JPRS ID: 9129 USSR REPORT EARTH SCIENCES

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• Content Type: REPORTS

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JPRS L/9129
6 June 1980 .
- U SS R Re ort
~
EARTH SCIENCES
t~OU~ 5/80)
FBIS FOREIGN BROADCA~T IN~'ORMATION SERVICE
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' JPRS L/9129
6 June 1980
~USSR REPORT
EARTH SCIENCES
(FOUO 5/80)
. CON TENTS .
METEOROLOGY
, Complex Active-Passive Sounding ~f Cluud Cover 1
Some Posaibilitiea of Using the Synthetic Apertures Method
for Obaerving Meteorolagical Targets 11
OCSANOG~APHY
Observations of Fronta in the Polymode Area 18
Study of Temperature Fluctuations With Inertial and Diurnal
Periode 22
Separation of Semidiurnal Temperature Fluctuations Determined
- by the Barotropic Tide and Internal Waves 28
Study of the Diurnal and Semi-Diurnal Temperature Fluctuations. 33
S~udy of Abyssal Teffiperature and Density Structure and the
- Velocity Profiles in an Ant~cyclonic Eddy 47
Polymode International Large-Sca1e Ocean Experiment............ 52
Study of the Train Structure of Short-Period Temperature
Fluctuationa 59
Phase Radiogeodetic Systems for Marine Research 65
Articles on Theory and Prediction vf Tsunamis 68
TERRESTRIAL GEOPHYSICS
&eismogec+logy of the Mongolian-Okhotsk Lineament (Eastern
Flank~.....~..........+ 72
Holography and Optical I~ata Processing in Geology and
Geophysica 7S
' 3� [III - USSR - 21K S&T FOUO] -
L~~1D HL~L~T/tT*? ��.~.r+
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.
Ssismotectonic Deformation in the Garm Region 79
_ PHYSICS OF THE ATMOSPHERE
Poseibility of Stimulation of Turbulence in the Polar Magnet-
osphere: First Resulte of 'Mini-I' 108
Ionospheric Effecta in a Geophyaical Experiment With a
_ ' Powerful MI~-Generator ..............o..................... 120
Polarization of Artificial VLF Emisaions in the Auroral Zone 129
Reaults of Observations Carried Out During Vertical
Sounding of the Region of the High-Latitude Ionosphere
Disturbed by Powerful Radioemission 134
- 'Araks' Experiment. Da~pler Radar Measurements of the _
Effects of In3ection of an Artificial Electron Beam into _
the Northern Aemisphere Ionosphere 141
Radar Observations of Dense Ionization Created by an
Artificial Electron Beam 159
Surface Radiophysical Obaervations of the Leakage of
Particles in a Magnetically Con~ugate Region in the
Northern~ Hemisphere in the Soviet-French 'Araks'
Experiment 171
, ~
- b -
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METEOROLOGY -
COI~LEX ACTIVE-~ASSIVE SOUNDING OF CLOUD COVER
' L~sningrad TRUDY GLAVNOY GEOFIZICHESKOY OBSERVAT~JRII: METODY AKTI~INOY I
; PASSIVNOY RADIOLOKATSII V 1~TEOROLOGII No 411, 1978 pp 3-12
[AIt1C1Fi by G. G. Sh~L`hu1~C~.I1~ L. P. BObyleV ~ Y8. K. I1' in, A. I. Lyr88hk0 ~ ~
P1. F. Mikhaylov, N. I. Novozhilov, N. D. $opova]
[Text] The methoda of active and pasaive radar aounding.are being used suc- -
ceasfully to solve an entire sei~es of ineteorological probleme [7]..-Both methods
taken separately have their disadvantages and advantages, which ie alao de-
termined by the specif ic nature of the problem at hand. Thus, when provid-
ing etorm warnings the beat results are obtained by the active radar method
at the eaaie time as when determining temperature and moisture profilea pre-
fereace is given to the radiothermal location method. The fact that none of -
the remote methods of c:lectromagnetic souading provides sufficiently complete
information about the physical state of the cloud atmosphere indicatea the
neceseity for complex utilization of them. When eatimating the parametera
of the cloud atmoapr~ere the characteriatics of the reflected signal and the
i natural thermal radio wavelength emiasion of the investigated target muat be
~ obtained eynchronouely.
I
! The complex utilization of the active-passive radar method appeare to be the
moet proepective for diagnoeing the state of cloud aystema in order to esti-
mate their euitability for the use of artificial means of regulating preci-
pitation. It ie expedieat to uae the eame complex method also to monitor
the reaults of the indicated active inputs.
To etudy the poeaibility of solving the above-enumerated problema, the GGO
[Main Geophyaica Observatory] hae developed a model of an active-passive
radar based on the I~LL-2. In addition, a procedure has been developed for -
cletermining the parameters of the cloud atmoaphere, and it has been checked -
out experimentally under field conditions.
_ Active-Paasive Radar Complex
_ For complete matching of the thermal ~ocation and radar information in time
and space, simultaneoua operation of a radiometer and radar on one an~enna
- ia neceasary. Thie operation i~ poseible or.ly under the condition of solving
1
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the problem of electromagnetic compatibili.ty inasmuch ae the radiometer ie a
very highly aenaitive inatrument. and to eliminate interf erence from the
powerful pul8ee of an active radar, decoupling of less than 120 decibels is
required between them [4]. Another aepect of joint operation of the radio-
~ meter and radar ie pref erenca for a technical design whfch will not require
eignificant alterations in either the radiometer or radar circuitry.
To the antenna 3
f 2
3
~ ~ ~
6
4
Figure 1. Block dia~ram of an active-passive radar complex
operating on a= 3.2 cm. 1-- diacharger (R), 2-- N4tL
noiee generator (GSh), 3-- 1~tI. receiver, 4-- radiometer
(RM)~ 5-- pin I attenuator, 6-- pin III attenuator, 7--
commutator (K). .
The Main Geophysics Observatory has developed a~oint active-passive complex
baeed on the atandard MRL-2 mobile radar and a modulation radiometer opera-
ting on a wavelength of a~ 3.2 cm with a senaitivity ZK (si~? for a time
conatant of ~ 1 aec. The design of the complex follows.
~ A superhigh frequency commutator (K) based on pin-diodea on a double T-bridge .
(see Figure 1) is built in between the noiae generator (GSh) of the MRL-2
radar and its receiver input. Fram one of the outputs of this commutator
the aignal goea to the input o� the IrIItL-2 receiver; from the other output it
goea to the input of the radiometer. The modulation frequency of the radio-
m~eter is equal to the seading frequency of the radar. The reference voltage
of the radiometer is generated by a special generator which is synchronized
by the MRL-2 atart pulse and will permit a reference voltage phase ahift.
The commutator (K) is controlled by the reference voltage of the radiometer.
The reference voltage phase is established in auch a way that by the time
tl (eee Figure 2) directly before the beginning of the pulse of the MRL
noiee generator, tt~e radiometer input will be closed. In this case, the
pin II attenuator ie closed, and the signal from the antenna goe8 through
the commutator (K) to t he input of the MRL receiver, insuring normal.function-
ing of the MR;~. Here the decoupling of the ra3iometer and the I~IItL is de-
fined as the aum of the attenuations of the pin II attenuator and the inter- -
_ nal superhigh frequency commutator of the radiometer. ~ao of the type AP-5
- pin-diodes, which are seriee included, and each of which in~roducea an at-
tenuation of 40 decibels, are uaed as the pin II attenuator. The attenuation
2
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introduced by the internal superhigh frequency commutator of the radiometer
will be 30 decibels; conaequently, the total decoupling of the radiometer
and the I~IItL with respect to the wave guide channel will be 110 decibels.
The additional decoupling of the radiometer and the MRL ie achieved by eelec-
ting the frequancy characterietice of the channele of the intermediate fre-
quoncy amplifier of the radiomet~sr and the I~fRL in accordance with the recom-
mendationa of [4], and it amounts to about 30 decibele. Thus, the total de-
coupling will be about 140 decihels, which, within the 1imi~s of accuracy of
the measurementa, completely excludes the effe~t of the MRL on the radiometer.
/
i Z
! i T J i f J
~ f ~ � -
~ ur
tr t: c
Figure 2. Diagram of the operation of the active-passive
complex. I-- pin i valt~ge diagram, II pin II voltage
diagram, III MRL and radiometer signal; 1-- signal of
~ the MRL noise generator, 2-- IrL.RL pulse, 3-- echo.
At the time t2(t2 - tl =(1/2)T, where T is the time between the two pulses
of the MRL transmitter) the pin II attenuator opPns, connecting the radiome-
ter input to the antenna of the complex. In this case ~he atr~nuator pin I
closes. Ttne time t2 corresponds to the MRI,-2 range of 9~~ km where the echo
is absent during operation of the ccmplex ~.n the near zone. Here the decoup-
ling decreasea to 30 decibels, but in view of the abaence of the MRL echo, this
is ent~rely adequate.
_ In order to eliminate t�e influence oi the MRL diacharger (R) in the preioni-
zation state on the Lac?iomPter, inatead of a dc voltage of 700 volts, a 7~:0
- volt meander is fed 'co the discharger which coincides with respect to phase
with the control voltage Upin II (see Figure 2).
This operating mode o� the complex insurea normal functioning of the modula-
tion radiomet~r ~nd the MF~L-2 with reduction of the range of the latter to
90 km.
_ The advantagea of the d~scribed complex are the following:
1) a high degree of decoupling of t~ie radiometer and the MRL;
2) simplicity of atructural d~:~ign;
3
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3) the poasibility of using any radiometer in the three-centimeter range in
the complex.
The deficiencies must in~lude the followi.ng:
1) large losses in the wave $uide channel of the I~tL fro~ the antenna to the
input of, the receiver (~a.5 decibel8), which leade to a noticeable decrease
in the actual eenaitivity of the r~diometer;
2) high requiremer~ta on the phase stability of the reference voltage of the
radiometer; ~
3) reduction of the MRL range to 90 km (the latter directly when, operating in the
near zone).
Estimation of the Water Reserve and the Water Content Profile of the Cloud
Ueing the Active-Passive Radar Complex
By using an active-passive radar comp~ex operating on a wavelength of a=
~ 3.2 cm, it ia posaible to eatimate both the water reaerve of the cloud and
the water content diatribution in it in the direction of the maximum of the
antenna radiation pattern. In order to determine the water reaerve of $
cloud during mea8u~ements of the radiothermal emisaion on one wavelength it
ia poasible to use the method of radio brightness contrast. The radio-
brightneas contraat [1] is defined as the diff erence of the radio brightnese
' temperature of the cloud atmosphere at the zenith angle 8 and the radio-
brightness.temper~rure of the same atmoaphere without considering the clouds.
~t is possible to measure this contrast directly only by using the radiome-
ter, scanning by the antenna at a fixed zenith angle from the cloud to the
section of clear aky. However, this doea not always appear posaible.
Therefore in the given paper the radio brightness temperature of the pure
atmoaphere was calculated by the radia sounding data (the radio sounding
station ia located along side the radiameasuring test area).
The radiobrightness contrast is related to the water reserve of the clouds by
a correlatione In order to find thia correlation, model calculations were
performad on the BESM-6 computer. Madels investigated in reference [3] were
taken as the models of the cloud atmosphere. These models describe the real
~ atmoaphere of the northwestern part of r.he European Territory of the USSR.
Data files on the presaure, temperature and humidity prof iles obtained using
radiosounding in Voyeykovo in the summer are used for the calculations. Each _
element of the given files (each epecifi.c situation of the~cloud atmosphere)
was randomly asaigned values of the altitudes of the low~r and upper boun-
c~aries of the cloud layer and alao its water content (water content within
the li~its of the cloud layer was censidered constant). The indicated pa-
rameters and also the water reaerve of the cloud were caiculated by the
formulas: ~
~nn=zn-}-S,o~� . (1)
4
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Zs a ~N ~ `sl,ZM~ ~2~
. Z. _ -I- Sa aZ~, (3)
w a ~~Z~ - ZM~f /4~
\
where w ia the water content, g/m3; ZH, 2B are the altitudes of the lower and
upper cloud boundaries, km; W ie the water reserve, kg/m2. The bar over the
symbol deaotea average values, and the letter 6 denotes the mean square de- -
viatione. The avPrage values and the mean aquare deviations of tha cloud
cover garametere were aelected ia accordance with the type of cloud cover
~3] ~rhich was obaerved f or the given case of radio aounding. In formulas
(1)-(3), S1, S2 and S3 denote the c}uasir~ndom numbers distributed according
to a raormal law. In order to obtain thea, a random number generator was
_ used from the ].ibrary of atandard programs for the BE~M-6 computer.
The calculation of the specific absorption coefficient waich is needed for
calculating the radiobrightneae temperature was made using the procedure
described in reference [2].
The radiobrightnesa contrast as a function of the water reserve of the clouda -
(in the vertical directioa) for a= 3.2 ~m wAS calculated for 4 values of the
zezith angle: 6 a 70, 80, 85 and 89� {without considering refraction). This
raage of angles corresponde to the range of operation of the active-passive
complex. As was noted, the correlation between W and ~Tbright is linear.
Since our problem is estimation of W by the measured values of the contrast
~Tbright~e~~' the relation bezween the given values ig conveniently found in
t~e f urm
. 5
_ W = (~�cp) a TA(A), ~ ( )
(a)
~
= ICey: a. bright
where ~ is the regresaion coeff icient, and Q~ ia the mean square deviation
of thia coefficient. The values of ~ and Q~ found by the 3.east squares
method are pr~aented in Table 1. In order to have the possibility of estima-
ting the water reserve with respect to the contrast measurPd st any angle
from the investigated range it ie necessary to know the coeffici~ent c~ for all
valuea of A. The dependence of ~ on 6 is linear. Consequently,
~=~i~-~aA.- ~6~ ~
_ It ie easy to f~nc'. valuea of ~ and
1 ~2:
_ ~1 ~ 0,3436; _ -0,0038. ~
. (%1
5 -
~nv n~TrTeT Trer. n*nv
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Fina~ly,
W = [0,3436 - 0,~038 9]A TA(9). ~8~
It is neceseary to note that in the given case we have in mind the wat~r re- ~
serve of tbe cloud in the vertical direction. In order to find the wat~r
reserve of a~ cloud along the directioa of the maximum of the radi~ation
pattern of the antenna, it is necessary to multiply the vertical water re-
aerve by sec A . -
In order to restore the water content profile in the cloud it is possible to
use the value of the water reae'rve obtained by the radiometer and the radar
reflectivity profile obtained ueing the MRL [5]. The initial poaition is the
lcaown relatior_ between radar reflectivity and the water content [6]:
Z = Aw�, ( 9 ) -
where A and b are the unkaowa parameters. The parameter b can var.y.�from 1 ,
to 2[6]. In reference [6] it is recnmmended that a value of b= 2 be ae-
- lected f or the cumulonimbus clouds which are the object of investigation of
this paper. flence,
. YZ ~m, ( lp)
,Knowing the reflectivity profile in the direction it is possible to inte-
grate expreasion (10):
_
f 1~Z d1=1/ A f w(!)d! Wn
t ~ (11)
where W~ is the ~ater reserve of the cloud in the direction Thie makes
it possible to find the value of the parameter A:
J A - {,~Y~dtls Wi. (12) _
1'
Now, knowing the parsmeter A, it is poasibl~ to determine the water content ~
at any point of the cloud in the direction Q b}r the formula
~(1) = Yzc~~l~� ~13~ -
, Experiment and Analyais of the Results
T'iuring the summer of 1977 on the active-passive radar complex ~ 3.2 cm) _
inetalled at the tegt area of the Main Geophysics Observatory in Voyeykovo, -
a eeri.es of observations were made on the eumu~onimbus clouds (Cb). Radio-
sounding of the atmosphere was perf ormed during the obaervations. -
6
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Table 1. Values of the regression~co~ffic~ent and its mean
equare deviation as a function of W=(~�a )~T for ~
~ bright _
- ~~3.2cm
_ I eD -
~o ~o sa e~
~ 0,081 0~043 0,024 0,009
_ Qp Q008 0~004 Q002 0,00! .
