
of the ray penetrating to lesser depth h pr onto the surface of observations,
' Q K:Pr) is the apparent velocity of the waves at the point of the hodo-
graph obtained at distance t~ hpr from the point of the explosion and v]c(L, Hpr~
is the apparent velocity of the waves at the point of the hodograph obtained
at distance ~ Hpr from the point of the explosion. _
- Solution of integral (9.1) is possible by approximate methods by replacing -
the integral by a finite sum of rectangles, trapezoids or parabolas [17].
' TYie formula of parabolas yields the greatest accuracy and the formula of
rectangles yields the least accuracy at the same values of n(n is the equal
parts into which the integration interval is divided). An estimate of ~he
accuracy of calculations of vp carried out for a profile of the crust (se~e _
Figure 3) by formulas of parabolas and rectangles showed the following.
values of vp calculated by the fczrmula of rectangles differ from those of
vp determined by ~he formula of parabolas by + 30 m/s at depths less than 3 km.
Z'he values of vp determined by the two methods coincide at depths greater than
3]rnt. The latter permits one to use the formula of finite sums of rectangles -
in calculations of vp. It has the form
~ v (OhnP) ~ (9. 2)
H~p - n h~ arcch v~A j~nP~ ~
where h= ( Q I~r - L~.h~pr)/n is the elementary segment of sumnation. _
The curves vpPl = f(HPr) and vgpl = f(HPr), calculated by formula (9.2), are
- f(H) and vg = f(H) using the following
rearranged into the curves vpsr - sr
formulis :
' �n
~ e: .
1 (9.3)
v~p = R .
~ t�
_ 1
where ~ z is ~e ~?ickness of individual layers and t~ is the vertical travel
time of the P or 5 waves in each layer.
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~ .
~ ,
~;~x? . . : ; . . > _ . . . . . _ , , . . . .
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~ Since the curve of variation of velocity with depth can be approximated by a
~straight line in each sufficiently small segment ~ z, the value of t~ is
determined by the formula [116] for the linear law of vari.ation of velocity
with depth
tB vx~ 1n~1+~~~~ (9.4)
~ where vn is the velocity in the upper part (initial) of each layer L1 z and
~S is the gradient of variation of velocity with depth.
Graphs of the mean velocit.ies of P and ~ waves and ICsr, obtained on a"Zemlya"
profile 260 km lang from'~iive points of explosion, are presented in Figure 106.
~ f: 2 3 ~ . Sv cP vs~
/c !0 20 rc~
2 ~ 2 ~ ~
_ ~
4 a ~ ~
s ~ 1 s i~~ .
~ 1 i ~
s ; ; e i ~ .
_ :~v q ro i ~
~~z I I 11 n i n
~ `
_ !4 11� 14 _
~ ~ 1 ~ i�
' ~ ~ ~ , ~s ~ ~ . -
~e it ~ ~I
i.
~
zo. I: 1 Zo i .
~
1~ � j ; i 22
- Zy ` ~ ' 24
16 ~ ` 1 26
_ ~ , ~
- Y8 i ~ 28 ,
1 I
- ~0 ~ 2 � i 30
_ ~ I 32
_ 3y ~3 ~ .
_ Q ~ ' 34
34 q .
~ I I ~
36 $ i N K"- ~ �
N,KM
- Figure 106. Curves of Dependence of vpsr = f(H), ~Ssr_� f(H) and
Ksr = f(H) Compiled From Data of Five (1-5) Points of
~ Explosion
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The curvss vpsr = f(H) and vssr = f(H) are rearranged into vertical hodographs =
for stratification of the time and depth profiles of the crust. The times on
vertical hodographs are determined by the ordinary methodWhich the,stratalical
hodographs are averaged by segments of straight lines by
velocities of longitudinal and transverse waves are calculated. The latter ~
are rearranged into graphs of the stratal velocities of P and S waves as a
function of depth H and 0 tpS_p. Z'he values of 0 tpS-P are calculated by
the Hasegawa formula [176]. Graphs of the stratalWith retard to deflections
waves constructed as a function of H and p tpS-P g
are plotted on the depth and time profiles, respectively, constructed by PS -
waves.
The accuracy of determining the velocities and depths by the Wiechert-
Herglotz-Chibisov method is esti.mated by the method proposed in [37]. Accord-
ing to the formulas of this paper, if the distance between the observat~ion
_ points is 5 km, the errors of tying them in are + 100 m and the difference
of the arrival times of the waves to two adjacent pointssin le9hodographsdfor
th~ relative error of determining the values of vppl by 9
depths from 3 to 35 km reaches 15 percent, the error of determining depths
reaches 30-40 percent and the errors of determining the mean vslocities and
I~r reach 10-15 percent. The use of opposite and overtaking hodographs to
~ determine vpsr, Ksr and H permits one to significantly reduce the relativosite -
error of determining ~hese values. Thus, if there are 3-4 direct and opp
systems.corresponding to the same segment of the depth pro~iHe, i~edecreasesce
interval of the existence of curves vpsr = f(H) and I~r ~
to +(2-3) percent for vpsr and + 5 percent for I~sr at H= 0.9;. The large
relative error of deterniining Ksr by single hodographs, equal to 10-15 percent,
and the small error in determination by a series of hodographs 5 percent)
indicate the need to find 3-4 opposat~o determinekthe value offiCsra single
segment or to use supplementary dat
, Methods of Determining Coefficients K
Coeffic.~ents Ksr are determined by data of explosions and near earthquakes .
registered by "Zemlya" stations, by data of seismic loggin~, by calculation
~ by the Hasegawa formula, by recordings of direct P and S waves over the focus
of a local earthqualce, by Vadati graphs and by tp of hodographs of refracted
P and S waves.
