JPRS ID: 9817 SUB-SAHARAN AFRICA REPORT

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JPRS L/10079
28 October 1981
Translation
FINESTRUCTURE AND SYNOPTIC VARIABILITY OF THE SEAS
- Ed. by
A.M. Aytsam
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. JPRS L/10079
28 October 1981
FINESTRUCTURE AND SYNOPTIC VARIA~ILITY OF THE SEAS
Tallinn TnNKAYA S~rRUKTURA I SINOPTICHESKAYA IZMENCHIVOST' :~:ORF.Y in
Russian 1977 (signed to press 23 Oct 80) pp 1-200
jText of bo~k edited by A.M. Aytsam, Ee~ti NSV Teaduste Akadeemia,
1980, 2~0 copies, 200 pages]
CONTENTS
Foreword . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 1
Finestructure of Deep Waters of the 4pen Part of th~ Baltic Sea, by
A. Aytsam, Ya. Laanemets, M.-Ya. r.ilover . . . . . . . . . . . . . . . . . . . 2
Spatial Variability in the Temperature of the Surface Layer of the Baltic Sea,
by A. M. Ayatsam, Yu. Kh. Pavel' son . . . . . . . . . . . . . . . . . . . . . 5
Investigation of the Variability of G~rrents on a Synoptic Scale in the
Central Par.t of the Baltic Sea in 1977-1980, by A. Aytsam, L. Talpsepp 9
~ Results of STD Mapping in the B~DSEX Traverse on the Baltic Sea, A. Aytsam,
Yu. El' ken . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 13
Finestructure of the Thermocline in the Ocean, by.V. S..Belyayev 17
A Nbdel of Interstratified ~rbulence in the Ocean, by V. S. ~elyayev,
R. V. Ozmidov . . . . . . . . . , . . _ . . . . . . . . . . . . . . . . . . . . . . . 21
Syno~tic Variability of Equatorial Currents in the Pacific ~cean, by
V. A. Bubnov, D. Yegorikhin . . . . . . . . . . . . . . . . . . . . . . . . 25
Vertical Structure of Ctiirrent Velocities and Internal Waves in the Ocean,
- by Ye. P. Varlatyy, V. V. Navrotskiy, I. D. Rostov . . . . . . . . . . . . . . 29
Some Results of Synchronous Measurements of the Vertical Structure of
Temperature, Salin,ity, Speed of Sound and the Current Vector Velocity,
by Ye. P. Varlatyy, I. D. R,~stov . . . . . . . . . . . . . . . . . . . . . . . 33
- An Acoustic Measuring Complex for Research on the Microstructure of
Hydrophysical Fields in the Ocean, by Ye. P. Varlatyy, V. P. ~'ikhomi.rov 36
Possibilities for Studying Finestructure and Turbulent Pulsations of the
Ocean's Density Field With a Laser Photoelectric Interferometer, by
V. D. Vlasov . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 40
- a - (I - USSR - E FOUO]
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The Diversity of Physical Cycles in the Upper Layer of the Ocean, by
A. I. Ginzburg, K. N. Fedorov . . . . . . . . . . . . . . . . . . . . . . . 45
Internal Waves and Turbulence in Synoptic Eddies Accordix~g to Data on
Vertical Finestructure,by V. Z. Dykman, O. I. Yefremov, 0. A. Kioyeleva,
~ N. A. Pantaleyev . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 49
Transformation of the Fnergy Density of Internal Waves in a Synoptic Eddy,
by V. Z. Dykman, A. A. Slepyshev . . . . . . . . . . . . . . . . . . . . . 54
Interpretation of KhVT Data in a Statistical Analysis of Density Field
Variability, by A. I. Yermolenko . . . . . . . . . . . . . . . . . . . . . . 58
Numerical Models of Synoptic Variability in Deli~ited Regions of the Oceans
and Seas, by V. M. Kamenkovich, V. D. Larichev, B. V. Khar'kov 63
Simulation of the Upper Quasi-ikziform Layer, by T. R. Kil'matov,
S. N. Protasov . . . . . . . . . . � . . . . . . . . . . . . . . . . . . . 66
Current and Average Three-Dimensiona"~ Spectrums of Synoptic Variability
of a Current Field, According to "Polyirode" Data, by K. V. IGonyayev,
K. D. Sabinin . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 70
A Model of the Dynamics of an Isolated Synoptic Eddy, by G. K. Korotayev 72
~xperimental Research on Synoptic Eddies in the Open Ocean, by M. N. Komlyakov 76
~ �
Free Rc~ssby waves as a Factor Responsible for Fluctuation of Synoptic-Scale
Oceanological C`haracteristics (Using the Kuroshio and Oyashio Waker
Systems as an Example), by L. K. Kramareva . . . . . . . . . . . . . . . . . 78
Nbdeling the Water Temperature of the Baltic Sea, by T. Kullas, R. Tam;alu 82