Table 2. Experimental resulta using the active-passive radar
complex (a ~ 3.2 cm) on 3 July 1977. _
Time Coordinates
hrs. min 82i- eleva- Tbr.ex~K ::br.qlear PTbr. 1�r t~
muth tion
9 08 16b 7S a8,7 ~~4 40,3 10,50 0,24
~ 9 12 . 187 10,0 53,3 19.7 3!',6 8,35 0,24
t3 52 36 20,0 59,6 10.2 49,4 11.75 0,57 `
l4 21 133 ~ 20,0 82~7 10~2 72,5 17,25 d,40
- I4 21 l 33 30,4 88,7 61 ~68 14,80 0,40 '
Note. Tbright exp is the experimentai value of the radio-
brightness temperature, Tbright.clear is the value of Tbright ~
_ for a clear sky, ~Tbright is the radiobrightness contrast,
WR is the water reserve of the cloud in the sounding d~rection,
_ ZH is the altitude of the lower cloud boundary.
The investigated thick Cb were aelected using the MRL plan position indica-
tor. In order to obtain the radar reflectivtty, a signal from an oscillo- -
graph was recorded on photographic film using the FARM photo attachment.
In order to avoid obtaining clipped $ignals, damping was introduced and the
correspondin~.isoecho level was selected. The photography was done with
each decrease in damping by 6 decibels. By the series of frames olitained
for eg.ch sounding direction, graphe were constructed of the variation of re-
,
flectivity along the soundin~ beam.
In order to determine the antenna temperatures the radiometer was calibrated
with respect to the "zenith." H~re the calculation of the radiobrightness
temperature of the clear sky when observing in the zenith was made by the
radiosounding data. On the obaervation days, an analysis was made of the
synoptic conditions and the nature of the cloud-forming processes.
For analyais of the experimental results a seriea of observations of the Cb ~
on 3 July 1977 was selected. On that day a cold front pasaed in the morning -
7
' TAV~ A~+w~n~ ~.~w w..~
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- with low stratiformis dropping in places to 50 meters. During the
day active convection, showers and thunderstorms were observed in the un-
- stable sir masa behind the front. ,
Table 2 gives the resulta of sounding the Cb on 3 Ju1y 1977. With respect to -
magnitude of the water reaerve of the cloud along the sounding beam and with -
re~pnct to the reflectivity profile, water content prof iles were reproduced.
Figura 3 ehows the result of i;his reproducti~n for 0912 houra on an a2imuth
of A ~ 187� and with an elevation of S~ 10�~ The figure ehowa the profile
of the lagarithm of the radar reflectivitv lg Z and the water content profile
w, g/m3. Aa is obvious from the figure, the course of ~he water content pro-
file repeata the course of the 1g Z profile. The values of the water con-
tents themselvea (maximum ~4 g/m3, average ~1-1.5 g/m3 correspond completely
to th~ water content of the Cb which can be observed [3].
In order to coordinate the reproduced prof ile of the water content with the
_ cloud Figure 4 gives the picture of the clflud system obtained using the IDV
of the I~iL-2 on the near azimuth (A = 164�). Of courge, the difference in
azimuth o~ 23� doea not permit exact coordination of the reproduced water
content profile with the cloud which was observed using the active-pasaive
co.mplex. However, it ia possible nevertheieas to make some def ined remarka.
The first three peaka of the water content profile are for cloud I. In the
free epace between clouds I and II, the wat~r content in practice dro~s to
zero. Then the growth of the water content wir.h the local maximum for a dis-
tance of ~10-11 km from the active-passive complex is observed. This maximum
corresponds to cloud II. Thea the water content gradually decreases, drop- ~
ping to zero. This corre�ponds to the fact that the sounding beam (it is
shaam ae a solid etraight line in Figure 4) pasaes through the upper layera
of the claud at an altitude of 3-4 lain. Either insignif icant water content or
cryetalline phase is observed in these layera.
I~Z U!E/MJ ~g~
f 4 _ _ . y -
` 0 J � ~ / -
, / 1
-f 2 ' ~ / ~ 1
. / ~ ~ 1 .
I ~ / 1 ~ ~
_ -1 � ~ I 1 / / 1~
- ~ \ / ~
~3 ~ 2 4 6 8 10 LK~w
_ Figure 3. Prof ile of the logarithm of the radar reflectivity
(1) and the reproduced wate.r content profile (2) corres~ponding
to the case ~f sounding the Cb on 3 Juty 1977.
Key: a. g/m~ -
8
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Z KN . . -
8 ' ' f `
_ 4 ~ � o~
~ 4 8 !2 f6 ~0 14 28 32 J6 l rtM '
Figure 4. Diagram of a cloud ayatem obtained oa the IDV of _
the MRL on 3 July 197.7 (0912 hours) an an azimuth of A~ 164�. e-
I~- firet Cb cloud. II aecond Cb cloud, 1-- dir~c.*.ion of
~ the sounding beam of the active-psaeive complex. _
It must be noted that, unfo~tun~tely, during observations of the Cb using the
active-paasive complex, direct aircraft souziding to obtain.direct data on the -
water content ie impoasible. This doea not permit c~mparison of the repro-
duced water content profile with the actually existing water. content prof~le -
in the cloud. Such a comparison can be realized, however, for the aqueous `
_ ni~boatratus clouda (Ns), aircraft saunding of which is posaible. .
Conclueions
The experimen~al observations of the cumulonimbus clouds using the active-
passive complex demonstrated that the propoaed procedure for estimating the
water reserve of the cloud and reproducing the water content profile along
the sounding beam ie prospective for the complex inveatigation of cloud sys-
tems. These cloud parameters are highly important when diagnoeing the auita-
bility of cloud syatema for weather modif ication to regulate precipitation
and ~onitor the reaults of these weather modification operations. HowevPr,
the authora admit that the effect depends t~ a significant degree on the
evolution of the clouds obaerved at the given time and the changes which
occur in the moiat+ire content characteriatics themselves with time. In order
to diecover the cloud evolution, a special observation procedure is needed,
above all a sufficiently high frequency of observations of the same cloud
center inasmuch as another center (another mesosyatem) can be in a different
stage of development and undergo ita own evolution. It is also necessary to
includa a procedure for estimating the integral water vapor content in the
complex method in order to have the posaibility of tracing the redistribution
of two water phases in the cloud with time. _
The developmEnt of the complex methods of cloud sounding considering the
' stated remarke and also the methoda of analyzing the physical processes of
~ cloud formation based on active-passive radar equipment is the next goal of
the collective of authora.
9
~nu n~rrreT rTC~ n*rrv
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BIBLIOGRAPHY
1. L. P. B~bylsv, M. A. Vagishcheva, A. I. Novaselov, et al., "Study of
- the Water Content o� C1QUde Uaing the Three-Cent~meter Radiometer," _
TRUDY GGO (Works of the Main Geuphyeica Observatory), No 328, 1975,
pa~~s 50-55a
2. L. P. Bobylev, M. A. Vasishcheva, G. G. S~~chukin, "~9etermination of the
_ Integral Moi.sture Cantent Parameters of a Cloud Atmoephere Directly by
thP Values of the Radio'arightneas Temperature," TRUDY GGO, No 395, 1977,
_ pages 59-67.
3. M. A. Vasishcheva, G. G. Shchukin, "Experimental Study of the Water Con- _
tent of Clouds. Statiatical Models of the Atmoaphere," OBZOR VNIIGN:I-- ,
1~!'rSD, SER. METEOROLOGIYA (VNIIGMI Survey MTsD, Meteorology Series),
Obninek, 1976, 94 pagea. -
4. N. V. Gornostayev, A.. I...Novoaelov, V. A. Petruahevskiy, et al., "Active- -
Pasei~ve Radar for Studying the Atmoaphere," TRUJY GGO, No 32$, 1975,
pagea 120-124.
- 5. N. D. ~opova, G. G. Shchukin, "Proc~dure for Aetermin~ing the Water Con-
tent Prdf ile in Clouda by the Paeaive-Active Radar Method," TRUDY GGp,
No 395, 1977, pages 68-71.
~ 6. V. D. Stepanenko, RADIOLOKATS7YA V METEOROLOGII (Radar in Meteorology), ~
Leningrad, Gidrometeoizdat, 1973, 343 pagea.
7. V. D. Stepanenko, G. G. Shchukin, G. B. Brylev, "Active and Passive
Radar Sounding of Clouds, Precipitation and Thunderatorma," SOVREMENIYE
FUNDAM3~ITAL'NYYE I PRIKLADIYYE ISSLEDOVANIY~i GLAVNOY GEOFIZICHESKOY
OBSERVATORII IM. A. I. VOYE~KOVA (Modern Basic and Applied Research of
the Main Geophysics Obeervatory imeni A. I. Voyeykov), Leningrad, Gidro-
meteoizdat, 1977, pages 77-87.
COPYRIGHT: Glavnaya geofizicheskaya observatoriya im. A. I. Voyeykova (GGO),
1978. �
i~
10845
CSO: 8144/1073 -
10
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r
SOME POSSIBILITIES OF USING THE ~YNT~iETIi, APERTURES METHOD FOR OBSERVING
METEOROLOGICAL TARGETS
_ Leningrad TRUDY GLAVNOY GEOFIZICHESKOY OBSERVATORII: METODY AKTIVNOY I
. PASSIVNOY RADIOLOKATSII V METEOROLOGII No 411, 1978 pp 107-112
[Arti.cle by Yu. A. Mel'nik] -
~ [T~xt] One of the moat significant achievements in radar theory and engiiieer-
ing in recent decades was the development of the synthetic aper.turea method
wh~e~ made it poasible to increase th~ resolution of the radar syatems.for aur-
vey~ag the ~arth's surface to va].uas commensurate urith optical devices [1].
Aa ~e kno~m, thia method ia based on using the a priori data on the ~.aw o� ~
variation of the signal phase where during the procees of radar obeervation
the target is ahifted relative to the radar by a known law. For the harmonic
sounding oscillation with a frequency w the echo of the point target
ll~~
w ~
turna out to be modulated. The variation of the amplitude S is usually
neglected; the signal phase ~(t) is determined by the distance R to the tar-
- get. If the law of displacement of the target R(t) is known, the received
eignal can be sub~ected to.optimal processing which for the regular component
of the aignals is defined by the expreasion
~w . _ _
l _
Q1T~ ' ~ S~t~ $~t - T~(Lt. ~ ~ 2~
Ita maximum value ~ 2
QM (1/2)S T is pr.oportional to the signal energy for the _
obeervation time T. -
The optimal processing Zeads to the "cem~,ression" of the aignal inauring
high reaolution of the syatem. Thus, for example, it ia known that in the
radar for surveying the earth's aurface the accumulation of the signal on
' the path of movement of the radar d~ is equivalent to the use of a large _
synthetic antenna of dimenaion d~ which at a range R~ determines the linear
11
L'AD AL'L~Tl~T AT TTQL+ /~*TT V
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- resolut~.on Ox =~/d~R~, where ~ is the wavelength. The maximum possible path
on ~ahich the aignal ie received in turn dependa on the beam width of the real
antenna (that ie, on ite aperture d), and it is d~ ~~RD/d. From theee ex-
preseione it follows that tha admiaeible value of the reeolution along the
direction af movement ie equal to the aperture of the real Fintenna inetalled
on the ai.rcraf t .
' The method of synthetic ~antennas can be extended to the caee of a set of ~ar-
geta made up of particles which move by given laws. The procesaing aystem
:.an be designed for isolation of the total signal of all the elemQntary re-
flectors, the parameters of morion of which vl, ~v2, vn lie within cer- .
tain limits v+ + ~V1, v2 + Ov2, vn � Ovn. The result of the procesaing for
the obaervation time T is proportiona~ to the energy of the signal character- ~
izing the reflectivity of certain particlea in the irradiated apace, the pa-
ra~eters of which lie within the indicated limita. The set of these limits
_ establishes the region of inde~erminacy, inside which it ie impoaeible to
measure the apecific values of the parameters.
The region of determinacy dependa on the characteristics of the radar and the
observatian conditions. In the special case it can. turn out that all the
limits ~vi, with the exception of oae (for example, ~vl) exceed the maximum
- actually poasible variations ot the corresponding parameters of motion. In -
thia caee the syetem fer type-space coherent proceaeing of the eignals ia the _
- met~;r that measures the number of particles, the parameter of motion of which
v~ ia within the limita of vl � ~vl. Being given various valu~s of the para-
meter as a result of the time-apace proceaeing of the signal, it is possible
to determine the particle diatribution vl by this parameter with the reaolved
interval ~vl.
For the solution of the stuted problem it is necessary to determine how the
output eff ect of the optimal proceasin$ syatem varies if the parameters of
motion of the elementary targeta deviate from the given values. For this ~
purpoae it is expedient to introduce a generali~ed parameter in terms of '
which the deviations Ovi of the apecific investigated valuea of vi can be !
expreased. The phase lead the increment of the signal phase for the ob-
servation time T-- ia the generalized detuning parameter under certain
assumptions easily made in practice.
Let us propoae that under other invariant conditions the actiual law of aotion
of the target differs somewhat from the given one, and the received signal is
def ined by the f ormula
s(t) = S cos[w t ~(r) -I- ~'(t)]~ (3)
where ~~(t) is the phase incremeat by comparison with the calculated ~(t).
In this case'the output effect of the system can be represented by the ex-
preeaion ~
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r -
Q = ~ f cos ~'~t) dt. (4)
u
Lst ua def ine the relative value of the output effect t~ ~ Q/QM conaidering
that the deviation of the phase of the given law takes place linearly:
~~~t~ - ~~t~T (5)
and at the end of the observation intexval the nhase lead reachee a value of
Here the output effect of the proceasing syatem
y+ = sin (b)
depends only. on the phase lead. For a small phase lead where the proceseing _
syetem in practice is matched with the aignal, the value of ~ is equal to .
one. Aa the phase lead increases (for >~r/2) the output effect ~ assumes
different values within the iimits of zero to 1/~'. The maxi~um of this
value
~ 1~~~ ~7)
can be considered a responae to the signal of the given detuned filter.
The phase lead ie a funntion of the parameters of motion of the target. The
variation of some parameter v by comparison with the calculated value leads
to ~he appearance of the phase lead and attenuation of the output efFect
by 1/~' timea. If we consider the output effect as a function of several
parametere vl, v2, v~, the deviations of these parameters from the
calculated values (vi, v2, vn) and the attenuation of the output effect
caused by them are characterized by the indeterminacy function ~(vl, v2,
vn). Geometrically the function can be represented by the indeterminacy
body in the (n + 1)-dimenaional epace. The boundaries of the region of in-
determinacy can be given by attenua~ion of the output signal to the level of
t~~ or the resalved phase lead corresponding to it = 1/~~.
Thue~~ the region of indeterminacy ie the cross section of the body of inde-
terminacy on the level = 1/~~~ and can be represented by the equation
~(o Y~, o vZ, . . , e Y�> = t~a ~8~
The emall phase lead
= 1/~+(y;, Yz, . . . , Y;,)~ .
13
~ - TI~t~ ATT~~~T ~ ~ ~~w~ w.~
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which is a function o� the amall deviations of the parameters of motion
vi, v2, vn from the calculated valuee, can.be expresaed in terme of
theee deviatione as
~ v' v ` . . v' .
~ � ~ ~9~ _
Thie makes it poesitile to find the region of indeterminacy coneidering the
affect of each parameter on th~ phase lead separately.
For illustration of the posaibilities of the method let us conaic3er. the _
example of radar obaervation of the~precigitation, assuming that the speed of
the particles v is conatant and is directed vertically. Let us find the
region of in3eterminacy when the observation ia made.by the ground coherent
radar (see Figure 1), and the synthesizing is done as a result of the natural
movemeat of the particles. With accuracy to the conatant coefficiente t~e -
- expresaion (9) for this case can be represented in the form
~k~R -}-~vT~-{-~v,~~l, (10)
where ~h ie the resolution with respect to altitude, ~vr and ~vT are the re-
solutiona with respect to radial and tangential velocity, respectively.
(a) i
~
~DC eUr aur
u7
v .
~ ;
,
Qo
Figure 1. Syntheaizing aa a result of the n~tural motion of
the particlea of the ground coherent radar.