The mean velocity distribution curves of Pa~esultaofsprocessing theefirstd
by using the formulas of N. N. Puzyrev as _
arrivals of P and S waves by the Wiechert-Herglotz-Chibisov method. 2'heY
permit one to calculate KS~ by direct division of the values of vpsr bY
vSsr, corresponding to the same depth. The derived curves of Ksr = f(H) are
characterized by wide spreads. The values of Ksr for the same depths of the
same profile, but found by different single hodographs may differ up to
+ 0.3 (Figure 106). Summary hodographs must be compilfdH
Ymustlthen be cal-
similar geological conditions~a~o reducelthe spread of curves of Ksr = f(H). -
culated a second time for the
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The data derived in this manner coincide ioest with the curves ICsr = f(H)
determined by other metY~ads, including seismic logging studies.
" The curve ICsr = f(H) from data of seismic logging of deep boreholes is de-
termined by the same method as the curve vpsr = f(H) and vSsr = f(H). If
there are vertical hod.ographs found as a result of seismic logging, Ksr is
calculated by the formula -
~
s
R~p= t; . (9.5)
P
- Determination of I~ r by the Hasegawa formula is possible if the depth (from
drilling data or from MOV data) and the mean velocity of longitudinal waves
ico this depth.are precisely known and the delay time of the transient com-
posite PS wave with respect to the P wave ( ta tps_p) for this same depth
is found for each level of the sedimentary mantle or basement surface. Co-
efficient I~r is calculated by the simplified or complete Hasegawa formula -
(see Chapter 2). The simplified formula can be used when determining Ksr
by earthquakes with .L~ ~ 70�. The errors of determining I~r may reach +
(0.1-0.2) or more for earthquakes with lesser values~of
The value of ICsr is calculated by recordings obtained above the focus of the
local earthquake by the formula
K Tg-T0 (9.6)
~ Tp-To
The value of Ksr is determined by Vadati graphs in the following manner. The
angular coefficients of the graphs TS = f(Tp) (see Figure 101) is the mean -
value of I~r on the path from the focus to the recording station. The graphs
- of the function Ksr = f(hoch) is compiled to find the distribution of this
coefficient with depth. The spread of values with Ksr around the curve usu-
ally does not exceed +(0.1-0.2) with error of determining the focal depth
not below 10 percent.
The value of I~ r is calculated by the value of tp of refracted P and S waves
using the following formulas. The depth of location of the refracting boun-
dary for the hodograph of the re~racted wave at short distances from xn can
be determined by the formulas for the leading waves:
v
. ~pep t S~p ,
- ~j-IOP CO9ip = OS CosigH (9.~)
H
_ where ipn and ign are the critical angles for the rays of P and S waves
emerging onto the observativn surface in the regions of the initial points.
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Assuming that cos ipn ~ cos ign, we find
t03 llpcP
' top ~ "s~~ (9.8)
Thus, having hodographs of P and S waves related to the same refraction boun-
dary and also the conjugate points on the hodographs of these waves along the
entire profile, the lines tpp and tpg are constructed and the values of I~ r
` are calculated. The error of determining ICsr does not exceed +(0.1-0.2)
~ second in this case.
The value of Kpl is determined from seismic logging data and also from mater- -
ials of explosions and earthquakes registered by "Zemlya" stations. The
values of ICP1 are determined from seismi.c logging data as the ratio of stratal
velocities of longitudinal. waves to the stratal velocities of transverse waves
' in each layer of the sedimentary mantle. Based on materials of ~xplosions and
near earthquakes, the values of Kpl are determined by the ratios of the appar-
ent or boundary velocities of P and S waves (vpk/vgk or vpg/vgg), the time
ratios of P and S waves on the hodographs ((TS - TO)/(TP - TO)) a~d the ratios
of the stratal velocities of P and S waves calculated by the vertical hodo-
_ graphs of these waves. The depth for all these graphs is calculated by the
Wiechert-Herglotz-Chibisov method.
Determi:ning the Velocity Characteristics of the Medium in the Focal Zones of.
- Modern Earthquakes
The velocity parameter~ of the media at the focal zones are determined by the ~
. hodographs,and arrival times of direct P and S waves to the recording stations.
The following methods exist in this case: selection of the theoretical model
- of the medium and determination of the veloci.ties by solving a system of three-
dimensional hyperbolas (see Chapter 8).
Selection of the theoretical models of the medium begins almost immediately
upon determination of the focal coordinates (hoch of x,y) by the method of
intersections from hodographs of direct waves compiled previously. Having
selected the location of the focus by the triangle of lack of tie-in, the
theoretical hodograph and model of the medium and consequently the curves
vpsr = f(H) and vgsr = f(H) for which the hodograph was calculated are de-
tsrmined simultaneously.
'I"he second method is,more effective. It permits one, using the stations lo-
cated at different distances from the focus, to deternune the propagation
velocity of the P and S waves in the focal zone. Comparison of curves ~psr
found for local earthquakes when solving a system of three-dimensional
hyperbolas, with spacing of the recording stations at distances of 0-7 and
0-12 km from the focus to curves found for regions contiguous to the focal
zone, by processinq P and S waves from explosions and near earthquakes by the
Wiechert-Herglotz-Chibisov method is presented in Table 10. As can be seen
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Table 10. Mean Velocities of vpsr (in lan/s) Found Upon Processing of
Recordings from Explosions and Local and Near Earthquakes
~ ~ MecTe e xa~erpsCeexrt , 1
ppl4 }~8JIH9H0lt fA871CHHN CTBHANA ~3~~ ~I
il~ aanxcn oz eanqetrrpa St~axee
- H, x~ Bapuea aeY,nerpacesaa
0-7 xY 0-i2 roi _
g~p 2,95 - 3+5
3,25
gr5 3,35 3,i5 - 3+g
4~~ 3~~ 3~3 3,8 3,8
y~5 ~ 3,75 3,5~ 4,0 4,0
5~0 3,85 3,85 4,i . 4,l5
6~0 4,1 3,75 4,2 4,40
4~3 3,g5 4.25
8,5 4'S''
,~~t, 3,85 4,3 ' 4,6
~~5 y,y ~ g,R7 4,4 4,7 -
8'~ 4'5 3,95 4,45 ~
9,0 -
K,ey : .