Spectral Structure of Vertical Temperature Nonuniformities in ~the Oc;ean, by
I. D. Lozovatskiy, N. N. Korchashkin . . . . . . . . . . . . . . . . . . . . 87
A Particular Nbdel of Turbulence Interstratification,.b~ M. M. Lyubimtsev 91
Use of Dynamic Stochastic Nbdels for Integrated Treatment of Oceanological
Measurements, by V. A. Nbiseyenko . . . . . . . . . . . . . . . . 95
The Concept of Finestructure and Its Discrimination in the Ocean, by
V. V. Navrotskiy . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 99
Intrusions and Differentia~-Diffusional Convection in Cromwell's Current,
by V. T. Pa.ka . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 102
Apparatus for Studying the Finestructure af Hydrophysical Fields, by
V. T. Paka . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . > 106
Activation of Small-Scale Turbulence by Internal Waves in the Presence of
Fine Microstruc~ure, by Ye. N. Pelinovskiy, I. A. Soustova 110
5pace-Time Spectrum Analysis of the Temp~erature Field of "Polytmde"
Traverse, by V. G. Polnikov . . . . . . . . . . . . . . . . . . . . . . . . 114
Laws Governing the Distribution and Variability of the Characteristics of
the Thermohaline Finestructure of the Northwest Pacific, by I. D. RQStov 118
-b-
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73iisotropic Spectrums of Wavef~riri Turbulence in the R-Plane, ny A. G. Sazontov. 120
Eddy-Resolving Numerical Nbdels of Ocean Currents, by D. G. Seidov, _
K. K. Rusetskiy . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 125
Formation of the Synoptic Variability of Seas Experiencing Free and
Limited Exchange With the Ocean, and the Problems of Its Computation
and Prediction, by Yu. V. Sustavov . . . . . . . . . . . . . . . . . . . . . 129
Linear Reaction of a Stratified Ocean to a Moving Tropical Cyclone, by
G. G. Sityrin . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 134
A New Viewpoint on Fronts in the Ocean, by K. ~1. Fedorov 139
Simulation of Hydrodynamic Processes in the Sea Wa.th a Model of lmtationally
Anisotropic Turbulent Flows, by Ya. Kheynloo . . . . . . . . . . . . . . . . 143
A Cascade Model of Turbulent Diffusion, by Ya. IQzeynloo, A. Toompuu 147
Investigation of the Fir.estructure of Hydroghysical Fields by a Remote
Acoustic Method, by V. P. Shevtsov . . . . . . . . . . . . . . . . . . . . . 152
, The Mechanism Behind Finestructure Generation by Narrow-Spectrum Internal
Wave Trairs, by V. I. Shrira . . . . . . . . . . . . . . . . . . . . . . . . 156
List of Authors . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 160
List of Abbreviations . . . . . . . . . . . . . . � � � � � � � � � � � � . . 160
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FORE4VORD
Ir~ recent decades oceanologists have established presence of significant variabilit,y
in ocean waters, embracing from several seconds to seve~al years in time, and from
millimeters to thousands of kilameters in space. Variability of ocean waters is
elicited by various physical processes= however, the laws of these processes are
not always sufficiently well known.
Scientists of the Baltic Sea Division of the Institute of Thermophysics and Electro-
physics began intense.research on variability af the Baltic Sea in 1976. Expeditionary
research conduct~d aboard the scientiFic research ve~sel "Ayu-Dag" also established
- significant variability in waters of the Baltic Sea. In 20 trips made in 4 years,
many typical traits af the variability of B~ltic waters were dete~mined, especially
- i.n regard to finestructure and synoptic variability. The necessity for extracting"
optimum information from the accumulated experimental material, and for critically .
discussing the obtained results, led to the idea of holding a seminar-symposium on
the finestructure and synoptic variability of th~ seas and oceans.
The idea of conducting such a semi,nar-symposium was appr�oved by the scientific
society of oceanologists, as is evi3enced by the present collection of report
summa.ries .