Key: 1. radar
The limiting valuea of each of the indicated resolutiona (under the condition
that the remaining parameters have rated valuea) are preaented in Table 1.
As follows from the data in the table, with amall accumulation time the sys-
tem is the standard meter of the radial velocity of the particlea. However,
for a large observation time there ia sufficiently high resolution with re-
spect to the tangential component of the velocity which is unusual for the
exiating doppler systeme.
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V PAC ~g)
s
~ I ~
i
~ i -
a~ ~ \
I \
~ \
v vT
' VT
Figure 2. Synthesizing as a reault of motion of the radar. .
Key: a. radar
Table 1. Limiting resolution with respect to altitude (~h) of
the tangential (~vT) and radial (~vr) velocity of the particlea
as a function of the observatifln time T for the stationary
- ground radar with a distance R~ = 300 km, wavel~ngth a s 3 cm
and partiale velocity v= 5 mJsec.
' ' ( rsec
o~t ( i . ~ io ~ iw
~h K . . . . . . . . . . 18000 1li~00 180 18
A vT w~se~ 1~8� 10� 1800 18 0.18
0 v~ ~~-sec 0,3 0,03 0.003 0~0003
Table 2. Limiting resolution along the path (~x) and with
respect to the particle velocity (pv) as a function of the
observation time T for radar moving with a velocity v= 7.5
km/aec for R~ ~ 300 km, a 3 cm and v= 5 m/aec..
I r sec
o,oi o,i ~ i
O x w ~ 80 8 0,8
~ v wJgeC 3 0,3 0,03
Let us consider $nother., t'heo~etically�different case where the synthesizing
ie realized as a reault of the.movement of the radar. Let us propose ~.hat
the speed of the carrier V~ 7.5 km/sec, and tne altitude from whicr~ ;...e
observation is made (R~) is 300 km (see Figure 2). The equation of tne
15
~
~ L~AD A~y+TnT A7 iTnn A*tr ~s ~
i
. . . . . . . . . . . I
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Table 3. Limtting reaolution along the path (~x), with
reepect to altitudE (Oh) and velocity of the particles
(~v) as a function ef observation time T f or rt+dar moving
with a velocity of 700 lm/hr for RD - 3 km, a~ 3 cm and
_~t.~_ 5__ID~.sec
rsec ~ '
�~01 ~ ~ i -
A x w 50 5 0,5
~ h x ~ 50 5
0 v w~gec 3 0,3 0,03
region of indeterminacy for thia case can be approximately represented in the
f orm
VT ~
A x-~- o v ~=1.
(11)
Ae followa from the data in T~ble 2 for a comparatively small time of signal
accumulation there are quite high values of the resolution with respect to
the speed of the particles (Ov) and the position of the observed �~olume along
the direction of motion of the carrier (~x). The system is not s~naitive to
the remaining parametera.
The resolutiona of ~x and ~v can either be poaiti~ve or negative. Therefore
formula (11) definea four straight lines in the coordinates x;, v' with re-
apect to the rated values of x and v. The region defined by these straight
lines (see Figure 2) includes the set of parameters of motion of the par-
ticles, the signals of which are released by thQ processing aystem.
~ .
U ,
- ~ . ev i
i
~ , -a.x o.x
-.x y~ v ~ r !
i
/I ~ ~
~ -ov ~
-v~
Figure 3. Region of parameters of motion of particles, the ,
aignals of which are generated by the processing syatem.
Analogously to formulae (10) and (11), the expressfon can be obtained for the ~
region of indeterminacy where the observation ia made from an sircraft. A~
_ ~
16
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follows from the data in Table 3, the ayatem has some re~~lution with reapect
to altitude which is explained by the comparatively small removal of the
observed region.
Thus, tha mathod of aynthetic aparturea ia theoretically applicable for obser- -
vatioa of ineteorological targete. However~ for determining the practical
poeaibilitiea of its realization and eatimating the effectiveneee, special
etudies are required. `
_ HIBLIOGRAPIiY
l. A. P. Reutov, B. A. Mikhaylov, G. S. Kondratenko, et al., RADIOLOKATSION-
NYYE STANTSII BOKdVOGO OBZOttA (Side Viewiag Rads~r), Moscow, Sovetskoye
; radio, 1970, 360 pages.
COPYRIGHT: Glavnaya geofizicheekaya observatoriya im. A. I. Voyeykova (GGO),
1978.
10845
CSO: 8144~1073
17
F~R ()FFT(:TAT. TTCF. nxr v
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~ OCEANOGRAPHY .
OBSERVATIONS OF FRONTS IN THE POLYMODE ARF.A
Moscow OKEAN~~OGICHESKIYE ISSLEDOVANIYA in Russian No 30, 1979 pp 86-88
[Article by A. G. Zatespin, A. Yu. Rrasnopevt$ev,.K. N. Fedorov]
[Text] The existence of fronta in the Sargasso Sea ia a well-known fact -
[l, 2]. flowever, tfie subtropical convergence zone intercepting the
5argasao Sea is a large-ecale front separating the more saline and ,
warmer aouthern waters ~~and the fresher and colder northern waters. The
results obtained by A. D. Voorhis, et al. [2J indicate that ~he temperature
fronts occur at the boundariea of the "tongues" of warm and cold water
which are caused by affectfve transport by the geostrophic currents
connected with the eddies. The opinion has been stated that the fronts in
the ocean are well to be aeen in the fall and winter period, and in the
summer they are masked by warming of the upper layer. On the 25th trip of
the "Akademik Kurchatov" scientific reaearch ship~.an effort was made to
generalize this scattere~ information about the fronts which can be
extracted from the data of synchrnnous density surveys, from direct measure-
meaCs of the current velocities, towing of a thermistor and measurement by
a Chermal-saliaity probe on the path of the ship in the region of expedi-
tionary operations. As a result~ it is possible to draw the following
conclueions. . ,
- ~ ~ ~ i
- , l. In apite of the masking effect of the summer warming, the fronts in '
the vicinity of the test area are comparatively easily detected by the ;
temperature and salinity measurements in the surface.:layer of the ocean. '
The density survey also permits determination of the approximate position '
of the fronta. The sharpest fronts were in September, which is explained
by sharpening of the zonal temperature and salinity gradienta. Theae
gradients were smallest in August. During the time of the operations in
the test area~ 13 cases of intersection of fronts by the ship were
recor.ded. The temperature gradients on the fronts fluctuated from 0.2 to
2.0�C; the salinity gradients fluctuated from 0.2 to 0.4 parts per thousand. ~
Gradien~e from 0.1 to 2.5 deg/1~ and from 0.1 to 0.2 parCs per thousand/1~ ;
correaponded to them. On the average the temperature gradient was 0.2
to 0.3 deg/km. ;
~
_ ~
18 ; ~
i
)
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;
~ ~~19,228 4
28,2 '
1~d
~ 1Q 1~0 30'
27,8 ~
" 2 0_ v
Q
- Z~4 18,k 18,
, ~ U 2~0
A ~ 28,?
- 1
- 2a,4 - za,t Zd
, , 28,1 ~
M � � 70 6d
Figure 1. Tetnperature at a depth of 10 meters (September): -
cyclone center; A-- anticyclone center. The regions
of location of the fronts are cr.oss hatched.
2. The fronts detected in the test area were characterized by positive
correlation of the temperature and saZinity gradients with far from com-
plete compensation with respect to density. Here the density gradient -
was mQre frequently determined by the temperature contribution than the ~
salinity contribution.
3. The data of the density and the XBT-surveys confirmed the reault~ of
A. D. Voorhis, et al. [3] pertaining.to the existence of the warm and
- cold "tongues" of the~advective origin connected with the dynamics of the
eddies. We have noted an analogous picture also in the salinity distribu-
tion~ that is, the "tongues" and "spots" of more saliae and fresher water
were detected. This structure of the temperature and salinity fields was
correlated with the etructure of the eddy field.~ Usually the fronts are
loeated on the boundaries of the "tongues" and "spots." Fig 1 shows the
temperature map on which the cyclone and anticyclone centers are indi-
cated. The fronta were located in the crosshatched zones.
4. In the vertical sections the fronts are traced to the upper boundary
of the layer of 18-degree water (100-200 meters) and obviously do not
penetrate deeper. This is also confirmed by the T, S-diagrams of the
vertical temperature and salinity distributions with respect to different
_ sides of the fronts; they are~analogous to the T, S-diagrams obtained in
their time by E. J. IEatz [1]..
It is important to note that an explicit relation of the front positions
to the atructure of the eddy field and to the vertical thermochaline
structure of the deep water has been detected. The fronts are located
above the peripheral regions of the eddies where maximum deviations of
the isotherms and isochalines of the principal thermocline are observed.
19
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~ i
_ . I
' f07 fOS f03 f0Y 99 97 95 93 92 23, SKH ~ -
0 . '-"i ~
_ i zs ,
i
. li'= -
f00 10 i -
19 i
i
, IQD ' i
- . � . . .
S00 � ` .
Ii ,
- . ~e ~
aoo
. ' -
soo -
f6
� >S !
!00 I
14
~
f3 ~
~ 700 f2 i
800
n Q~
' ~
T'C � ~
2Q,4
18"0 '
2~d j~) ' �
Figure 2. VerticaL section in the temperature field according
to the data from the XBT-survey (a), recording of the surface
temperature (b)
As direct measurementa show. these regions correspond to the maximum
orbital current velocities in the eddies. Fig 2 shows the vertical
aection �in the tempe~ature field. In Fig 2 the curve reproducing the -
aection of the analogous temperature recording recorded by the.towed gauge
indicates the position of the froat on the aurface in the scale of the~~.
section. The problem arisea of whether the fronte are not characteristic -
"conductors" between the eurface and abyssal layers which promote heat
and tnase exchange through the the~ocline. According to the opinion of
Voortiis, et al. [3], by means of the above-described "tongues" of water
of advective origin connected with the eddies, horizontal heat tranafer ~
is realized. It is not excluded that the ~eddies have a significant
influence also on the vertical transfer through the fronts occurring on
their interaction. Hence, it is clear that the program for fur~her ~
20 -
. ~
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. . ----t
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. . . _
FOR AFFICIAL USE ONLY
reaearch ahould ir.cl~sde the etud~r o~ the vertical etructure o~ the fronta
and th~ir intexact~.on with the eddy ~ield.
Abatract
Tha relaticn of the temperature-salinity fronts in the ocean surface
- laqer to the large-scale surface temperat~re and salinity fields and the `
eddy field atructure in a thermocline ia analyzed.
BIBLIOGRAPHY
l. Itatz~ E. J. "Further Study of a Front in the Sargasso Sea,"
TELLUS, Vol 1~DCI, No 2., 1969, pp 259-2G9o
2. Voorhie, A. D,; Here~y, j. B.. "Oceanic Thermal Fronts in the
Sargasso Sea~" J. GEOPIiXS. RBS., Vol 69, No 18, 19b4, pp 3809-3814.
3. Voorhie, A. D.; Schroeder~ E. H.; Leetmaa, A. "The Influence of Deep
Meaoecale Eddies cn Sea Surfaee Temperature in the North Atlantic
Subtropical Convergence," J. PHYS. OCEANOGR., No 6,,1976, pp 953-961.
COPYRIGHT; Mezhdovedomstvennyy g~eofizicheskiy komitet pri Prezidium
e1N SSSR, 1979
[8044/0785-10845]
10845 ~
CSO: 8044/0785
.
21
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~
- I
- i
i .
STUDY OF TEI~ERATURE FLUCTUATIONS WITH INERTIAL AND DIURNAL PERIODS
Moscow OKEANOLOGICSESKIYE ISSLEDOVANIYA in Russian No 30~ 1979 pp 89-92
[Article by L. I. Limanskaya, ~e. G. Morozov, A. S. Samodurov]
[Text] The measurementa of the temperature fluctuations in the varioua
parts of the ocean, as a ru1e, reveal the presence of energy peaks both ~
on inertial and diurnal periods [1]. This is connected with the exietence -
of different physical mechanisms exciting oscillations with the indicated
periods.. The temperature fluctuations with a period of 24 hours are �
caueed by a baroclinic tide which obviously is caused by the interaction
of the barotropic tide of the same period with unevenaesses of the ocean ~
floor or the coastal shelf [2-4]. The sources of the temperature fluctua-
tions with an inertial period are lesa in~estigated. However, on the
basia of the frequently noted fact of their alternation in space and in -
time it is considered that the nonuniformities in the wind field are
responsible for generation [5, 6].
The region in which the studies are performed by the POLYMODE program has
the negative peculiarity~:thst the inertial period is close to 24 hours.
The difference in the physical classes generating, on the one hand, the
tidal fluctuationa of the diurnal period, and on the other hand, the
inertial fluctuations, has aroused interest in the effort to expand the ~
Cempexature of the appearance of the two mentioned phenomena in natural
aeries.
The epectral functions calculated,by the numerous temperature realizations
in the test area indicate the presence of a clearly expressed peak on a
period of about 24 hours. It is possible to consider that this peak ia
caused by two processes the diurnal internal gravity waves (a period
of 24 hours) and the inertial fluctuations with a period close to 24 hours
(the local inertial period on a latitude of 30�.is 24 hours, on a latitude
of 29�, at the center of the test area, it is 24.75 hours, at the southern
part of the buoy test area (buoy II), 25.85 hours).
22
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A~ a reeult o~ such a sntall dif~erence between the periode and ineu�ficient
length o_` the sar~tes theae :fluctuatione a~e not separated by tha spectral
methode. Actually, the frequency di~fereace on adjacent points of the
spectrum ie . .
~ Of -1 f 2M~t,
where MAt ie the maximum shift of the correlation function in ur~its of time.
In order to aeparate the periods T1~24 hours and T2=25.85 houra~ the fre-
quency reaolution must be
ef=~- 1 ~1 ~
?'t ' ~T, ~ 2M:1 i
The shift of the correlation fuuction here is
_ Met = T'~T ~ ~ 168~~,~1~ .
2(T, - T, j
- Keys l. houra ' -
In order to insure 20� of freedom of~ the calculations the aeries must~be
no less than 1680 hours, that is~ about 70 days. Sere the values of the
epectral functions on the fr.equencies of interest to us will correspond to
the ad~ acent pointe of the spectrum with numbers 13 and 14 respec~tively.
For reliable separation it.is necessaxy that there be at least one point
between the corre$ponding points of the spectrum, and this leada to an
increase by twofold, that is, a five month series is required.
In order to obtain preliminary ideas about the structure of the inertial
and diurnal internal oscillations and their time variability, we made
an effort to separate these oscillations using the method of complex
demodulation first used in oceanology by V. Ye. Prival'skiy [7]. Thus~
we etud ied these oacillations directly by the series of isolated harmonica
of both.periods. The filtration parameter here must be selected as follows
(filtration by the slidi.ng mean):
~ t 1 1 1 y-i ~~i~
~ T~ Tz r 335 . .
Key: l. hours'1
that~is, the filter parameter must be 335 hours. Selecting this filter
and adjusting.the calculation for one selected frequency, we.completely
auppressed the second. ~
The results of the calculation (that is, the harmonics of each of the
periods) for the point II(the 50 meter horizon) are presented in Fig 1.
_ ~ The duration of the ser~es is from 24 July to 26 September.
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FOR O~~ICtAL U~c, ~1NLY
er,�c ~ ~
g4 ~
- 0,2 ' ~ ~
u
41 . . ~
R4 a~ '
� ~4 . . ~ -
Qt n
pil
. . l
0,1
~ ~ ~ i i i ' . .
f0 ZO 30 � 40 SO cym~ru (1)
. b~ . ,
Figure 1. Inertial (a) and diurnal (b) harmonics of the
temperature realization on the buoy II(horizon 50 meters)
obtained by "gluing" of the seriea according to the data '
of two buoys operating in series with resAect to time. -
xey:
i. a8y8 -
From Fig 1 it is obvious that the nature of the variability uf each type
of fluctuation is different. This indicates that this variability ia
determined by the nature of the fluctuations themselves and not by the
variation of the vertical temperature gradiex~t in time. For the inerti~l ;
period the train atruct~re is characteristic actually with one obvious ~
oscillation train for the entire two-rmonth observation period. The
24-hour fluctuation ~s charactex3zed by 12-13 day variability which can ~
be connected, on the one hand, with'the synoptic processea [5], and on "
the other harid, with the semimonthly inequality of the barotropic tides
generating the internal waves [8], The result obtained can be considered ~
somewhat unexpected. C. Day and F. Webster [9] performed measurements of
- the currents south of the Bermuda Islands at a latitude of close to 30�.