1. Explosions . -
2. Local earthquakes with different distance of recording stations
- from epicenter
3. Near earthquakes
from the given.comparison, the minimum values are those of.vpsr obtained by
recording stations at distances from 0 to 7 km from the focus. This permits .
one, knowing the locations of the recording stations and focal depths by
which the reduced values of vpsr were found, to limit in space the zone of
reduced values of vpsr and vpPl with an error of 1-2 km.
_ . ~
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Part 3
THE DEEP STRUCTURE OF THE EARTH'S CRUST AND UPPER MANTLE
- OF DIFFERENT GEOTECTONIC ZONES
THE DEEP STRUCTURE OF THE CRYSTALLIN~ MA5S OF THE EARTH'S CRUST AND UPPER
~
MANTLE IN THE RAYONS OF TASHKENT
Dioscow SEYSMICHESKIYE ISSLEDOVANIYA S APPARATUROY "ZEMLYA" in Russian 1977
signed to press 31 Jan 77 pp 202-212
[Chapter 10 from the book "Seysmicheskiye issledovaniya s appa-raturoy
'Zemlya by I. V. Pomerantseva and A. N. Mozzhenko, Izdatel'stvo Nedra,
1,400 copies, 256 pages] _
[Text] The deep structure of the earth's crust and upper mantle was found
as a result of studies with the "Zemlya" stations on the Southeastern Russian
Series of formations in the Azov-Kuban', Pre-Caspian and North German Depres- .
sions and in the rayons of Tashkent.
The volume of studies on the Southeastern Russian Series (with station spac-
- ing of 5-10 km) comprises approximately 600 km of the profiles, that in the
Pre-Caspian Depression comprises 400 km and that in the Azov-Kuban' Depression
comprises 250 km. A total of 540 km of profiles on an area of 400 km2 was de-
veloped in the Pre-Tashkent Depression with station spacing from 50n m to 5 km
and 3,500 km of profiles were developed on an area of 50,000 km2 with station
spacing of 5-6 km within the North German Depression. The number of recordings
_ from local, near and remote earthquakes and explosions registered in all these
regions in presented in Table 7.
The deep structure of the crust and mantle was determined as a result of using .
P, S ancl PS waves registered by "Zemlya" stations from res~te earthquakes
(A = 160�) and explosions = 0-100�) of different distances in the fre-
quency band of 0.5-1U Hz in all the named regions, the velocity characteristics
- of individual layers of the crust and upper mantle were determined and the
~ zones of deep, regional faults of the crust, to part of which are confined the
foci of local earthquakes, were distinguished.
- Conducting the studies with the �Zemlya" device for a number of KMPV and GSZ
- profiles sequentially or simultaneously with these methods made it possible
to compare the derived profiles and the wave patterns by the recordings from
earthquakes and explosions, to de~ermine their divergence and similarity and
to formulate the bases of a rational complex of seismic and seismological
investigations to study the deep structure of the earth's crust and upper
mantle of different geological provinces.
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An idea of the behavior of the interfaces of the crust in the upper mantle _
(H = 100 km) near Tashkent and the behav~or of the interfaces in the crust
to the northeast and southeast from Tashkent w~s obtain~d as a result of.
investigations with the "Zemlya" stations in Tashkent during 1966-1967.
, The velocity characteristics of the crust and mantle to depths of approxi-
mately 110 km are given from data of processing incidental and special. ex-
- plosions ( L~ = 0-45 km) and near earthquakes ( l~ ~ 600 km) . The foc;al zone _
in the crust located under tYie center of Tashkent and the velocity character-
istics of the medium in it were determined from recordings of P and S waves
from aftershocks of the Tashkent earthqualce. The structure of the earth's
crust of the Pre-Tashkent region and adjacent Almalyk, Angren and other ore _
zones was determined during subsequent investigations in 1968-1970 [21].
The structure of the crust near Tashkent and the behavior of the surface of
� the Paleozoic basement in the direction northeast, east and southeast of
Tashkent to its emergence onto the surface are eliminated in this section.
Criteria of the Intrarayon Stratification and Interrayon Correlation of
Interfaces of the Earth's Crust
Until recently the main and in some cases the only criterion for relating
~ the deep seismic boundary to some level of the crust and identification of
it in different regions in the absence of deep boreholes is the value of the
- stratal (or boundary)* velocity. Generalization of the material by the prop-
agation velocities of longitudinal waves in the Soviet Union and in different _
parts of the globe [105] permits stratification of the interfaces of the
_ earth's crust by the values of vpg or vppl in the following manner: a) the
- surface of the folded Paleozoic basement at depths of deposition from 0 to
5 km has a value of vpg which varies from 4.3 to 5.8 km/s; b) the surface
of the crystalline mass of the earth's crust--the Pre-Cambrian basement--
is characterized by values of stratal velacities, equal to 6-6.3 km/s on
the average, at deposition depths of 5-13 km; c) the surface of the basaltic
layer in different regions of the globe has a value of vppl = 6.4-5.8 km/s;
d) the boundary within the basaltic layer, conditionally named the Conrad-I
- surface in some regions of the USSR [41, 42, 103, 105, 110] is characterized -
by vpPl = 7.0-7.3 km/s; e) the boundary intermediate between the Conrad-I
and Mohorovicic Discontinuities, also arbitrarily named Conrad-II, has a value
of vpPl = 7.6-7.8 km/s; and f) the upper part of the mantle (the Mohorovicic
Discontinuity) is determined jointly with the values of vppl. = 8-8.2 km/s;
- g) additional interfaces characterized by ve].ocities of longitudinal waves -
of 8.4 km/s (H ~ 50-60 km), 9 km/s (H = 80-90 km) and so on, were noted in
the earth's rnantle [123, 150] .