Discussion of the latest Xesul~s oF research o;~ variability of the World Ocean at
different scales, and comparative analysis of these results and intormation on the
variability of the Baltic Sea will probably promote further development of research
on variability of the seas and oceans.
The report summaries were placed in this collection in the form in which they wEre
submitted by the authors. Therefore the editor of this coll~ction claitns r~o responsi-
bility for misprints and mistakes in the text.
1
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Finestructure of Deep Waters of tkie Open Part of the Balt~.c Sea
A. Aytsam, Ya. Laanemets, M.-Ya. lGilover
Introduction
The open part of the Baltic Sea may be divided into four Iayers in relation to
vertical temperature distribution: an upper iaixed la~?e�r, the thern?ocZine, an
intermediate cold winter--convection layer and an abyssal layer (halocline)~ The
average structure of watrer in the abyssal layer is governed by intrusion processes
through th~ Danish straits (saltier and warmex wate,r enters the sea! and by v~ertical
exchange pro~esses. Research on processes occurring in the marine environment and
ass,essments of vertical exchange of scala~r magnitudes make broad use of the results
of vertical soundi.ng of temperature and sali:~ity fields with salinity-temperature-
density probes. Vertical structure may be interpretec~ as iche result of the inter-
action of differPn~ processes, ones which often overlap in scale. These problems
are reviewed in (1,2,3,4).
Measurements and Analysis Procedure
Several series of vertical soundings were made with a Mark III Neil Brown probe
at the central station of the BOSEX traverse in 1979 and 1980 in order to study
verticalsatructure formation in the abyssal layer of the Baltic Sea. In spring 1979
six series of 30 soundings each, in an interval.of deptlzs from 70 t~ 95 meters, were
made from aboard a c~rifting vessel in sti).l weather. Following each series the
- vessel returned to its startir.g point. The vessel..drifted 1-2 km. The time inter-
val between soundings was 3 minutes.
In spring 1980 two series of 20 soundinqs ea.^.h were made in the BOSEX transverse in
an intsrval of dePth$ from 60 to 90 meters and a time ~nterval of 3.5 minutes. The
- first series was completed before a storm, and the sec+~nd series was completed
3-4 days following the end of an 8-9 point storm.
The probe was lowered at a rate of 25 cm/sec, and the recording rate was 3a tintes
per second, which made a depth resolution of about 1 cm possible. During init,~.al
treatment, all readings were interpolated to a oonstant interval of 2 cm. The
measured series was divided into an average and a pulsating component with the
help of a cosine filter.
2
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~he BPF [not further identified] method was used to coarpute spectral densities ~
following preliminary smoothing with a fenr-poin~Ka~iser-Bessel. fi2ter (5) .
Discussion of Re~ults
The influence exerted by shores and the Danish straits may be assumed to be low
within the area of the BOSEX traverse. The vertical temperatnre, salinity and
density profiles varied monotonously with depth in the .interval fram 60 to 95 meters.
It was hypothesized that wave-generated vortical turbulence, laminar convection
(because temperature and salinity increas~ with depth in the Baltic Sea's abyssal
lay~r) and the kinematic effect of internal waves are the prinaipal processes
fo~uing the vertical structure of scalar magnitudes at the'fixiestructural aund
microstructural levels. Mc>reoasr when t'~e iirst two processes occur, they are
accompanied by vertical transport of scalar maqnitudea.
Zb determi.ne the oonditio~s under which lac~i~aar convection occurs, we calcslated
the function Rp~ZZ~ = S( )L1S' with the ver~ical interval being ~Z = 10 cm. Analysis
r~ ( ' ) d2'i
of the function Rp(ZZ) showed that Rp(ZZ) < 15 only at some specific points of the
vertical profile, and that for the most part Rp(Z~) ~ 15, which implies purely molecu-
lar diffusion. Of vour~e, a final.conclusion as~to the importance of laminar con-
vection to vertical transport in the abyssal layer of the open part of the Baltic
Sea would require analysis of greater detail. One more thi~ng we should note here
is that in double-diff.usion processes, the a~ass fl0w is directed cbwnward, which re- ~
quires additional upward turbulent flow or vertical transport.