- ~ The results of the investigations indicate that the energy of the fluctua- ~
tions with a period of about 24 hours experiences eignificant variability '
in time. According to the data of the mentioned authors, on the 50-meter ;
horizon this varial~ility correlates quite well with the paesage of storma ~
over the east coast of the United States. The relatively amooth varia- ~
tion of the amplitude of the inertial temperature fluctuationa with time i
discovered in this paper can be=.connected with the fact that~ weather i
conditions as a whole varied little during the period during which the
- meseurementa were taken. The recorded train of inertial oscil.lations ~
,
~ 24 ~
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poasibly is connected with the intenei~icati.on o� the wiad in the test
area to 1~-11 m/sec obaervad ia the laet l0.days ~of Auguet for 7 or~8 daye.
~
_ By the measurement reaults during the �irst setup in July Auguat, the ~
abyssal atructure of the time variability of the d3urnal and inertial
fluctuations was analyzed. �
Fig 2 ahowa the graph of the amplitude variati~n of the diurnal and inertial
fluctuationa in time for different horizons at the point II for a period of
about 30 days in Auguat. The nature of the variability of the inertial
fluctuations with respect to depth is different. At individual times in
certain horizons an increase in the oscillation amplitude is observed
whereae on other horizona, a decrease in it occura, which is connected
with nonatationary regime and nonuniformity of the inertial flucruations.
e~t . .
ODn at ,
: gf .
' ~~IDN~~ y Q ~ ' �
Q~ .
x~, g2 as . .
az
,
' ~e,oa Q0e
Q04 0,04
' f S f0 xf 20a0aycma f S f0 ~f IOa4rycnr~
~1~ b~ - (1)
Figure 2. Variation of the amplitude of the inertial (a) ~
and diurnal (b) temperature fluctuations for the 50~ 400~
70Q:and 1400 meter horizons during August 1977.
I�eiy � '
�1. August
~ This atructure can be determined by the multimodal nature of the fluctua-
tionc or different sources generating oscillations at different depths.
This can be determined also by a time delay in the different horizona of
the diaturbance propagated with respect to depth from the surface. An
imsufficient number of ineasuremeat horizons does not permit reliable
confirmation of the latter. However, the disturbances are delayed with
respect to depth. According to the rough eatimatee the average propaga- -
tion rate of the disturbance downward is about 1.3 m/hr in the layer from
50 to 700 meters.
The amplitudes of diurnal temperature fluctuations vary at different dept":
according to different laws. However, the variability in the upper
400 metere is smaller. Their variability in the deep pair of horizons
. 25
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r un ur r i~..eaa. u....
at 700 and 1400 meters ia also simi.lax. Obviously, there are two differ-
ent eyetaws generated by di~~eraat sourcee in the diurnal fluctuatione.
This poesibility in this area was indicated previously in reference (10].
It ie possible to propose that tha~diurnal fluctuations in the upper layer
daterminad by the internal wavea of the diuraal period are geaerated by
tha iateraction of the barotropic tide witn the coastal shelf of the
. naarby islands or continent [4]. The fluctuations in the basic thermo- ~
cline caa also be determined by the internal waves generated by the baro-
tropic tide interacting with the unevenneases of the bottom [2~ 3).
In conclusion it ie~necessary to note that the arr~,litudes of the tempera-
ture fluctuations oa inertisl and diurnal periods are approximately
identical, and tt~erefore they make an equal contributio.n to the formation
of unseparated peak in the spectral densities of the temperature fluctua-
tione.
Abatract
By means of complex demodulation the diurnal and inertial temperature
fluctuations are distinguished ae measured on buoy stations of the POLYMODE
test area. Tha time and depth variability of each of the fluctuationa is
studied. Hypotheaee are suggeated for the mechanism of the fluctuations '
under the conditiona of the teat area.
: .BIBLIOGRAPI~Y �
1. Ivaaov~ Yu. A.; Morozov, Ye. G. "Study of the Temperature Fluctua- ~
tions on Tidal and Inertial Period," ATLANTICflESKIY GIDROFIZICHESKIY '
POLIGON-70 [Atlantic Hydrophyaical Polygon-70], Moscow, Nauka,
1974.
2. Cox, C. S.; Sandstrom, H. "Coupling of Internal and Surface Waves
In Water of Variabl,e Depth~,." J.. OCEANOGR. SOC. JAPAN, XX~TH ANNIV.,
1962,.pp 499-513. , '
;
3. Baines~ P. G. "Th~ Ceneration of Internal Tides by Flat-Bump ~
,
Topography," DEEP.SEA RES., No'.29, 1973, pp 179-205. i
I
4. Rattri, M. "Occurrence of Tides in the Coastal Zone," VNUTRENNIYE � I
YOLNY.(Internal Waves], Moscbw, Mir, 1964. ;
5. Moain. A. S.; Kamenkovich, V. M.; Kort, V. G. IZMETTCHIVOST' I
MIROVOGO OKEANA [Variability of the World OceanJ, Len~ngrad~
Qidrometeoizdat, 1974. ~
6. Pollard, R. T. "On the Generation by Winds of Inertial Waves in the '
Ocean,~~ DEEP SEA RES., No 17(4), 1970, (
~ 26
. .
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7. Prival~akiy, V. Xe. "Complex Aemodulation o~ Random Proceases snd
ite Applicatioa for the Analyais of Tides," MATERIALY XIIT NAUCHIdOY
KONFERENTSII DVGU [Material8 of the 13th Scientific Conference of ~
- the Far Eastern Hydrologic Administratioa], Vladivostok, Part 5,
No 1, 1969.
8. Ivanov, Yu. A.; Morozov, Ye. G. "Semimonthly Iaequal3ty of the
Interaal Wavea of the Tidal Period," DOKL~ AN SSSR [Reports of the
USSR Academy of Sciencea], Vol 236, No 3~ 1977.
9. Day, C.; Webster, F.. "Some Current Measurements in the Sargasso Sea,"
DEEP SEA RES., No 12(6), 1965, pp 805-8].4.
10. Mirabel'~ A. P.; M~orozov, Ye. G.; Plakhin, Ye. A. "Some Peculiarities
of the Vertical Structure of the Temperature of the Tropical Part of
, the North Atlantic," I2V. AN SSSR. SER. FIZ. ATM. I OKEANA [News
of the USSR Acadeury of Sciences, Physics of the Atmosphere and Ocean
Seriesl, Vol 9~ No 9, 1973. ~
COPYRIGHT: Mezhdovedomstvennyy geofizicheakiy komitet pri Prezidium
_ ' AN SSSR, 1979 ~
[804~4~/0785-10845] ' .
10845 ~
CSO: 8044/0785
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SEPARATION OF SFMIDIURNAL TEI~ERATURE FLUCTUATIONS DETERMINED BY THE
BAROTROPIC TIDE AND INTERNAL WAVES
M~oecow OKF~ANOLOGICHESKIYE ISSLEDOVANIYA in Russian No 30, 1979 pp 18-81
[Article by Ye. G. Morozov, A. S. Samodurov, L. P. Filatova]
[Teut] As ie known, in the ocean there are always two types of fluctua-
tiona of an identical time scale this is the aemidiurnal barotropic -
tide and the internal baroclinic gravity wave with the same period. The
spatial acale of thase oscillatione ia distinguished by approximately aa
order. However, when studying the fluctuations of the hydrological .
characteristics of the 12-hour period using time realizations of the
temperature and current at a point, the spatial scale cannot manifest
itself. Therefore, both types of oscillations are taken as a united whole.
Inasmuch as barotropic tide in practice causes no vertical shift of the
water particlea, the temperature fluctuations caused by it are insignif i-
cant. The temperature fluctuations are determined basically bj~ the
interaal gravity waves having a vertical velocity component, Therefore
the tidal~ internal wav~s~are studied by the temperature~fluctuations.
In many papers, in particular, in [1] it ia demonstrated that the hori-
zont~l coherence of the current fluctuation on a 12-hour period is small.
Thia ia explained by ttie fact that both the barotropic tide and the
baroclinic tide make�contributions to ~the current fluctuations approx-
imately in equal proportions. In addition,~from the general physical
arguments it is clear that the coherence of the fluctuations muat be rela-
tively hi~h.
In ref erence [2], b~ averaging the Fourier coeff icients vertically, an
effort was made to separate the velocity field into barotropic and baro-
clinic tides. In this study another procedure was used. For the separa-
tion of these fluctuations, ~ust as in reference [2] the property of the
barotrapic tide was used invariability of the horizontal current
velocity vertically. In the region encompassed by the POLYMODE program
(at point D) a buoy was installed with current velocity meters from the
surface to the bottom. The BPV-2 and BPV-6 instruments were installed
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at the 100, 700, 1400, 3000 and 4500 aaetex horizons at an ocean depth of
5200 meters, and at the 25~ 50, 100, and 700 meter horizons temperature
recordere ware suspended. The autonomous buoy stptioa operated for 9 days
with a meaeurement apacing~of 1 hour. Using the complex damodulation ~
procedure (3j~ the 12-hour harmoaic wae isolated from the realizatione
~utually a band wae isolated with a period of I2�2 houre). The realiza-
tion~ of the U and V componente, the velocity modulus and temperature were
subjected to thia processing. Thus, ia the current fluctuationa band that
lias been isolated, both batotropic tide and internal wave were present.
The internal wave will make a basic contribution to the temperature fluc-
tuations, for the temperature variatioas caused by advection of the hori-
zontal nonuniformities of the temperature by th~ barotropic tide are small,
especially deeper than~the seasonal thermocline layer. Below, a detailed
atudy was al.so made of the temperature fluctuationa.
After isolation of the narrow-frequency band from the series of currents
for separation of the internal and barotropic tides the currenta measured
every hour on one vertical were averaged. The series obtained was an
approximation to the velocity sexies (components and modulus) caused by
the barotropic tide, The word "approximation" was used inasmuch as the
five measurement horizons selected at the characteristic points of the
vertical~is the minimum number of ~horizons~for which such an operation
ia ~uatified. The ap~roximation to the barotropic tide that was ob~ained
' ie further interpreted by us as the barotropic tide. Increasing the num-
ber of current meters naturally should improve the result. However, _
even for auch a small number of observation horizons the expected result
was obtained. The isolated averaged series~of velocities (orbital
velocities of the particles of the barotropic tide) varied in time with
a period af 12 houra. The difference on each horizon between the initial
series which is the sum of the barotropic and the baroclinic tides and
averaged vertically, which is the barotropic tide, gives a series far _
the orbital velocity of the particles in the int,ernal wave. Let us denote
theae three series by UE, Ubt, UiW respectively. In all horizons the
series Uiw also fluctuate with a 12-hour period. It is necessa~y to
indicate the values of tfie oscillation amplitudes of the velocity modulus: -
for the series UE=10, Ubta~S-6, Uiw `5-6 cm/sec at~ depths to 1000 meters
= and 2-3 cm/sec at depths of more than 1000 meters for all variables.
Thus, during the semidiurnal fluctuations of the currents the barotropic
tide and the internal wave in the upper layers make an approximately equal
contribution; in the deep layers the barotropic tide makes the primary
- contribution.
It ie interesting to note that C. Wunsch [4] estimates the en~rgy of the
semidiurnal baroclinic tide on the whole throughout the ocean as 10-15~
, of the barotropic of the same period.
Using our data, it is possible to calculate the ratio of the enero-�
the baroclinic tide to barotropic in the vicinity of the investigateu te~:.
area by the expression
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~ ~
: ) � h~ ) J, (1) 1 '
. k = ~oo ~oo ~'N1 ~ e~e1400 ~ h3 ~ � h, ea.~~oo' hs
. ~~g�N . ~
Rey: 1. iw~internal wave
2. bt~barotropic tide
where Di is the disgersion of the current fluctuations caused by the
, baroclin~c tide on the corresponding measurement horizone; Abt is the
dispersion of the current fluctuations caused::by the barotropic tide;
hi is the layer thicknesa; H is the depth of the ocean; N- O~h~.
� ~ . . . � . . . i-~ .
A similar estimate for the relative energy of the internal tide in our '
calculations givea the value about 60X. Thia is ineignificaatly greater
than the value obtained bq Wunsch.
Let ue consider the resulte of analyzing the barotropic tide wave. Using
th ~ ~ ~ ~ I ~~-t
~'o ~ ~ ~
> V r~ o^
~ ' ~ m � ~
t~i ~ S e (4j v
D~7 ~ V
~ ^ ~ V v v U
a s V ~ ~
y r eo
x
. a~ 4
p m ~ U aL _ 4 .
P~ u ~ o, 9 x
y : ~t m a r. ~ g a .
7f p v a ~g
~ w a ~ '`'1, _ .
O~ X :C i" ~ d
~ f u ~ 4
~
�b " X s � u ~
Y ~ ~ ~ S a
D y x' S ~ ~ r N '
C
~ , o U ~ = U = q
v
N o, r.: ~ ~ ^ aai V Y
~ v v ~ ' ~
a ~
~ ~ ~ ~ ~ ~ x .
~
S
~i , ~ ; ~ ^ a
Q N ~ ' m
U
M v ~ I.~ I ~ m Q
a
V s , Li a Q a
~ , ~ 4 R , U ~ a U ,
. ~ C7 ~ . `t V o ^ ~
a : R Q ~ .
N - ; V . ~ ~ ~ ~
x
w ~ iC a ~ a a; ~
o ~ a = ~ % s
~ ~ ~ � ~z ~ n
- C! i t = r; =
~ ~ ~ ~ a ~ � Q ~ ~ '
YC m ~ ~ ~ ` ~
~ ~ ~ m S '
- u ' 1~ - a`~ ~ n pp
i ,e. . . ; . . C C - ^ ~ O.
N ~ ^ C �
~
~ ~ . n�'. 60
~ ~ ~ v ` C
~ Y O ,S ~
Yr
~ y y . . r... a C O
6ai :L . m ^ . 6=i ' ~
V � ' O ~S ~ ' ~ S 3S ~
~ T - ~ Y =~~.I F~- Q ~
3 w L~ x~ ~(X n 4-1
~
i a � ~ : i ir'o ~ ~ c~i� , . . ^
` ~ 3 a~ . = ca v' a O t~ i~"I C
o F K u ; . : . . . � iN v D+
o: u F., ~ ~ ` ~ ' ~ ~
~ o~~'. M . a~x a2� ag~-
~ Ap i~/ u'~ S 2 x ..5 $
~ - ~ . ~n
~ . r, . s y ~ : ~ m ~S ~
~ L+ R{'~~p � S y A � w t~' G
Sv ~ ~ C ~ u
55
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~ .
[Rey to table "Schedule of Interaa.t~onal Research under the POLYMODE
Program"]: ~ ,
,
l. Programs 14. Preliminary measurements, USSR
2. Types of operations~ times, 15. Synoptic experiment, USSR
participating countries 16. Array in the Gulf Stream,
3. Deaeity measurements (hydrologic, Canada
CTD, XBT-surveys) 17. Array in the Northeast
4. Preliminary meaeurementa, USSR Atlantic, England~ France,
5. Synoptic experiments, USSR Federal Republic of Germany
6. Preliminary measurements, USA 18. Current measurements by the
7. XBT-program, USSa, USA SOFAR floata
8. LD$, USSR, USA 19. Tests;'~USA .
- 9. Array II, USw 20. LDE, USA
10. Cluaters~A and B, USA 21. Current measurements by
11. Cluster C, USA , drifting buoys
' 12. LDE, USA 22. France
13. Inatrument meaeurements on, 23. LDE, USA
buoy stations ~
LDE local dynamic experiment; array a group of wavea in one line;
cluster a group of buoys clustered together.