*The term "boundary" velocity is conditional since the value of vq for re-
~ fracted waves corresponds to some part of the layer at the depth of maximum
ray penetration. However, individual layers may characterize vg in the
overall regional layout. -
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Table 11. Velocity Profile of Crust tinder Tashkent
~ r~y'tl..
3~InAexC a5 HM~C~ g~Jc I'nn xY
Haaeaw~e cnoe cnof[ 5
(1l i2) ~4~.
~ 3,~i l~7.._~,BI !,9-'l I 0-2,5
OcanowuHii qezon (6) I
I PZl
5,86 I 3,0 I 1,95 2,5--5~5
IIaneoaoHCtcxR ~?y~ta' I pZl ,
~esT ) AR
AR 6,2 I 3,35 1,85 I 5-9,5
Apaen ~8) I I - -
6,4-6,5I 3,65 I 4,75- I9,5-15,5
Cnoi+ c noBr~me~oiz I I-II l,83
cxopocT~o (g) II
I 6 I g~2~g,4 ~ 1,8 I 9,5-21
BwieoHOu (10) II-SI ,
si I i,75 I i6-ZO
6,85-7 I 3,9-4
Baaana~roHU~i~ c,noit (u~ si x~ H
r I
7~4 4~~ ~,75 20-30 -
Cnon rny6fxe IIOBepS- xj-"xII
soc~rx Kospaua-I
(K-I) . (12) xIi ~
7,6-7,8 4,35= l,75 . 30-~
_ ~ IIepa~iu cnoii rny6xce I{ I-~{I . 4,45
noeepr~oc~rnn Hospa-.
ua-l I (K-II) ~ 13 ~ xii '
xa M 7,6-7,8 4,5-4,6 i~7. 38-5f
BTO~ON cnou rny6xte I1- I '
HII, B~plenaee~c ' -
'fOJlbl(O II(1 CHOpOCTHH
- go~ S (14) MI ~
8-8,i ~ 4,7-4,8 i,7
` 3osa nepexoRa ar xo- 11iI-MII �
p~ x xas~t ~15)
MII I 5l-82
8-8,i I 4,7=4,8 ,I . i,7
_ IIepAUti~ caoi~ H xasx~ I Ml-MIII
(1 Fi1 - MIII ~ ~
g,2_8,4 4,8--4,95~ i,7 59--Sf?
B~ropoii, Tpernii g ~e- MIII- . _
Tsep~ cno?i H a~aa- -MIv
Tltlf (17~ M~-M~ .
Mv-M~I -
MvI 1~7 gg_1!0
Ce~w~oa c.noii s~aa- B adaa- 8,8-9 5,2-5?3 .
~ (18) ~9
MvI -
- MvII MVII .
Key : -
1. Name of layer 3. Index of boundary
2. Index of layer 4. km/s
- [Key continued on following page] _
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[Key continued from preceding page]
5. Depth, km 14. Second layer deeper than KII
6. Sedimentary mantle determined only by velocities
7. Paleozoic basement of S waves
8. Archean 15. Transition zone from crust
9. Layer with increased velocity to mantle
10. Waveguide 16. First layer in mantle
11. Basaltic layer 17. Second, third and fourth ,
12. Layer deeper than Conrad-I layers in mantle
discontinuity (K-I) 18. Seventh layer in mantle
13. First layer deeper than 19. In maritle _
Conrad-II discontinuity (K-II)
Stratification and correlation of the crustal interfaces is also carried out _
_ by the values of the strata? velocities. The interfaces determined by PS
waves are compared ta the boundaries of the velocity jumps obtained from P,
S and PS waves for this purpose by the methods described in ChaptPr 7. The
results of the comparisons are presented in Figure 94 and on the depth pro-
files of the North German Depression (see Figures 111 and 112).
The Velocity Boundaries of the Crust and Mantle of the Tashkent Depression
and_Their Geological Stratification
A total of 12 boundaries was determined from data of processing P and S
- waves from explosions and near earthquakes and also PS waves registered by _
- "Zpmlya" stations in the crust and mantle of the Tashkent Depression (Table 11).
Besides the interfaces of the crust enumerated in Table 11, boundaries from -
~ waves alone we're noted from P and S waves at depths of 71.5, 91.4 and 107
k~m (see Figure 70). A waveguide has been noted from experimental material _
' deeper than the mI boundary. However, it was not possible to find the dis-
tribution of vPpl and vSpl in it.
The Behavior of the Interfaces of the Earth's Crust and Mantle Under Tashkent
- A number of charts and disgrams of the depth distribution was compiled for
the following interfaces o.f the earth's crust as a result of the studies of _
- 1966-1967 [150] by means of 15 recording s~ations on an area of 900 km2:
surfaces of the Paleozoic (Figures 107 and 108) and Archean basements, the
. roof and bottom of the layer with increased velocity values (see Figure 107),
the surface of the basaltic laver (see Figure 64) and the Conrad-I and
Conrad-II discontinuities and the transition zone from the crust to the
- mantle (Figure 109).
The surface'of the Paleozoic basement, Ttie surface of the Paleozoic basement
- has a complex ].ateral structure under Tashkent (see Figure 108). On the
whole, the entire basement under Tashkent can be divided into three large
- zones: the Chinabad projection (Tashkent rampart), the Tashkent depression -
215
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a b 4t~p fr/7 10 y~ 1 11 ~ R,K~"
0 p~ -
pi~ S'~
I ~1 ~s ~-AR: ~ `~C'+Il
= 10 ~
~ IIs, + 1 ~ , s �
{6I ~~~~A~.~~ i
pp +s---~'---#---'-~~. ~f
s- ~~BS
~
Kt+ ~1 '~~y~ K~
D[ * + ~ ~ID
~
d0 KTP ~ -�------~6-7,d ~
40 { a ~1---�'� ~ + +
- ;1' ~ ` 4--K~
, ~+m ; M +
SO I
i~MII 8-$7 ~
~~G'L~Ull111 ~1/!1lLil/!1
Mp
15/7 1 Q1 Q3 ~4 ~5 ~6 ~7 S,B6 ~
N,w~
b 1p 2p 4 30 40 R,nM
0 P~
5,86
~ 1 --s'-- ~i 1'~{+f,'
r-~.~4 ~-II
~ j' ~ ? 1 6 , _
2~ ~ i '~i-~ ~ ?
�a~ ~
, � � S f~7
. . ~_3 ~
~ ' ~ r,_ � , �-t-�.+,.~y ~y I
30 ~ ~ fie~'e-D[
1 K
� ~ '~,s-~a
� ~
~i0 + i ' +
+
mmrl~l!!/T!/T~/~j~j ~ *.m77f1r~7 W~
~i,sl~Mt ~ ~lL1111111,~[;ii...iiii..lii.3i.i.i~.~..,
, SO ~ .,1'` + ~ : *-....`Mn
, I,~d 11lf~ 8-8,1 .
H,Kr
Figure 107. Profiles of tkie Earth's Crust Under Tashkent from
Profiles 0-0 (a) and IV-IV (b) (See Figure 108):
~ P21--surface of Paleozoic basement; AR--surface of presumably the
Archean basement; I and II--roof and bottom, rPSPectively, of layer _
with increased velocity; BS--surface of basaltic layer; KI--Conrad-I _
discontinuity; III--boundary deeper than Conrad-I discontinuity; _
KIIZp--Conrad-II discontinuity by P wave; KIIS--Conrad-II surface
by;;s wave; MIMII--roof and bottom, respectively, of transition zone
[Caption continued on following page] -
. 216
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[Caption continued from preceding page]
crust to mantle; MIII--section of boundary in upper mantle; 1-- -
locations of recording stations with numbers of individual sta-
tions (in the numerator) and stopovers (in denominator); 2--
points of depths from data of composite PS waves; 3--epicenters
of aftershocks of Tashkent earthquake located on line of profile;
4--epicenters of aftershocks of Tashkent earthquake located~at
distance up to 2 km from line of profile; 5--sections of boundaries
with sharp attentuation of PS waves; 6--faults from data of PS waves;
7--region of low values of velocities of longitudinal P waves (up
to 4.3 km/s) and coefficient K(up to 1.61) in the focal zone;
8--value of vpPl in km/s
itseif and the zone along the course of the Chirchik River. The first zone
encompasses the northeastern part of Tashkent. It is characterized in the
_ north by the most shallow absolute depths* of deposition of Paleozoic rock _
(700 m). Submergence of the basement from 700 m to 1.95-2.0 km is noted from -
the north-northeast to the south-southwest within this zone. The second zone--
the Tashkent depression itself--c~ccupies; the southwestern part of Tashkent.
It is characterized by deeper and smooth deposition of the surface of Paleo-
zoic rock. The absolute depths to the surface of the basement fluctuate within
very small limits--from 1.95 to 2 km. The third zone, located in the east and
southeast of Tashkent, is characterized by a more complex structure (see
. Figure 108). All the enumerated zones are joined to each other by a series
" of faults. The latter converge under the central part of the city where a
northeastern block of increased deposition of the basement surface is located
at an absolute depth of 1.25 km. A second, more submerged block (H = 1.8 km)
~ is observed to the southwest of it. The blocks are separated by a depression -
- (H ~ 2 km) inside which the isolin~ with depth of more than 2.4 km is formed.
This is the most submerged zone under the center of the city and is a seemingly
complex assembly of all the fault zones which separate the tectonic structures.
The surface of the presumably Archean basement. This surface(vpPl = 6.2 km/s)
has been determined under Tashkent only in some locations. A limited amount -
of data probably determined by the sharpness of the interface do not make it
possible to compile a chart,. One can only note that this boundary is located
at depths of 6-8 km (see Figure 107}.
- The roof and bottom of the layer with increased velocity values. The bottom
of a lyer with increased velocity is traced more clearly and universally in
the:_region of Tashkent and its roof is also determined in some sections (see
Figur~ 107). The traced boundaries are deposited concordantly everywhere.
The thickness of a layer is an average of 2 km. The same structural elements
as on the surface of the Paleozoic foundation: the Chinabad outcrop, the
_ ~
*
The depth marks are given from sea level,; ~
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Tashkent depression and the zone along the course of the Chirchik River,
have been determined along the bottom of the ~ayer. The indicated zones
are separated by fault systems which coincide with faults along the surface
of Paleozoic rock.
y 0
. ~';~~a~ _
- ~ ~~i IY
~ ~ ~~~A_ ~ o^
i L/~ , be
~ .~f"~ ~ ,,4ti~ _
, , ~ . ~i
, Ti,, -w ~ ~ ~ ~ ~
i i
~i~ ~'L~,;`^
~Z c ~~ti~
~ ? ~ .