2) (~uasisynchronous mesoscale hydrologic surveys using XBT probes,
ealinity temperature probes (ISTOK, AIST) and bathometric measurements in
the inside part of the test area with the same station grid apacing;
3) L~ong-term oceanographic observatioas at 19 autonomous oceanographic .
buoy stations inatalled at the corners of equilateral triangles (39 miles -
on a side) on the ineide body of water of a test area 134x154 miles with
its:center at the coordinates 29� north latitude, 70� west longitude;
4) Oceanographic observations in microareas on the acale of individual
eddy fornutions. -
Bottom depths in the water of the test area vary from 5100 to 5400 me~ers.
The current and temperature recorders were installed ori the 50~ 100~ 400,
700, and 1400 meter levels. The observations by the XBT probes were made
to a depth of 750 meters~ the.ISTOK and AIST probes and the bathometric
series, to 2000 meters.
Tha selection of the mentioned observation levels by the autonomous
buoy stations arose from the following arguments: 50 meters this is
the layer of active interaction with eynoptic processes in the atmosphere;
100 meters aea~rnal thermocline; 400 meters layer of 18-degree water �
of the Sargasso Sea; 700 meters 700 meters principal thermocline;
on thie level observ~tions are being made in accordance wiLh the American i
program using the SOFAR acoustic floats; 1400 meters depth of pure ~
barotropic synoptic current f luctuations. The TsIITT digital integrating ~
p ,
, 56 � ~
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. , FOR OFFICIAL USE OIJLY
- - � ~ .
. ' o 0 0 0 ' o 0 0 0
31~~u~.
0 0 0 0 0 0 0 (1)
0 0 o S o~ o ~ o 0 0
O O ~ K o O O
O O ~ O 0 ~ ~ O O O
A /
0 0 0 m O ~ O � o 0
0 0 0 O o 0 0
M A ~ T 29
O O O r~ 0 A f~ o O O
M -~4 ~
0 o ON O O i O' ~ c~ o 0
0 0 0 ~ O p O P o 0 0
.
0 0 0 0 0 0 0 '
~
0 0 o p o ~ o ~ o 0 0
. ~ !
0 0 0. o o. o . t
~ . Z~ ~ .
o: o 0 0 0 0 0 0
. ~
73~~.0. ~-t ~ 6B p'
~ ' - 4
~ Diagram of the POLYMODE expedition:
~1 - XBT-sounding; 2-- hydrologic series; 3-- STD-sounding;
4 autonomous buoy atations .
Key: � . . . . .
1: 31� north latitude .
automatic recorders developed and manufactured at the IOAN Institute
(designed by Valovskiy), the TsITT-3 meters (designed by Shekhvatov) and
, the BPV-2 recorders'(designed by Alekseyev)>were used to measure the
velocity vectors of the currents and the water temperature.
During the period from 11 July to 3 October 1977, the expeditionary ships
conducted five large-acale and three mesoscale surveys and also observa-
tiona ~in several microareas. During the same time the "Akademik Kurchatov"
scientific research ahip conducted 66 installations and 46 surveys of the
sutonomous oceanographic buoy stations.
v
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~ _
Duriag the first phase of the work in the test area, about.l millio~4
recordinge were made o� the current velocity vector components~ 463,000
water temperature recordings, obaervations at 1800 hydrologic�atations '
and temparature aounding stationa. All of the data went through primary
proce8sing.
The materials of this and the su~sequent stages of the expedition will be
published in the collections of articles OKEANOLOGICHESKIYE ISSLEDOVANIYA
~ [Oceanological Research], Nos 31, 32~ and so on.
Abstract
The Soviet-American POLYMODE proram, the goals of the experiment, the
ship measur�emznt program and structure of the test area~s in the south-
weatern part of the North Atlantic are described. The main types of the
studiea to be performed during the expedition and the time-space scales
to be atudied are analyzed.
~ CAPYRIGHT: Mezhdovedomstvennyy geofizicheskiy komitet pri Prezidium ~
AN SSSR~ 1979
[8044/0785-10845] ,
10845
CSO: 8044/0785 ~
I
.
. ~
1
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~
. ,
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. i
STUDY OF THE TRAIN STRUCTURE OF SHORT-PERIOD TEh~ERATURE FLUCTUATIONS
~
Moecow OKEANOLOGICHESKIYE ISSLIDOVANIYA in Rueaian No 30, 1979 pp 93-96
[Article by A. S. Samodurov, Ye. G. Morozov]
_ [Text] There are a significant aumber of studies in which it is noted
that the ehort-period (T�1 hour) internal gravity wavea exist in the
ocean in the form of individual groups separated by sections of relative
- quiet [1-4j. Most frequently the groups (or trains) of waves are detected
in defined ghases of the larger scale internal waves, as a rule, tidal.
flowever, the distinguishiag feature of the indicated measurements is the
fact that they basically were performed in the caastal shallow region
where the amplitudes of the long-period waves are maximal. In the case ~
where the regime of the large-acale wave is close to critical it was
demonstrated [5] that the wave train is formed in the vicinity of the point
u~c~, where u is the orbital velocity in the wave, c~ is the phase velocity.
The present study was undertaken in order to discover how much the train
- structure of the short-period internal waves is characteristic for the
open sea and also to determine the periodicity of the appearance of the
trains. It must be noted that experimeatally the train structure of the
short-period fluctuationa was also noted in the open sea [6-7], but its
e~i~tence w~e determined by the series' lasting no more than 8-10 days,
that is~ it was not confir~ned statistically. Therefore it is difficult to
~udg~ t~e p~riodicity of the appearance of the trains. The performed exper-
iment made it possible to obtain c~ntinuous series of long duration with
_ small discreteness.
We ha~ve used series lasting about'a month with a discreteness of 6 minutes.
W3th respect to the successive 2-day segments of this series spectral
functions were calculated for determining Che clearly expxessed energy-
bearing period T in the high-frequency region of the spectrum. The number
- of degrees of freedom was 20 everywhere. tin example of this series of
spectra is presented in Fig 1, from which it is obvious that on periods
close to 1 hour from time to time high energies appear. However~ after
a ahort time these flucCuations cease to give blips on the spectra.
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rvw VL C L~I1LW
It must be noted that the 50-meter horizon that we selected for investiga-
tian is the most characteristic by the variabi.lity of the fluctuation _
apectra in time and also the large vertical temperature gradients inasmuch
as it is located in the seasonal thermocliae layer. Let us note that on
. other horizona the variability of the spectra in time also occura. The
measurements performed with euch amall discretenesa at a depth of 1400
metazs indicate the presence of very strong variability also at thie depth.
Byiusiag the method:of complex demodulation [8], from the initial realiza-
tion fluctuations were isolated in a narrow range of perioda T+AT. The
value of At in all cases was 5 minutes. The period T wae selected by the
epectral analyeis, that is~ t ls also the period in the high-frequency
region of the spectrum at which high-energy blipe appeared. After pro-
ceaeing the seriea by the method of complex demodulatian, the harmonic of
~ the desired period was obtained with amplitude variable in time. From
thie harmonic~ a series of amplitudes were compiled. Its discretenesa
wae equal to the period T respectively. Thus, the series obtained is the
emielope of the harmonic isolated after complex demodulation. The spectrum
was again calculated by the formed series. The location of the peaks on
the conatructed spectrum (let.us call it indicates the most probable
periodic3ty of the appearanae of groups of high-frequency internal waves. ,
$t DZHU~ '
~~l) ~ .
� 0,3 , ~
~
1 . 2 3 -
Q1 � �
, .
4~ ~ ,
r�
110 60 36 d0 14 7,nuM
~2~ ~ ~
~ '
� i
� ;
,
4 S . j
' ' . . f
Figure 1. Five functi~ons of the spectral density calculated by
the successive two-day series on the buoy M(50-meter horizon).
The graphs indicate the time vartability of the temperature
fluctuations. The numbers are the numbers of the realizatione.
xey:
1. S, deg2-min; 2. T, min
60 '
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aefore we proceed to a discuaston o~ the.zesults, let us note that the
ragion in which the measurements were ~ade is distinguiahed by a complex
ayatem of currents caused by the passage o~ the powerful ocean eddies.
In reference [9] it was demonetrated that as a result of the Doppler effect
e~ting here the tidal and inertial peaks in the temperature spectra can
- ahift with reapect to frequency, which frequently also occurs in reality.
- FoT th~ conditione of the teat area the ahifte can be highly significant. ~
Thue~ if the currents with a velocity of 30 to 50 cm/sec and a propagation
rate of the obaerved wave of di~uraal period are directed in opposite
directione, the correapoadYng peak shifts to the vicinity of the periods
of 38-60 houre. The described phenomenoa turned~out to be eignificant for
the reaults of this paper.
In Fig 2, a~ d, apectral functioas ar~ depicted for four pointa of the -
tes t area. According to the data of the spectral analysis for the aeries
obtained at the poiats M, fl, II, R the periods T of the isola�ted oacilla-
tione were selecte:l equal to 60, 48, 50 and 60 minutes respectively.
From Fig 2 it is obvious that at two points M aad II there is a blip on a
- period of about 24 hours; at the points H and K there are quite strong
peaks in the 40-hour range; at the point II, a blip of about 50 hours.
As for the semidiurrtal period, on the presented graphs it in practice
- does not appear.
In our opinion, the peculiaritiea in the behavior~of the function ~ are
caused by the following causes.
_ The grougs of short-period internal gravity waues are formed in defiried
phasea of the internal tidal waves. This process occurs as follows. If
the ahort-period waves have a group velocity equal to the phase velocity of
eome large-scale wave~ the nonlinear resonance interaction occurring in
the system leads to growth of the small-scale disturbances [10-12]. This
mechanism a~ust, be manifested most atrongly in the vicinity of the defined
phase of the long wave where as a result of the peculiarities of the
vert ical disCribution of the velocity intensity (the Richardson number is
minimal) the occurring small-acale wave disturbances are suppressed to
the least degree.
As an illustration in Fig 3 we have the temperature fluctuations with a.
period of 24 hours isolated from the initial series using t~~e method of
complex demodulation and variations in time of the fluctuation amplitude -
with a period of 48 minutes at the same point. It is obvious that zhe
peaks of the lower curves frequently occur for the same phase of the `
diurnal wave. It is interesting to note that the amplitude of the latter
in the indicated phase is zero. This means,'in particular, that the
time behavior of the amplitude of the short-period oscillation is caused
by aperiodic variations of the mean temperature gradient caused by the
diurnal wave.
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~ta~~MVN
~1~ � .
t:
QN ;0 a01 �
M Rd N p A'
40! QO! . ~
� R2
~ H n, aio n aeta n ,~t~ .n ~r ~2) .
Figure 2. Spectral density functions ~Y constructed by the
series of amplitude peaks after processing the aeries by
the method of complex demodulation according to the data
- of buoys M, H, II~ K(50-meter horizon)
Ktsy :
l. S. deg2-min
2. T~ houra ~
_ ~ !
er'c . . I
Q6 ~
Q4 a~ '
1t1
a1
R4 ~ .
Q6 �
A' C
a: ~ .
.
a~ .
- ~
, , , , , ,
f 1 3 ~ S 6 7 Q P f0 1! 7Z ~J T,cymn~ ~1 ~
Figure 3. Time variability of the diurnal temperature fluctua- ~
tion and temperature fluctuations with a period of 48 minutes ~
(50 meter horizon): a-- diurnal fluctuation harmonic, b--
amplitude of the fluctuation with a 48~minute period. The
liaes ~oin the amplitude peaks with a period of 48 minutea for
defined phases of the diurnal fluctuation.
Key :
1. T, days ~
. f
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' The appearance of the groups o� high-frequency waves with periads greater
than 24 h.~urs is caused by the Doppler ef�ect as a.result of which the
parameters of the diurnal internal wave vary [9]. _
The "energy" of *_he groups of waves appearing with diurnal periodicity is
greater than the "energy" of the trains of semidiurnal period inasmuch as
- the parameters of diurnal wave are�.such that in them the occurrence of
the traine of short-period waves has greater probability. The internal
wave with a 24-hour period is characterized by large mode number [9].
This means that the vertical scale of the diurnal wave is less than semi-
diurnal and, consequently, here for equal amplitude large vertical velocity
gradients are formed. In addition, for equal amplitudes the diurnal wave
ie ateeper than the semidiurnal as a result of the fact that for a large
mode number tha wave length is shorter. This leads to instability of the
wave and the formation of a pack,et of short-period waves.
_ The increase in "energy" of the trains on periods of 38-60 hours is
explained by the fact that the corresponding gradients of the quasi-
etationary current are superposed on the vertical velocity gradients in
the diurnal wave. This implies an increase in the overall velocity shift
and pramotes more intense growth of the short-period disturbances.
Abstract
The periodirity of the short-period internal wave trains is gtudied. The
wave trains are~shown to occur with the period of the diurnal tidal wave
due to the instability of the latter.
BIBLIOGRAPHY
1. Ziegenbein, J. "Short Internal Waves in the Strait of Gibraltar,"
DEEP SEA RES.,.Vol 6, No S, 1969.
2. Gade, G.; Eriksen, F. "~Jotes on the Internal Tide and Secondary
Oscillations in the Strait of Gibral.tar~" ARBOK UNI V. BERGEN,
MAT.-NATUR. SER., No 9, 1969.
3. Hecht, A.; Hughes, P. "Observations of Temperature Fluctuations in
_ the Upper Layers of the Bay of Biscay," DEEP SEA RES., Vol 18, No 7,
1971.
4. Byshev, V. I.;� Ivanov, Yu. A.; Morozov, Ye. G. "Study of Temperature
Fluctuations in the Frequency Range af the Internal Gravity Waves," -
_ IZV. AN SSSR. SER. FIZ. ATM. I OKEANA [News of the USSR Academy of
. Sciences. Physics of the Atm~sphere and Ocean Series], Vol 7,
No 1, 1971.
5. Samodurov, A. S. "Generation of Internal Wave Trains in the Ocean,"
ISSLIDOVANIYE IZMENCHIVOSTI GIDROFIZICHESKTKH POLEY V OKEANE [St-:uy
of the Variability of the Hydrophysical Fields in the Oc~an], Moscow,
Nauka, 1974.
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~~6. Sabinin, K. D. "Some Peculiarities of Short-Period Wavea in ~he
Ocean~" IZV. AN SSSR. SER. ~IZ. ATM. I OI~EANA, Vol 9, No 1, 1973.
7. l~orozov, Ye. G.; Plakhin, Ye. A.; Shapovalov, S. M. "Study of the
Temperature Fluctuations in the Northwestern Part of the Pacif ic
Ocean in the Frequency Band of the Internal Gravity Waves,"
OKEANOLOGIYA [Oceanology]~ Vol 16~ No 1, ~976.
8. Prival'skiy-,-V. Ye. "Complex Demodulation of Random Processes and
Its Applicatioa for Tide Aaalysis," MATERIALY XIII NAUCHNOY
KONFERENTSII DVGU [Materials of the 13th Scientific Conference of
the Far Eastern Hydrologic Administration], Part 5, No 1,
Vladivostok, 1969.
9. Morozov, Ye. G.; Samodurov, A. S.; Limanskaya, L. I.; Filatova, L. P.
"Study of the Diurnal and Semidiurnal Temp~ratu~e Fluctuations~"
sea the present collection, p 63. '
10. M~Iatyre, M, E. "Mean Motions aad Impulse of a Guided Internal
Gravity Wave Packe~~" J. FLIIID MECHAN.,.No 60, 1973, pp 801-811.
11. Grimshaw, R. "The modulation and Stability of an Internal Gravity :
Wave," I~i. SOC. ROY. SCI., Liege, 6th Series, No X, 1976, pp 299-314.
12. Grimshaw, R. "The Modulation of an Internal Grsvity Wave Packet R
and the Resonance with the Mean Motion," STUD. IN APPLIED MATHF~I.,
No 56, 1977, pp 241-266.
COPYRIGHT: Mezhdovedomstvennyy geofi,zicheskiy komitet pri Prezidium
AN SSSR, 1979 ~
[8044/0785-10845]
10845
CSO: 8044/0785 '
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,
UDC ~28.516;62?.396.962.21
PHASE RADIOGEOAETIC SYSTEMS FOR MARINE RESEARCH
Moscow FAZOVYYE RADIOGEODEZICHESKIYE SISTEMY DLYA MORSKIKH ISSLEDOVANIY
(Phase Radiogeodetic Systems for Marine Research) in Russian 1979 aigned
to press 11 Nov 79 pp 2, 152-153, 162-163
[Annotation, conclusion and table of contents of book by A. M. Agafonnikov,
Izdatel'stvo "Nauka," 1,000 copies, 164 pages]
[Text) Annotation. In this book the author generalizes and systematizes in-
formation on phase radiogeodetic systems operating in the range 1.5-3 MHz.