~ !0
6 . ~ . ~
, ~
_ Z . a ~ 1^
_ I`~ B ~
~
_ ~ / ~S ~16
~ ~ ~~a ~ i-
~ ~
.1.ti .ti ~ ) O ~ .
/ ~
,ti`6 ~,8-~4~ ~ i' ~
6 , / ,'t =7,~
/
~ ~ .i~ -Z2
~ /
~ .
_ i
- ib~8 ~ ---s Z l~-~3 ~ 5 ~ 6 ,
_ Figure 108. Relief Map of Surface of Paleozoic Basement Under
Tashkent (Compiled by'I. V. Pomerantseva and L. I.
Kagalova):
A~--Chinabad outcrop; B--Tashkent depression; C--Chirchik zone;
1--individual recording stations of 1966 (a), 1967 (b) and 1968
(c) (the nwmber of the station is in the numerator and the number _
of the stopover is in the denominator); 2--ce~tain (a) and less
certain (b) isolines along the surface of the Paleozoic basement;
3--fault zones (a) and lines (b) from data of "Zemlya" stations;
4--profiles; 5--epicenters of aftershocks of Tashkent earthquake
of 26 April 1956 from data of "Zemlya" stations; 6--regions where
reduced values of stratal velocities of P waves up to 4.3 km/s -
and of coefficient K(1.61) are observed
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The most shallow depths to the bottom of the layer (9.5-10 km) are noted in
the northeast of the area of. study--under the Tashkent rampart--and the
deepest depths (12-14.5 lan) are noted within the Tashkent depression itself
_ and along the course of the Chirchik River. Submergence of the bottom of
the layer with increased velocity occurs along the fault system of north-
_ westerly strike (see Figure 107). A small downwarp with amplitude up to -
1.5 km is located under the center of the city, which is correlated with
the closed depression within the canyon along Paleozoic rock.
The surface of the basaltic layer. This surface (vppl = 6.8 km/s) is in-
versely deposited compared to the boundaries enumerated above. ~'he most
submerged region (up to 20-20.5 km) is located under the Chinabad zone (see _
Figure 64). The most uplifted part (up to 16 km) is noted in the southeastern
part of Tashkent in the region of the course of the Chirc;hik River. The
Tashkent depression is characterized by intermediate depths of 1%-18 km. A,
downwarp up to 21 km deep has been determined under the center of the city -
with slight displacement toward the northeast (see Figure 64).
The Conrad-I Discontinuity. The Chinabad zone (20-22 km) and the zone of ' -
the Tashkent depression (24 km) is distinguished along the Conrad-I dis-
continuity. The most shallow depth markers along this boundary are con-
fined to the region of the course of the Chirchik River (18-20 km) and to ,
the northwesterly part of Tashkent (20 km). An uplifted zone (up to 21 km)
- is noted under the center of Tashkent.
The Conrad-II Discontinuity. This surface has been determined both by the
S wave (vgpl = 4.5-4.6 km/s) and by the P wave (vppl = 7.4-7.7 lan/s). Ex-
, tended and sustained boundaries terminate in the crust deeper ~han this
- surface (see Figure 107). The 3epths to this boundary vary from 30 to 34 km.
The transition zone from the crust to the mantle. Either the roof (MI) or
the bottom (MII) is distinguished in the transition zone from the crust to
_ the mantle (vppl = 8.0-8.2 km/s) (see Figures 107 and 109). The joint region
~ of tracing the MI and MII boundaries is very insignificant. The roof o� the
transition zone (MI) is located at depths from ~5 to 47-48 km and the bottom
- of the transition zone (MII) is characterized by depths of 49-53 km. The _
bottom of the zone is easily distinguished in the northwestern and southwestern
parts of the city and the roof is distinguished mainly in the southeastern and
- northeastern parts. The boundary of the northwestern and southeastern zones
has a northeasterly strike and passes through the epicentral zone under the
center of the city, approximately in the directi~n of profile IV-TV.
The interfaces in the mantle. The boundaries are located at depths of 60,
70, 80 and 90-100 km. The boundaries in the mantle are essentially undeter-
_ ~ mined directly under Tashkent, especially under its center, since the exchange
points with the spacing of the stations used were located southwesterly of ~
- Tashkent due to the large drifts. The values of depths vary from 59 to 64 km
along the MIII boundary (H = 60 km). The zone of the southwesterly-north- -
easterly strike with relatively increased deposition of the boundary (up to
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IS ~ I S~ I ~ ~ ~ -
5~ 49 ~
494 / ~ Z 51
4 2~ SO I ,
7_4 S z
s~
y47'~I 5JI52 46 ~ f~
ry ~ 49 ' ~ 57 qy~S4
51 a~
-y, 49 k7
6~4 k7 r-
~S7'~
51 >4~
I ~ Ip 47 -Sl ~ ~ ~47
~ I s I Sd 54 Sz 5i~47 4E r~--48-
55 s2 S,p-54 4 ~9 4~52 r/~o
SD~ ~ ~ 0 9-5~ ,~s
I
S Sy ~ 15/`1 5u y`~
- ys 48 -k5
Si ~ ~47~~yo.-3D-_
~5 ~8 _5 ,
47-
45 5D 4;
47
4 y6-Sl
45 y.y
SO ~4 47 k7
_ I ~ ~~y~y 46
k5'
\ 5 ~9 49
51 ~
4 \~~s ~
- 54 5~.~ 71,50~ y9
5
I ~ \ -
~ Z 5 53
`52 S~ \46 I
I \ 50 49
1
,14f7 1 ~2 ~3 ~4 ,1 5
- Figure 109. Relief Diagram of Transition Zone from Crust to Mantle
Under Tashkent:
1--locations of "Zemlya" recording stations (the number of the
station is in the numerator and the number of the stopover is in
the denominator); 2 and 3--depths, in km, to the bottom and roof -
of the transition zone, respectively, from the crust to the mantle
with directions to the recording stations; 4--profiles of distribu-
tion of MI and MII tracing zones; 5--profile IV-IV passing through
~ the epicentral zone (see Figure 108) .