'I'heir circuitry is described, as is the instrumentation itself and the
methods for using it. Information is given on the propagation of radio
waves. The proble;ns involved in increasing the accuracy of systems and
the prospects and directione of their development are considered. The
monograph is intended for scientific workers, graduate students, engineera
and students specializing in the f ield of marine geodesy and radionaviga-
tion. Tables 2, figures 77. Bibliography of 184 items.
Conclusian. As already confirmed by the enormous experience in their use,
phase radiogeodetic systems as a tool for horizontal coordinate tie-in
_ have a number of valuable qualities which make them indispensable in -
conducting many types of marine research and exploration work: high accur-
acy, continuity of operation, technical aimplicity in obtaining a reading
of thz conditional coordinates. At the same time they have a number of
shortcomings restricting the pcssibilities of their use: low effective
range, c:eed for setting up and servicing a cha.in of shore stations, and
ambigujv~y of the phase reading. How promising are phase radiogeodetic sys- ~
tems and will they not be replaced by other systems and apparatus having
poaitive q~ialities but which are without some of their shortcomings?
The most probable alternative for phase radiogeodetic systems are satellite
navigational and geodetic systems which operate without interruption. Ex- -
ieting satellite navigational systems have a high discreteness of deter-
minations (up to one determination each one or two hours in the low lati-
tudes in the "Transit" system) and a duration of one determination equal
to the time of satellite transit over the radiohorizon of th~ point to
be determined (12-18 minutes). In the United States specialiats have c~~-
veloped a plan for the continuausly operating "Navstar" satellite -
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L'Vl\ VL'i lv~~u~ _ ....`.a
navigational ayatem which it is planned will be in operation in 1985. Ac-
cording to preliminary computat~.ons, it will provide usere (which at
firet will be the United Statee Army, Navy and Air Force) with a contin-
uous determination of position with a horizontal and vertical error of 30
m. For the time being no real accaracy evaluatione have been publiehed. In
, the future syatems of thie class can evidently replace phase radiogeodetic
systems. However, this will require that they ensure a guaranteed accuracy
in determining poaition the same as phase radiogeodetic systems and that
- the coat of the apparatus and its operation be the same as in phase radio-
geodetic systems. A period of about 10-20 yeara after introduction of the
"Navstar" aystem may evidently be required in order to attain these
indicea and Li~til then the system will be used in regions where the re-
quired accuracy and continuity of tie-in cannot be ensured by phase radio- ~
geodetic syatems due to the imposaibility of further deploymen.t. It can
therefore be asserted that in the next 15-20 years phase radiogeodetic sys-
tems wi11 not be replaced by satellite system~, at least in the tradition-
al greas of their use.
During recent years communicationa have appeared in the press concerning
the use of tropospheric scattering for increasing the effective range of
ultrashort-wave aystems to 300 km. The advantages of the ultrashort-wave
range are: abaence of reflections from the ionoaphere and considerably less-
er reatrictions on the width of the signal spectrum, as a result of which
exclusively wide-band systems ensuring an unambiguous determination of
poaition with a still higher accuracy than phase radiogeodetic systems
are uaed in this range. Unfortunately, the effective range of these systems
is limited to the distance of direct visibility, not exceeding 70 km over
the aea under ordinary canditions (the heights of raising anterinas is about
20-30 m). Tropospheric scattering makes possible a considerable increase
in the range of propagation of ultrashort waves beyond t~e horizon, but in
this case it is necessary t~ have a very great increase in transmitter
powers. To a considerable degree this limits the possibilities of using
such systema. In addition, the conditions for tropospheric propagation
are characterized by inatability associated with tropospheric turbulence.
For these reasona there is no basis for assuming that ultrashort-wave
radiogeodetic aystems with the use of tropospheric scattering can be an
alternative to phase radiogeodetic systems, although in some favorable
cases they cax~ be used instead of them.
It therefore follows from everything set forth above that phase radiogeo-
- detic systems operating in the range 1.5-3 MHz will continue to remain an
indispensable means for highly precise horizontal coordinate tie-in f.or the
coastal zones af seas and oceans and will be promising for at least the
next 15-20 years. This will require their further inatrumental improve-
ment and the further development of ~:~thods for their use.
66
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CONTENTS Page
Preface 3
Chapter 1. Theoretical Principles of Radiogeodesy. Fundamental Concepts
1.1. Principles of determining pasition on earth's surface 9
1.2. Errors in determining position (fundamentals of theory) 11
1.3. Basic information from theory of harmonic oscillations 16 _
1.4. Methods for determining distances and differences in dis-
tances by phase radioelectronic apparatus 22
1.5. Phase radiogeodetic meaeurements and their information content 42
Chapter 2. Radiation, Reception and Propagation of Radio Waves in the
Range 1.5-4 MHz
2.1. Radiation and reception of radio waves 49
2.2. Prapagation of radio waves in homogeneous medium 60
2.3. Propagation of radio waves along earth's surface 62
2.4. Propagation of radio waves in the ionasphere 71
Chaptsr 3. Phase Radiogeodetic System Circer~itry and Apparatus
3.1. Circuits and apparatus for producing and detecting phase shift 80
3.2. Radiogeodetic phase meters, phase indicators and phase
recorders 90
3.3. Reference oscillators 102
3.4. Radio transmitters and transmitting antennas 105
3.5. Radio receiving apparatua and receiving antennas 108
3.6. Existing phase radiogeodetic syatems 111
Chapter 4. Instrument Errors in Phase Radiogeodetic Systems and
Measures for Reducing Them
~ 4.1. General characteristics 115
4.2. Phase errors in high-frequency circuits of radio receivers 118
4.3. Phase errora in rectifier and low-freqtlency circuits of radio
, receivers 124
4.4. Phase errora in radio tranamitters 129
Chapter 5. Principles of Method for Using Phase Radiogeodetic Systems
and Prospects for Their Further Development
5.~. Generalized method for using phase radiogeadetic systems 131
5.2. Prospects and possible directions in development of phase
- radiogeodetic systems 142
5.3. Combining of phase radiogeodetic systems with other systems
and apparatus for navigation and determining a ship's
position 148
Conclusion 152
Bibliography 154
COPYRIGHT: Izdatel'stvc "Nauka," 1979
[291-5303]
5303/CSO: 1865
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ARTICLES ON THEORY AND PREDICTION OF TSUNAMIS
Moscow TEORIYA I OPERATIVNYY PROGNOZ TSUNAMI (The Theory and Operational
Prediction of Tsunamis) in Ruasian 1980 signed to press 1 Nov 79 pp 3-4, 173
[Preface and table of contents from collection of articles edited by V. N.
Nekrasova, Izdatel'stvo "Nauka," 800 copies, 179 pages]
[Text] Preface. Thia collection of articles was prepared by the Commiasion
- on Taunamis of the InterdepartmPntal Council on Seismology and Seismic Re-
sistant Construction of the Presidium USSR Academy of Sciences in collabor-
ation with the Sakhalin Multidiaciplir~e Scientific Research Institute Far
Eastern Scientific Center USSR Academy of Sciences and other organiza-
tions. Earlier collections of articles of this type were published by the
. Interdepartmental Council on Seiamology and Seismic Resistant Construction
and the Sakhalin Multidiscipline Scientific Besearch Institute in 1956,
1961, 1968, 1972, 1973, 1977 and 1978 (twice).
M~oat of.the articles in this collection are devoted to improvement in the
v seismic method for predictir.g tsunamis, which since the beginning of the
1950's, when the aervice for warning the population of the Far East about
the approach of taunamis was established, to the present time in easence
remaina the aole working method for making such predictions. Due to its
stattetical character it cannot, in principle, enaure a 100% reliability
and effectiveness of the service. The universal improvement of this meth- ~
od is evidently of great importance. Appropriate efforts are now being
undertaken in the following directions: 1) search for new criteria relat-
ing earthquakes to the generation of tsunamis; 2) refinement of the mag-
nitude criterion in relation to generation of tsunamis; 3) automation of
proceaeing of aeismological data.
Ae additional criteria relating to the generation of tsunamis, during re-
cent yeara it has been traditional to study the spectral composition of
body waves, earthquake depth and focal mechanism. In this collection of
articles A. I. Ivashchenko and A. A. Poplavskiy, R. N. Burymskaya and N. A.
Zhbrqkunova examine the aearch for spectral criteria; definite progress is
noted here, but it muat be noted that the mean abaolute level of the am-
plitude apectrum of a longitudinal wave discriminated by A. I. Ivashchenko
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- and A. A. Poplavskiy as a criter.ion for an earthquake generating a tsu-
nami in esaence means giving a preference to tne magnitude mp over the
ordinary magnitude M in evaluating whether an earthquake leads to the
formation of a tsunami. A detailed examination of the possibilitiea of
using the earthquake focal wecl~anism for increasing the effectiveness
of prediction ia examined in aa article by R. N. Burymskaya and Ye. A.
Vorob'yeva; the problem is difficult to solve due to the need for uaing
data for only one atation under the present conditiona of the service.
The articlea of A. I. Ivashchenko and F. D. Zhuk, L. S. Oakorbin and 0.
N. Solov'yeva refine the peculiarities of computation of magnitude of
an earthquake under the conditions of operational work at tsunami sta-
- tions. The results make it possible to increase the accuracy of comput-
ations. A. A. Poplavskiy and I. N. Tikhonov continue a long-term cycle
of atudies for creating a set of algorithma on the basis of which it
' would be possible to automate determination of the principal paxameters
of an earthquake. The article by Ye. A. Vorob'yeva is devoted to a non-
traditional method for determining the epicentral distance of an earth-
quake, since on the records of instruments at tsunami stations in the
Far East transverse waves frequently are poorly expressed or are en-
tirely absent. This section was prepared under the direction of A. A.
Poplavskiy.
Three published articles describe individual possible components of an
observation system for the detection of tsunamis in the open ocean.'For
example, I. M. Shenderovich and G. N. Mar propose a filter of a funda- ~
mentally new type for discriminating tsunamis from the superposing of ' _
ocean level oscillations; A. G. Smagin and his colleagues propose a
quartz senaor for measuring ocean level; B. V. Levin, B. M. Lisenko and
V. Ye. Rokotyan propose that lidars be used for detecting tsunamis at
relatively short distances from the shore.
Individual articles are devoted to further theoretical work on problems
related to tsunami excitation and propagation. They contain new, orig-
inal results. S. S. Voyt, A. N. Lebedev and B. I. Sebokin examine the
problem of tsunami excitation when there is a horizontal effect on the
water layer a quite typical case under natural conditions, but vir-
tually not considered in the literature (in contrast to vertical m~ve-
ments of the sea floor). V. F. Ivanov and L. V. Cherkesov undertake a
study of the contribution of dispersion and nonlinearity to the trans-
formation of tsunamis in the process of approach of waves to the shore
and obtain refined estimates. An article by Ye. N. Pelinovskiy, I. A.
Soust~~va and V. Ye. Fridman examines the phenomenon of diffraction of
teun:~mis which is difficu].t to analyze and therefore which has been
poorly studied.
The sub,ject matter of two articles is treated for the first time in a
collection of articles on the tsunami problem. A note by A. M. Shury-
gin gives a preliminary atatistical analysis of the process of inun-
dation of the coast by taunami waves in the example of Libya and
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~�n
the article by V. A. Butkovskiy, N. V. Deryugin and N. A. Simonov describes
- an automated ayatem tor warning the population about tsunamis which has been
created on Kamchatka which makes maximum use of the ordinary radio and tele-
vieioa system. In the cycle of further studies of the taunami prob?_em, great :
attention wi11 undoubtedly be devoted to the problems involved in tsunami
regionalization and communication subsystems. ~
Although within the framework of a collection of articles it is impoasible
to reflect all the attainments in atudies of the taunami problem in the
USSR, it can be hoped that even in this form 't will be of coneiderable in-
' terest for apecialiste interested in development of ineans and methods for
contending with auch threatening calamities.
A. A. Poplavskiy and B. N. Sheyn took an active part in preparing the col-
lection of articles.
CONTENTS .Pa$e
Foreword 3
Voyt, S. S., Lebedev, A. N., Sebekin, B. I., "Some Peculiarities of ;
Tsunami Waves Related to the Characteristics of the Disturbance ~
Focus" 5
- Pelinovekiy, Ye. N., Soustova, I. A., Fridman, V. Ye., "Diffraction of
Taunami Waves in an Ocean of Variable Depth" 12 '
Ivanov, V. F., Cherkesov, L. V., "Role of the Joint Effect of Dispersion
and Nonlinearity During the Movement of Tsunami Waves in the Shelf ,
2one" 18 ;
I
Poplavskiy, A. A., "Automatic Operational Tsunami Forecasting" 29 !
Tikhonov, I. N., "Algorithms for Eatimating Epicentral Diatances from i
the Records of 'Yuzhno-Sakhalinsk' Seismic Station" 35 j
Ivashchenko, A. I., Poplavskiy, A. A., "Some Results of an Additional i-
Inveatigation of the Problem of Recognizing the Tsunami-Generating ;
Nature of an Earthquake" ~ 42 '
Tikhonov, I. N., Poplavakiy, A. A., "Initial Computer Analyais of a
Seiamogram Containing Intensive Noise" 49
Burymskaya, R. N., Zhbrykunova, N. A., "Analysis of Spectral and Tempor-
al Characteriatics of Strong Kurile Earthquakea of 1975-1976" 64 ;
Ivashchenko, A. I., Zhuk, F. D., "Calibration Curves for Determining
mp and mS from Records of Mechanical Seismographs" 74
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CONTENTS (Continued) Page
Oskorbin, L. S., Solov'yeva, "Nomogram for Operational Determination of
the Magnitude of a Near Strong Earthquake ~rom Body Waves Regietered
- by Seiamographs with Mechanical Registry" 107
Vorob'yeva, Ye. A., "Travel Time Curve of the Maximum Phase of Surface
Waves at Cloae Diatances" 112
Vorob'yeva, Ye. A., "Relationehip o~ the S/'P Parameter of a Seismic
Record Obtained in the Near Zone to Orientation of a Fault Plaze at
the Focus" 119
Burymskaya, R. N., "Some Resulta of Inveatigation of the Streased State
in the Earth's Crust and Upper Mantle in the Kurile-Ramchatka Zone" 133
Sh~irygin, A. M., "Long-Range Forecasting of Strong Tsunamia" 141
Shenderovich, I. M., Mar, G. N., "Filters for Subsonic iz~equencies for
Use in Inatruments for Measuring Tsunami Waves" 146
Smagin, A. G., Grundel', L. M., Kurkin, Yu. P., Mil'shteyn, B. G.,
"Highly Sensitive Frequency Sensor of Change in Level of Hydrostatic -
Presaure" 151 -
Levin, B. V., Lysenko, B. M., Rokotyan, V. Ye., "Lidar Methoda fc,r In-
veatigating Long Waves at the Sea Surface" 154
Butkovakiy, V. A., Deryugin, N. V., Simonov, N. A., "Automated Syatem
for Warning the Population of the Threat of Tsunami Waves" 159
- Alekseyev, A. A., Voyt, S. S., Solov'yev, S. L., "International Sympo-
aium on the Taunami Problem at Ensenada" 169
COPYRIGHT: Izdatel'et~ro "Nauka," 1980
[289-5303] ~
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- -
TERRESTRIAL GEOPHYSICS
UDC 550.34; 551.24+550.312+551.34+621.311.21+625.110
SEISMOGEOLOGY OF THE MONGOLIAN-ORAOTSK LINEAMENT (EASTERN FLANK)
,
Novoaibirsk S~;SMOGEOLOGIYA MONGOLO-OKHOTSKOGO LINEAAIrIIENTA (VOSTOCHNYY FLANG)
(Seiamology of the Mongolian-Okhotsk Lineament (Eastern Flank)) in Ruesian
1979 s~.gned to press 18 Sep 79 pp 2-4 and table of contents
- [Annotation, introduction and table of contents from book by V. V. Nikol- ~
ayev, R. M. Semenov and V. P. Solonenko, Izdatel'stvo "Nauka," Sibirskoye
Otdeleniye, 1,000 copies, number of pages not given3
[Text] Annotation. The geological structure, neotectonics and seismogeology
of the Tukuringra-Dzhagdinskaya part of the Mongoli~n-Okhotsk zone of deep
faulta are examined for the first time for seismic r~gionalization pur-
posea. Seiamogeological, seismic and geophysical data are uaed in deter-
mining the potential aeismicity of apecific morphostructurea and for
carrying out seismic regionalization of a territory earlier considered to '
be virtually aseismic. The aeismogeological conditions of the Zeya Hydro-
electsic Power Station and the Zeya segment of the route of the Baykal-Amur
. Railroad are de~cribed. The book will be of interest to seiamogeologiets,
aeismologists, specialists in the field of neotectonics, and also thoae
engaged in the planning of tranaportation, hydraulic, industrial and civil
etructurea, . ,
Introduction. A system of rangea, the Yankan, Tukuringra and Dzhagdy, ex- !
tenda 1atiLudinally across the entire uFper Amur region. This system ia ~
bounded on the north by the Tukuringra-Stanovoye intermontane depression ;
and the Udekn-Zeyakiy downwarp, and on the south by the Verkhne-Amurskaya '
depression and the Amur-Zeya plain. This mountainous ridge is associated '
with the Yankanskiy and Tukuringra-Dzhagdinskiy anticlinoria, whose for- ,
mation is structurally closely related to the 12ongolian-Okhotsk marginal ,
suture.