. 56 km), which surrounds the city from the east and southeast, is distinguished
in the northwestern part of the area.
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Even fewer exchange points than along the MIII boundary have been found
' along boundaries MIV-MVI. It is difficult to make any judgment about the
" relief of these boundaries from available material. One can only determine
! the range of depths at which these boundaries are distinguished: 67-75 km
for MIV, 77-81 km for MV and 86-100 km for MVI.
Surface Structure af the Paleozoic Basement to the East and Southeast of
Tashkent
Investigations with 15 "Zemlya" stations, conducted in 1968 and partially in -
1969, made it possible to compile a schematic chart of depths to the surface
of the Paleozoic basement to the east and southeast of Tashkent (Figure 110). -
This chart is easily tied in to the chart of the Paleozoic surface under Tash-
kent and permits one to determine the relationship of the deep structure of
the Paleozoic basement of Tashkent and the mountain systems surrounding it -
on the east and southeast. The depth markers to the Paleozoic basemen~ vary `
gradually from 0.3 to 3.2 km. The strike of the isolines is mainly northeast-
~ erly and is seemingly controlled by the location of the boundary of the emerg- -
ence of the Paleozoic basement to the earth's suzface. A gradual monoclinal
submergence of the Paleozoic surface in a north~~esterly direction, from 300 m
to 2.5 km, is noted. A sharp rise to depths of 1.6 km is further observed at
a distance of 4-6 km.
The Seismic Activity of the Territory of Study and its Relationship to the
Deep Structure
The greatest seismic activity of the Tashkent area was observed during April-
September 1966. Approximately 305 aftershocks of the Tashkent earthquake of
1966 were registered by "Zemlya" stations during this period. A graph of the -
distribution of earthquakes in time and their depths are presented in [110].
To establish the regularities of displacement of the foci of the aftershocks
of the Tashkent earthquake, the latter were applied to a chart along the surface
of the Paleozoic basement (see Figure 108) and the depth profiles of the crust
(see Figure 107). The epicenters of the earthquake aftershocks are grouped on
the chart in a narrow local zone in the central part of Tashkent. The area
occupied by the epicenters does not exceed 2 X 3 km. The foci are located at
depths from 3 to 9 km (see Figure 107) seemingly along the plane inclined toward
the vert}cal at an angle of 15� and having a northwesterly strike. The epicen-
tral zone along the surface of the crystalline rock is confined to sections of
joining of the three large blocks of the crust determined from data of "Zemlya"
stations under Tashkent: Chinabad, Tashkent and Chirchik. The propagation
velocity of longitudinal waves in the crystalline mass of the crust of the
epicentral zone at depths from 3 to 9 km is equal to 4.3-4.5 km/s and Kpl = 1.61.
The velocity in the Paleozoic basement is equal to 5.8-6 km/s and Kpl = 1.73 in
- the remaining area of Tashkent and its suburbs.
Comparison of the foci of the aftershocks of the Tashkent earthquake of
26 April 1966 to the deep structure of the crust shows that the foci are lo-
cated at the points of manifestation of active modern tectonic movements and
221 ~
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~ ~ Q m S l \.1 ~ ~ ~ ~tA~
~ - \ \ J~s /
~.-0.6. ~ ~ ,m -
~ ~ ~ % ~m ```c ~
i Z ~ ~ /ii
i i Mn ~~9~ ~,ct~'
/
/ ~ ~tt ~O 6,,, ,n,,,~
~3 ~ \ ~ �,/iL.~~o~~ j~~` U
' .
~ O ca" ~ /
X } ~ ~ � \ v~~,`~,^/ n
~1\ J~ ti ~
O
~ } A'1.~
'l � , ~ i ~ ;~Q~ `'l.~
~ ~ ~6 17~1,~~;..~
. } ~w \ I ` ~ �
? ' '
f % ~rC~ / ~
+ ~ ~.i, 0~~ o,~4~~
k~~
' J~/ ~ / ~ ~`�0'~ ~ ~~c~-"
~c~r~~ i. ~,tio,~`~' � ~ ~j~l�
~ ~~m ~Po
~ i~~ ~ ~ i~ .
.
~ ~~~,f~~ ~00~~ � -
~ o o ~ ~ ~ti� , ~ ~m \ -
. ~ ~
~ ~ q9'
~
. ~
O ~j /m,p'~/ii~~// ~ \ .
4 - ~
o~ ~ "',s _'i
a 0/ L� ~ ~i. ,~---o,s ~
_ � ` ~J 11 ~ ~ 0~6
~ ~ �1m , ~ m
~0~~ ~ / ~ ~~m m ~~~,8
~ ~ � / ~ ~j ` ~
1
0 i /
.ti.�- 0,a~' o~
Figure 110. Relief Chart of Surface of Paleozoic Basement Under
Tashkent and Within Its Southeastern Framework (Com-
piled by I. V. Pomerantseva and E. K. Kostrova):
1--isolines (in ]an) from data of I. V. Pomerantseva and L. I.
Kagalova under Tashkent, confident (a) and less confident (b);
2--isolines (in km) from data of I. V. Pomerantseva southeast of
Tashkent; 3--isolines (in km) from data of B. B. Tal'-Virskiy;
4--isolines (in km) from KMPV data; 5--points where the values of
depths along the PS waves were found by different authors: a--
data of I. V. Pomerantseva and L. I. Kagalova; b--data of L. S. ~
Shumilina; c--data of Ye. M. Butovskaya and T. M. Gol'tseva; -
6--boundary of outcrops of Paleozoic basement to earth's surface;
- 7--fault zones from data of B. B. Tal'-Virskiy; 8--epicentral zone
~ of Tashkent earthquake of 26 April 1966.
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_ are confined to the faults of the crust having significantly distinct
structure and reduced propagation velocities of elastic longitudinal waves
with reduced coefficient K. The epicentral zone is located above the deep
zone of the faults which touch the entire crust and upper mantle (see
Figure 107). -
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THE DEEP STF:UCTURE OF THE EARTH' S CRUST OF THE NORTH ~Eg~.~N DEPRESSION
Moscow SEYSMICHESKIYE ISSLEDOVANIYA S APPARATUROY "ZEMLYA" in Russian
1977 signed to press 31 Jan 1977 pp 212-223
[Chapter 11 from the book "Seysmicheskiye issledovaniya s apparaturoy 'Zemlya"'
by I. V. Pomerantseva and A. N. Mozzhenko, Izdatel'stvo Nedra,1,400 copies
256 pages]
[Text] Studies were carried out with the "Zemlya" device in the German
Democratic Republic in two stages. Experimental studies to determine the
possibilities of studying the structure of the earth's crust of the German
Democratic Republic by using these stations were carried out during the first
stage in 1968. The conditions for reception of seismic signals were deter-
mined, the band of registered frequencies was established, the seasonal
nature of the microseism background was investigated, and the technical- -
methadical procedures for conducting field investigations with respect to
~ the conditions ot the German Democratic Republic and so on were developed
during the studies. It was established that the effect of the environment
during the corresponding method and technique of the investigations could be
reduced to a minimum (see Chapter 4).
Based on the results of experimental investigations during the second stage,
investigations with the "Zemlya" device over the entire northern part of the
German Democratic Republic were carried out from March 1969 through September
1970. A total of 3,500 km of profiles on an area of approximately 50,000 km2
was completed and 946 remote earthquakes and 118 special explosions were
registered during this period by using 25 "Zemlya" recording stations. Time
profiles of the ea.rth's crust on all the profiles were obtained from remote
earthquakes from P and PS waves as a result of the field operations. Systems _
of direct and counter hodographs of P and,S waves were obtained in addition
to the time profiles 2,200 long.
Complex processing of the first arrivals of P and S waves from explosions and
of P and PS waves from remote earthquakes made it possible to construct the
depth charts and profiles of the crust of the North German Depression over
the entire area and also to find the velocity models of the crust and to com-
pile charts of distribution of the stratal veloci.ties of P waves and coefficient
K of the lower sedimentary mantle and the upper part of the crt~stalline mass
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- of the earth's crust, The mean and stratal velocity distribution curves of P ~
and S waves with depth were found for the entire crust.
The velocity Interfaces of the Earth's Crust and Their Stratification
Data on the propagation velocities of longitudinal waves in the crystalline
mass of the crust wexe available in limited numbers toward the beginning of
operations with the "Zemlya" stations within the North German Depression.
Experimental data on the propagation velocities of transverse waves in the
crystalline part of the crust are generally absent. A total of 11 layers
was distinguished in the mass of the earth's crust from data of explosions
and earthquakes registered by "Zemlya" stations; (Table 12). -
- Processing the composite PS waves from remote earthquakes made it possible
~ to significantly refine the depths and to construct the relief of the inter-
face of the crust, to separate the lows of the sedimentary layer with the
surface of the Variscian basement and to determine the transition zone from -
the crust to the mantle and the boundaries within the mantle.
'I'he surface of the Variscian basement was confirmed by data of five boreholes.
Taking into account the general geological concepts about the structure of -
the North German Depression [171] and its position between the roofs of the
Variscian and Pre-Cambrian basements, the surface of the Caledonian basement
was determined. The stratographic position of this boundary was confirmed
by superdeep drilling 2.5 years after completion of the investigations. The
surface of the Variscides was confirmed in two different locations by two
boreholes drilled three years after completion of the investigations. The
interfaces within the crust were stratified by values of vpPl according to
the criteria outlined in Chapter 10. `
- Some Data on the Nature of Propagation and the Structural Shapes of the
Interfaces of the Earth's Crust
The same crustal interfaces as for P and S waves from explosions were deter-
mined as a result of processing PS waves from remote earthquakes within the
North German Depression. The clearest, most marked and most easily traced
of them are the surfaces of the Caledonian (PZ1) and Pre-Cambrian (PR + AR)
basements and the surfaces of the basaltic layer (BI) itself and the layers
of the Conrad-I (KI) and Mohorovicic (MI and MII) discontinuities. The sur-
- face of the Variscian basement (PZ2), the roof of the transition zone from
the granitic to the basaltic layer (Lp) and the boundaries in the basaltic _
layer (BII and KII) were less clearly traced. A surface coinciding in depths
to horizon Z(Zechstein), was traced almost everywhere in the sedimentary
mantlE. Tuff deposits of rotligendes (RE) and also the roof (J') and bottom
(J") of stratal effusives in the lows of the sedimentary mantle were determined
- in some regions. Effusive-intrusive formations (J) above the Pre-Cambrian were
determi.ned within the Eastern Elbe gravitational and magnetic maximums (the
Prignitskiy block) and in the northeastern area of the investigation. Struc-
tural charts were constructed for all the levels of the crystalline mass of
the earth's crust.
225
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