The Tukuringra-Dzhagdinskaya mountainous country is poorly populated. Nat-
urally, information concerning its seismicity was extremely scanty and
since seismic catastrophes have not occurred here, it has not attracted
the attention of seismologists and seismogeologista. The low level of
seiemic informa~ion was equated to a low level of aeismic activity of the
territory 5 scale units according to the norma given in the SNiP P-A.12-
69 (STROITEL'STVO..., 1970), although seismogeologista had assumed earlier
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that atrong earthquakes can occur here (Garahkov, 1931; Solonenko, 1950).
In connection with the planning of the Zeya Hydroelectric Power Station
the Institut~ of Physica of the Earth USSR Academy of Sciencea durinA
1964-1968 carried out a study of the seismicity in the seiamically danger-
ous zone of the hydroelectric power etation. The period of investigationa
by the Institute of Physics of the Earth coincided witih a period of de-
creased activity and thia zone was deemed to be aseismic.
IiAwever, on the basis of reconnaiseance seiamogeological observations in
1968 the region of the Zeya Hydroelectric Power station was deemed by us
to be seismically active; the seismic danger for the Zeya Hydroelectric
Power Station was related to specific atructures the Tukuringra-Dzhag-
dinskiy a:~ticlinorium and a deep fault (Yuzhno-Tukuringrekiy fault) passing
near the dam site. Planning organizations were informed of this on time.
But only after a strong (8 scale units) earthquake on 2 November 1973 was
it possible to carry out syatematic engineering field work in the neigh-
borhood of the hydroelectric power station (data on the seismicity of the
Zeya segment of the Baykal-Amur Railroad route were collected incidental
to this work).
The seismogeological investigations in 1974-1975 were made primarily in
the seiemically active zone of the Tukuringra-Dzhagdy Ranges and to a lesa-
- er degr~e to the north and south of it over an area of more than 120,000
lan2. Parallel to this structure, along the Stanovoy Range, there is still
another seismically active zone which spatially corresponds to a zone of
extansive manifestation of dis~unctive tectonics, a complex system of
horata and grabens, high contrast and ~.ntensity of neotectonic movements
accompanied by Quaternary volcanism. The Stanovoy deep fault with a high
potential aeismicity can also be traced here. -
A segment of the route of the Baykal-Amur Railroad and its branch Tynda-
Berkakit is under the influence of the earthquakes of this zone.
The principal purpose of this book is a deacription of the geostructural,
neotectonic and seismotectonic characteristics of the Tukuringra-Dzhagdin-
akiy mountainous ~one in relation to its deep structure and seismicity
so that on this basis it would be posaible to compile a seismic regional-
ization map of the general type which in essence would graphically reflect
the prediction of intensity of intermediate-maximum earthquakes and the
regions of their occurrence. The authora by no means consider the solu-
tion of the problem proposed in this study to be above reproach, especial-
ly for auch a geologically complex region where not a single fundamental
problem in the field of structural geology has an unambiguous solution.
The age of the folded systems and their boundaries are determined differ-
ently on each new map of structural geology. In addition, the geological
history evolution of the earth's crust is one of the criteria for deter-
mining the seismic potential of specific morphostructures.
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The authora express deep app-~ciation to special:ists in varioua fiptds at
the Geology Institute Yakutsk Affiliate Siberian Department USSR Academy
of Scisnces (B. M. Knz'min, A. G. Larionov), the Inatitute of Tectonica
and Geophysics Far Eastern Scientific Center USSR Academy of Sciences (F.
G. Rarchagin, L. A. Mastyulin, F. S. Onukhov, G. F. Ufimtsev) and the In-
etitute of the Earth's Cruat (A. D. Sarapulov, A. S. Yendrikhinekiy, V. M.
Knchetkov, N. A. Logachev, S. D. I~il'ko, and othera), and also apecialista
3n the technical editing laboratory of the Institute of the Earth's Crust,
who invested much work in ~inalizing the manuacript. _
CON.TENTS Page
Introduction 3
Chapter I. Problems in the Method for Seismogeological Research
and Study of Seismicity of a Territory 5
Concerning the reaearch method 5
- Seismicity 7 -
Chapter II. Tectonic Structure of Pre-Cenozoic Basement 24
Stanovaya zone ~ ~ 27
Mongolian-Okhotak zone 29
Suture zone and main deep faults 37
Chapter III. Principal Recent Strucrures and Mechanism of Their
Development 39
Age of peneplane ' 39
Mnst important recent structures 41
Horizontal movements 43 .
Elementa of deep structure of morphostructures 48
Statistical analysis of recent vertical tectonic movements 51
Chapter IV. Seismotectonice and Potsntial Seiamicity of
Morphostr�ctures and Zones of Activated Faults 54
Quantitative evaluation of neo- and seismotectonic movements 56
Morphostructural analyeis 66
M,oet important activa~ed faults 82
Chapter V. Seismic Regionalization and Problems of "Induced"
Seismicity 90
Initial data . 9d
, Description of saismic regions 95
Refinement of the initial scale unit for Zeya Hydroelectric Power
Station construction region and the prob.lem of "induced"
earthquakes 99
_ Seismogeological conditions along route of Baykal-Amur Railroad 103
Conclueion 105
Bibliography 107
COPYRIGHT: Izdatel'stvo "Nauka," 1979
[278-5303]
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~
HOLOGRApHY AND OPTICAL DATA PROCESSING IN GEOLOGY AND GEOPHYSICS
Leningrad GOLOGR4FIYA I OPTICHESKAYA OBRABOTKA INFORMATSII V GEOLOGII I
GEOFIZIKE in Russian 1979, pp 2-4, 193-194
[Annotation, table of contents and introduction from book edited by S. B.
Gurevich, Order of Lenin Physico-Technical Institute imeni A. F. Ioffe,
Leningred, S00 copies, 195 pages]
[Text] Annotation ~
Reports read at the All-U nion Seminar on Optico-electronic Methods of Pro-
cessYng Geological and Geophysical Data, held in Tomsk in 1978, served es
the basis for the present col?ection. The main theme of the collection is
the processing of large masses of geophysical data and the creation nf new
instruments and"devices f or the optical processing of geological and geo-
physical materials. SpeciPic methods and de~�ices are examined along with
survey reports on that theme. The materials presented in the articles are
of great importance for the development of work envisaged by the national
economic plan. They provide the possi~ility for specialists, geophysicists
and geologists to taecome acquainted .with t~e new possibilities opened up
by hologrephy and methods of optical data processing in tasks of searching
and prospecting for minerals.
CON~.'ENTS
Pege
l
Introduotion 3
0. A. Potapov. The problem of processing large masses of geological
and geophysicel data and ways to solve it 5
A. N. Galanov, V. P. Ivanchenkov, Z. V. Krivosheyev, P. V. Mineyev,
H. F. Onyushev and L. N. U1'chenko. Investi,gation of a combined
optico-electronic system for processing seismic data 19
S. M. Kofsman and Ye. A. Kopilevich. Optical f iltration of seismic
time segments with erbitrary filter parameters 's~
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G. I. Poskonnyy and V. P. Ivanchenkov, Investig~~ions of some
possibilities of optico-electronic com,~uter devides with spetially
incoherent sources of radiation 38
D. A. Kutukov and G. A~ Gusov. Improvement of thQ characteristics
of optical devices used to process geological and geophysical data 50
S. M. Kofsmen and Ye. A. Kopilevich. Use of synthesized holograms
in seismic data filtration 58
V. p. Ivanchenkov and V. A. Shlotgauer. Phase-frequency analysis of
seismic vibrations and s ome ways to realize it in optico-electronic
data processing systems 65
V. S. Pinzhin, Z. B. Khayut and V. A. Shlotgauer. Electronic
computer units of non-coherent"optical spectrum analyzer 74
R. S. Bechevskiy, S. A. Vasil'yev, G. I. Gas'kevich, B. V.
Gorodechnyy, N. I. Kalashnikov and I. Muravskiy. On the question
of developing the principles o~ contruction of optical processors 85
R. S. Bachevskiy, N. I. Kalashnikov, L. I. Kuravskiy ond 0. I.
1Q~arlova. On the questinn of coherent-optical processing of
optically reproducible recordings of area seismic ohservations 89
0, A. Potapov, 0. ~C. Vorob'yev and V. I. Dubyanskiy. Holographic
optico-digital processing of seismic survey data 95
0. A. Potepov and A. Ye. Shutkin [deceased]. Prospects of use of
coherent optical devices in systems f or the gathering, processing
and storage of geological arid geophysical data 102 -
A. N. Galanov and V. P. I`anchenkov. On estimating the properties
o! some methods o! spatially modulated registration of signals in
optico-electronic date processing systems 110
A. V. Dutov. Investigation of the noise resistance of some methods
of optical counting of geopttysical data 123
1~. I. Yurga and V. P. Tarasenko. Optico-eleet~ronic system of im~ge
enalysis based on an optical correla tor and electronic compute~r 134
A. B. Beklemishev. Seismic recording visualizAtion device based
- on the use of liquid crystalline media 144
A. B. Beklemishev, V. P. Alampiyev, Ye. M. Makeyeva, A. P. Shevalev
end V. V. Nemtsov. Analysis and interpretation of instability in
a liquid-crystalline matrix "with a me~ory" 153
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Page
V. P. Goiosov, V. Ye. Savarenskiy and S. D. Trankovsk!;. Use of
a pulsed laser to excite ultrasonic vibrations 163
R. S. Bachevskiy, S. A. Vasil'yev and G. I. Gas'kevich. Use of
- the method of optic ma tch ing of f i ltrat ion f or the ana lys is of
lineament grids 175
D. A. Yanutsh, Z. G. Yefimova and N. V. Skublova. Use of coherent
optical processing in the geological decipherment of aerial photo
surveys ' lg2
Introduction .
The complexity of the problems to be solved in the search for petroleum,
gas and solid mineral resources requires a considerable increase of com-
~ pute~ capacities and the developm~ent of inethods and means of effective
processing of geological and geophysical data. Computer compleses based
on second and third generetion elecCronic computers existing at the pre-
sent time do not completely meet contemporary requirements, in connection
with which a number of important end necessary algorithms for the�process-
ing of geological and geophysical data of ten are not realized in practice.
It should be expected that in proportion to the development of work on
area systems of observations and seismic holography the requirements for
the efficiency and operativeness of data processing will grow s till more.
In that respect much interest is aroused by the further improvement of
digital means of data processing as well as the developa~ent of optical and
optico-electronic methods which have considerable possibilities with -
_ respect to the processing and storage of large flows of data.
At~the present time in a number of scientific~and production organizations
and W Z's of the country experience has begn 'accumulated in the develdpaent
and use of optical computer systems, experience that confirms the prospects
of development of thet direction of autamation of the process ing of data
ot exploration geophysics and geology.
The First All-Union seminar on the optic o-electronic processing of geologi-
cal and geophysical data, held ~in 1978 in Tomsk,~summed up definite results
of investigations in that area.
The present collection contains reports read at the seminar that were
devoted to ques tions in the development and invest�igation of optical com-
puting devices and hybrid optico-electronic data processing systems. S ome
methodical and technological methods of processing, directed toward im-
provement of the methods and means of proces~ing geological and geophysical
materials, are examine~. -
The publica~tion af the'collection, in our view, will undoubtedly have a
positive influence on the fua~ther conducting of investigations and wil~
permit acquainting specialists with the results achieved in this area.
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It is proposed to continue in the future the discussion of optico-elec-
- tronic mothods and means of processing geological and geophysical data and
to issue subsequent collections of articles.
Professor S. B. Gurevich and candidates
of technical sciences V. P. Ivanchenkov
and 0. A. Potapov
COPYRIGHT: LIYaF, 1979
` [291-2174]
2174
CSO: 1863
~
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UDC 5S~ . 3~l~1
SEISMOTEGTONIC DEFORMATION IN THE GARM REGION
Moscow ~LVESTIYA AKADEMII NAUK SSSR, FTLIKA ZEMI,I iri Russian No 10, 1979
PP 2~-~3
[Article by A. A yukk and S. L. Yu,nga~ 0. Yu. Shmidt Institute of Earth
Physics, USSR Acade~}r of Sciences]
Abstract. A study is ;aade of the seismatectonic 3efor-
mation in the Gasm Region ~f the Tadzhik SSR ba,sed on
2250 analyses of the mechanisms for ~the foci of weak
(M < 4~) surface sarthquakes in the period f`rom 1964~ to
1976. The tensor for the rate of seismotectonic defor-
mation is presented with accuracy to a consta,nt multi-
plier as a product of the guiding tenso~~ corresponding
to the mean mechanism by the sum of the seismic moments
of the earthqua,kes. Time-sta,ble nuclei of cieformation
are isolated with linear dimensions 20-30 km, �..�is-
cussion is held- of the general pa,ttern o~: seismotectonic
deformation of the region and qua,lita,tivc~ hypothASes are
advanced on the causes of this process. A comparison is
made of the vartical seismotectonic and tectonic move-
ments. The position of strong earthqua.kes is e,~mined on
the background of seismotectonic deforma.tion. .
[Text~ 1. Introduction �
Currently~ ba,sed on a nwnber of direct and indirect data, it is generally
, a~cepted that earthquakes are induced by a shift of the earth's material
over a certain weakenod s~face [1-4]. The model of two orthogonal dipoles
without moments is adopted as an adequa,te representation of the focus of an
earthqua.ke bot~ f,,r elastic irra,c~~.a,tion, and for the sta,tic field of shifts
[5-7]. The orientation of the dipoles, i,e., the mechanism of earthquakes
= is defined by the pasition of th~ fault p].a,ne and the direction of the shift
vectar.
Tectonic and physical analysis of the mecha.nisms for earthquakes is ~oossible
~n the path of direct compa,rison of the orienta,tions of equiva,lent pairs of
= forc~s used in a mat;iematic description of the rariiation ~o;a the eaxthqua,ke
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focus~ and the really active tectonic stresses. The substantiation of such
a comparison is apparently hardly to be implemented without the involvement
of a strong hypothesis on the coincidance of the direction of the shift and
the direction of action of the maximum tangential stress. Usually the
average direction of action of the pairs of forces of "compresaion" is
taken as the direction of the greatest tectonic compression. In precisel
tha sama ~a the direction of the least tectonic compression ("ex~ension"~
is found ~8~. We note that such a separate finding of the average direc-
tions is generally not completely correct, since it does no~ completely
guarantee their perpendicularity.
In the case where the primary datt: are insufficie~it for a relia.ble analysis
of individua.l me~hanisms a joint analysis of aIl the signs of the first
arrivals of ths P-waves from the earthquakes f~ om one relatively small
seismicall active volume is used in order to construct a certa.in average
mechanism ~9]. Recently mathods have been for mulated of joint ana.lysis of
individual axes of compression and extension. P ublications [10~11] have
set limitations on the position of the axes of the tectonic stresses in
relation t,o tha main axes of the defined mechanism. Based on these limi-
tations and with the additional hypothesis on the consta.ncy ~f the field of
tectonic stresses in the studied volume ['ll, i2] t,ave suggested a graphic
method of f inding the dixections of the main tectonic stresses. A study.of
the ma,croscopically uniform stressed sta.te can be made numerically [13].
A n alterna.tive approach is used in rela.tion to the investigation of the
mecha.nisms of earthquakes occurring in the environs of a la,rge regional
fault. It is hypothesized that the earthquakes occurring on individual
sections of the fault or on its accessory faults of the same course have
approximately parallel planss of shifts. The task consists of finding the
beat orientation of the flat layer that conta ins these shifts, and of
determining the direction of the dominant seismotectonic movement of the
opposite sides of tha layer. The method for study of such tasks that is
rEduced to diagonalling of the matrix ~f the second order compiled ~om
individual mechar.isms is suggested in publication [14] and is used in a
nwnber of other works L15, 16].
Curxently the directions have been revealed of the main tectonic stresses
in all the seismically active regions of the world. Horizont,a.l compression
dominates in the belts nf neotectonic activa.tion, in the young folded zones, -
as well as in the insular arches and in the zones of Ban'off under them; in
the zones of groove-genesis a near-horizon~ta.l extension do~ainates [17].
However, a c~s-tailed stud of thd stressed and deformed sta,tes still encoun-
ters great difficulties ~10].
Here it is appropriate to turn to detailed works on an investigation of the
_ mechanisms for foci of weak earthquakes in the Garm region [18-20~. The
Garm region ha.s been studied fairly well i~n a geological respect and has
been described in de;�a,il in many works [21~ 23-25, and others]. I~t 3.s a
rt of the large zone of s~ructural atricula.tion of Pamir and Tyan'-Shan'
~23,24]. The modern mountainous country was actually formed during the
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Quaternary time (Pleistocene) [23-25], The considerations axe advanced that
the entire zone of ax ticulation is undar conditions af intensive neax-
horizontal tectonic compression in the near-meridional direction [23,24].
This can serve as the cause for the intensive process of mountain fcarma.tion
as a result of deformation of the ancient eopleistocene surface. A study of
_ the parameters of over 1,000 mechanisms of eaxthquakes made it possible -to
nofi.e that in different ts of the Ga.rm region the orientation of compres-
sion axea va,ried [19-22~ These sa.me publications undertook an attempt to
- isolate the regions of depression and elevation according to the sign of
shift of the suspended sides of the shifts in the foci of earthquakes in
relation to the diurna.l surface~ but within the framework of the employe:~
technique the stability of the results was not high. A simple increase
in the sta,tistics does not permit a significant improvement in the obt.ained
results due to the great diversity of the individua.l analyses of the
ireechanisms. The evident need arose for the enlistment of new methods for
studying ths set of inechanisms ~f earthqua,ke foci.
According to the extant ideas, the seismotectonic deformation of macroscopic
volwkes of mounta.in massifs is governed by slip ings over the different-
- oriented weakened zones in the earthquake foci ~26-30]. A quantitative
study of the link between seismicity and the tectoniC ;process was possible
tha,nks to the appeaxance of inethods for determining the seismic moment of
an earthquake from observational data, [31]. Brune [32] linIced the contri-
butions of earthquakes to the rate of tectonic slip with respect tr. -_~egional
faults with the sum of the seismic moments of these earthquakes. Ar.alysis
of the seismotectonic deformation of the region results in a generalization
of Brune's formula, for the case where the earthquakes occur over cYiaotically
arranged faults [13, 27, 28]. Recen�~ly, computations have bsen mac'~e of the
~ se smotectonic deformation of certa,in seismically-active regions [13, 28,
29 . This work covers a f~.m ther development of this direction~ whereupon
special attention is given to development of new method approaches to
studying the set of ear thqua,ke mechanisms.
2. Technique for Studing Seismotectonic Daformations
Deformation of seismically active volutaes of rocka on the ma,croscopic level
of examination is described with the help of the tensor for ra~e of tectonic
deformation < ei~> [13]
s lim lim 1~ 1(u,n~-i-uln~) ds. . � (1) .
- rir..o uL-.o VT 2
a
~ Here ui(ia1,2~3)--vector of movement of a certain point xi in ~he Cartesian
system of coordina.~,es OX1X2.X3 in the time T, ni--unit vactor of external
perpendicular to the surface S of volume V~I,3. The intervals 1 and t cor-
respond to the dimensions of tha spatia.l-temporal environs of the earth-
qua,ke focus in which significant cha.nges occur in the local deformatians,
movements and other parameters.
8Z
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The limit tranaitions in formula should be understood in that sense
that for con~putation of < oi~ > with fixed values of 1 and t by means of an
increase in Z and T the representa.fi,ive spa.tial-temporal region is selected. _
Such a region contains a sufficient number of inclusions in ~he form of
faults in the earthquake foci~ so tY~a~t the avera.ge value for the rate of
tectonic deformation does not depend on the fluctuations in ~fhefield of
- taove~nts on the surface of the volume.
~ We will expla,in the geometric meaning of the t,ensor component one can determine
the rate of deformation in an arbitrary direction assigned by the unit
vector 1
=lrli� ~ (g) .
li~ the case that interests u~, when within -the volume V~here are fault _
surfaces s�, cX=1, 2~ 3... , N, the integral in definition (1) na.t~ally is
divided into two parts corresponding -to the ra~te of conti uo s deformation
and the rate of seismotectonic deformation wHe ~nin and we have been ~riented on the fact that
in some quite narrow region where w~wHecos ~(crosshatched in Fig 1), the
initial wave will be strongly absorbed, transmitting its energy to the
resonance electrona and the turbulence. Here, effects can occur which are
- connected with the eruption of electron fluxgs in the ionosphere Ig by
reemission of Wn, mi,~rti,o~~eflected electrons with large initial pitch angles
in the equatorial p`~ane wher~, as is known, the radiation intensity is
maximal. Finatly, the backscattering of the initial hiss waves from the
turbulent region WP can occur. In order to estimate the expected effect
we calculated the trajectory characteristics of the VLF-waves for M0~4,
various modele of the electron concentration and the distribution functions
of the high-energy electrons. Fig 2 shows the values of the L-parameter of
the tra~ectory, the angle ~ of the double group delay 2tg and the relative
proportion of the energy absorbed by the plasma for f=?5.0 kil'ohertz and
_ various magnetic disturbance conditione (different Kp-indexe~) depending on
the current magnetic latitude of the tra~ectory (A=60� the initial lati-
- tude, A=0� latitude of the geomagnetic equator). Let us explain the
meaning of the last value((8W~/8t) (NT)'1). The process of the absorption
of the wave energy and the correspnnding increase in energy of the electrona
' or turbulent degrees of freedom can be described by the following equation
d~+8i'a(NTe~-(j~~-- ~ ~1)
Equation (1) is written by analogy with the equation of the energy balance
in a colliding plasma. Here WE is the energy density of the heating wave,
NTe is the effective thermal energy of the plasma electrons, and the term
dv*~(NTe) describes the energy transmission to the turbulence with turbulent
- "frequency of the collisions" v* and the coeff ic~.Ent d. If the initial
level of the turbulence is low, then the value of ((-dWE/8t)(NT)-1=P) has
the meaning of the inverse type of building up the turbulence. If we pro-
pose that the established level of turbulence is such that ONTe/NTe~10-2-10-3
(and this ia characteristic for weak turbulence), it is possible to estimate
v* proportional to the square of the turbulent field amplitude [3].
~ I02-I03P'S'I.
. ~2~
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~O b
- - ~ . 0
4.0 ~ \ 8.
�
`
, .
~0
~ 0
~ i
-~40 '
Z tg, crX
!.0 /
?
i
i
O ~
! dWE/qt(N~T)'~
~
10"i 60 ; ~ JO
i
-!0"Z ' 1
~
r
~ f �13.0 xHi
^-Kp~l �.~~....~Kp=y ---KpaS I
Figure 2. Beam trajectory parameters as a function of .
latitude
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FUR Ur'r'1~lEw u~,: vLVLi
Obviously, the turbulence develops ~.n the region o~ m~.ni~tnum value o� P,
whereas in the reg~,ons o~ the maximum, energy trans~exred to the~wave ~rom -
the plasma and a buildup o~ its amplitude take place. :It is eas}* to find the
explicit forin
p~ (~E)~NT~. ~E~r'}'~'9 ���.d (NT~ ~3)
where Y is the increment (the decrement) of the system wave with an amplitude
of E; u, ut are the phase and group indexes of. refraction and a is tt~e anglc
between the group phase wave velocitiea. The calculations, part of which are _
illuetrated in Fig 2 indicate that the length of the turbulent region is
1000 to 3000 km, and its position is shifted toward the beginning of the
tra,jectory with respect to the point where w=wgecos This means that the
wave energy absorption takes place not on the cold, but on the low-energy
_ electron component with characteristic energies of ~0.1 to 5.0 kev. Fig 3
- shows the results of the tra~ectory calculatinns for several frequencies,
La4.0; Kp=1 and the standard model of the electron concentration with base
level at the altitude of 1000 lan, Nep=1.5�104 cm 3. The circlea indicate
the minimu.m values of P, and the x's, the region of disappearance of the
wavg (E/E
x
~
- ~
? q,lf' _
~
~ ~3~
~ ~ ~ ~
f
JOD Bp~n~,crK 19D
Figure 5. Slant range to the refZecting formatons and reflected
signal level as a function of time during the 14th in~ection cycle.
A diagram o~ the gun current is presented above.
Key:
1, sec 4. Signal level
2. Time, sec 5. Gun current
3. Range, lan
During the p~riod of injection of electrons with an energy of 27 kev the gun
operated without breakdowns in practice for onlv one (II) cycle. The delay
in this cycle was approximately 2.3 seconds. On the 14th, 15th and 16th
cycles (13 kev) the delay was 2.52 to 2.64 seconds. The plasmogenerator was
switched off before the 17th cycle. Obviously, this is conriected with an
increase in the delay to 3.5 seconds. -
As a result of breakdowns of the gun in the electron injection mode with an
- electron energy of 27 kev there were cases where the in~ection time turned
out to be less than 1 sec:. 0.1 to 0.7 sec. In these cases delays were -
observed of 0.7 to 1.0 seconds. -
Thus, it turned out that on injection of the electron beams. with the param-
eters uaed in the "Araks" experiment the particle eruptions in the magnet- '
ically con~ugate region occurred with anomalously large delays. It should
be expected that on electxon ~,n~ection along the rocket axis, that is, _
with pitch angles o~ 10�, the particle erupti,on in the northern hemiaphere
had to occur with delays of about 0.6 and 0.8 sec, respectively, for parti-
cles with energies of 27 and 15 kev. However, with the exception of
several cases of the in~ection o~ short pulses as a res~slt of breakdowns of
the gun, the delays turned out to be greater than expected by an amount
somewhat exceeding the b4unce period of the inj.ected particles.
175 -
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' L'VI~ VL'l l~Il[ll.~ V~.~ VIYLl
4
. .
y ' ~
4 ~ �
O
5
O 1
~O �
' ~ �
b
1
~ ~ ~
Q ~ �
~ t 1 ! 4
~2~ ,~If11~iMMOdA1 ilIWCtK4L1/,ClX ~
O-7~~ r
Figure 6. Delay in the occurrence of reflections (eruptions of
particles) in the northern hemisphere with respect to the injection
times on board the "Eridan" rocket in the northeriy launch.
0� and 70� injection on the rocket axis and at an angle of 70�
reapectively.
Key:
1. Delay, seconds
2. In~ection time, sec
' In addition to the anomalously large d~lay, also a type of "aftereffect" was
observed particle eruption from tubes of force disturbed during the injec-
tion time continued appreciably longer than the injection time by 10 or
, more seconds. Thus, on the 14th cycle the reflections from the range inter-
val of 430.5 to 434 lmn during which the particles were injected along the
rocket ax~[s for 3.84 seconds, continued with some interruption for 16.8 sec.
It is noteworthy that no particle eruptions from the range interval of
427.5 ta 42g lan, that is, from the tubes of force in which the particle
in~ectian was realized at an angle of 70� to the rocket axis, was detected
in practice.
The observed cases of quite rapid variation of the slant range to the ref lect- -
~ng formation are of significant interest. For example, in the time interval
of 286.8 to 286.92 sec (Fig 7) a short-term increase in the slant range by '
3.5 km occur.red. This variation of the slant range indicates that there are
quite fast shifts in the region of intrusion of the particles perpendicularly
~ to the e~rth's magnetic f ield. Indeed, in all probabYlity the dispersion -
of the radiowaves connected with the particle eruptions with an energy of
13 ~Cev occurs at an al~itude of 110 km. The results of the ot~servations
during the first launch demonstxated that when the calculated deviation of
- the radio beam from the normal to the earth's magnetic field exceeded 2.5�,
the intensity of the echo decreased below the detection threshold of the
equipment. If we propose that the observed variation o� tl:e slant range
is connected with variation of the posit~.on o~ the scattering region along
the magnetic field (along the line o� ~orce) and not across it, this leads
to an increase in d~viation o~ the radio beam from the normal to the magnetic
f ield to 14.5� and variation of the altitude (an increase in it) by 55 km. .
176 -
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- : : .
. . . . . - ~ - . _
- --~.---~-�~--~r-. ~ ~
~ ~ ~ . . .
~ ' ~ . ~ - , _
~-...~......r.;.~:~ . � _ ~ - . _ KH
~ ' ' ' � ` ' ' ' - � 47~3
r . . ; ..,r - y ~
� . ' ; ' � +'~.r: ,;i. 's r �;+..ri~,.. .r.,?;
, . . , . , ---�.~,...41f.~
~ ~ � ~ � � � �
~ + t.: ~iY. . ~~�1 : .
. � ' ! � ~
~ ? � ~ � ~j i T~ ~ ~ .
. . � � : : , j . � .
~t ' j'i~~`~. � , . , . ,''I
1~ � e~i--~~...1.~~
1I7 10I
B~lfMA ~ C!K ~1~
Figure 7. Example of the short fast variation of the slant
range to the particle eruption region.
In 60 milliseconds the reflecting region at an altitude of
about 110 1~ was shifted perpendicularly to the earth's mag-
- netic field by 3.5 km to the north, and then at the same time
it returned to the initial position.
Key:
1. Time, sec
The probability of recording the acattering of the radiowaves with such
deviations from orthogonalness is negligible.l In addition, the auroral -
scattering under natural conditions occurs below 135 lan. Thus, the case
rresented in Fig 7 indicates that from 286.8 to 286.92 seconds brief dis-
placement of the region of intru~ion of the pazticles acroas the magnetic
field was observed with a velocity reaching 58 lan/sec ,:he northerly direc- -
tion at an altitude of 110 km: the reflecting region shifted in 60 milli- '
aeconds at an altitude of 110 km to the north by 3.5 lan, and then ~!n the
same time it returned to thc initial positiori.
The experimentally observed, quite fast shift of the reflecting formations
acroas the magnetic field, which is of independent interest, permits some
conclusion tn he draw~n about the aftereffects. F?rom the case presented in
Fig 7, it ~s obvious that tiie reflecting formation, shifting to the north, -
occurs at each point in time at a new place. In the old location it can
disappear after 20 milliseconds. Thus, the aftereffect is connected m~re
with the fact that the particle eruption from the tubes of force di,sturbed
_ previously as a result of operation o� the gun continues with interruptions
for some time, and it is not connected with the large~li~etime of tfie dis-
' ~ersing ~ormaticas. -
COPYP.IGHT: Kol'skiy filial AN SSSR, 1978
[g1~+4/1072-10845]
lA. Kh. Pyatsi, "Auroral Scattering of Radio Waves," RADIOAVRORA (Radio Aur-
c~ra), Moscow, Nauka, pp 200-298, 1974.
10845 -END-
GSO: 8144/1072
. ~77
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