The BPF method was use3 to calculat~ the spectre3.~densities of vertical discontinuities
in temperature, salinity and specific gravity. Z'he maximum wave number is
Ku =1/2~Z = 25u'l. A transition zone bounded by wave numbers 3~H is the mean number of turbulent layers
in a unit interval of depths, we qet 6� 10-2 cycles/meter,
Et/Tz = 4.6�10-~K'3�1, where Tx is the mean vertical temperature gradient.
The results of ineasurements made in the ocean showed that depending on the relation-
ships between the parameters defining the conditions of small-scale fluctuations
in temperature, the finestructure subinterval in spectrum Et(K), where E~= A~~K3~ ,
(A = 4. 5� 10- 3), may tzans form directly into a buoyancy interval ~ where ET�:.c, ~ T; p' K
or into an inertial-convective interval ~T ~tET E4~ K~i� or into a viscous-convec-
tive interval (Et S~r ~K', Here, a 1, a2 , a 3--universal constants, Eu--turbulent
_ energy dissipation rate, Et--temperature nonuniformity equalization rate,
buoyancy parameter, t~, _(v/E) 1~Z--IGolmogorov's time sr,ale, ~--coefficient of mole-
cular viscosity. Taking account of the asymptotic nature and differences in dimen-
sions of spectrum Et(K) at large and small K, Lozovatskiy (1) obtained expressions
desci~.bing spectrum E(K) in the transitions from the finestructure subinter~,�al to
one of the :urbulence subintervals. These expressions contain typical scales Lt
L~ and Lt separating the finestructure interval from the bu,oyancy, inertial-convec-
1 tive and viscous-convective intervals respectively:
,
~T = T - - .
~ L
y: . T
. ctE _~ya, fie ~ . LT ~ ~s~~ tL fia .
and cl, c2, eg are dimensionless constants dF~fined as follows:
s
~ C~ _ ~ A/~�) _ /s ~ � (A~'~ 2~ .
C ~ � ~A~'~ _ yt ' ,
.
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Measurements of the vertical structure of the temperature field and simultaneous
observations of the internal wave field shawed that in the finestructure interval,
spectrum Et(K) =~IC-3 for sufficiently well developed short-perind internal waves,
while for waves of small amplitude, Et(K)tiK-~4-5~, and the spectrum is characterized
by a lower level. It may be possible that confluence of the internal wave field
is precisely what causes smoothing of inesos~ale nonuniformities in profile T(x).
However, we still do not have a firm idea about the dominant mechanisms responsible
- for the form of spectrum Et(K) in the range of scal~s,,from 104 to (102-101) cm.
Therefore, staying within the framework of dimensional theory, we will attempt to
reveal the dominant parameters that may indicate the mechanisms responsible for re-
distribution of the deviations of temperature fluctuations in relation to the scale
spectrum and making it possible to obtain an expression by which to describe the
average spectrum at KKp respectively. The interpolati:oh formula for Et(K) for the entire
range of scales under examination may be representec? as follows:
,E r~K) '~t ~ t~'- ~ K 3 C~
4~ 1 .(3)
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where scale LT is defined as L=(yl/Y2) z/Ta. At L.~K�i, Et(K) is described by
formula (2) , while when LTK�1, it is described by formula (1) . According to the
available data, [symbol left out; possibly L.~] varies basically within 10 and 20
meters. Zb directly confirm the possibility of using expression (3), we would
need to calculate parameters 2~z, T and ~`z using experimental data, and determine
dimensionless constants Y1 and Y2. Z'he first infozmation on nonuniform distribution
of the heat flux of a therimcline, obtained by means of instrumental measurements,
is presented in (2). Heat flux estimates were obtained in (3) with the help of
indirect calculationG for individual layers; these estimates also vary noticeably
in relation to z; at present, however, direct instrumental measurements of vertical
profiles u'tJS(z), suitable far appraisal o~ T and Tz, are unavailable.
Expression (3), which 3escribes spectrum E~(K) in the finestructure interval, and
formulas obi.:ained in (1) for the transitional area between the finestruc~ure inter-
val and one of the subintervals of small-scale turbulence, permit us to derive
general interpolation formul~s for spectrum Et(K) within the entire range_of wave
numbers--from 10-4 to 10~ cm 1 Naturally in this case the combination AT~ in the
2:~-1. Z'hen, de-
expressions for scales L~, Lt and Lt~ must be substituted by Y1~z
pending on whether the finestructure interval i.:s followed by the buoyancy, inertial-
convective or viscous-convective interval, the spectrum of tei:lperature nonuniformi-
ties Et(K) would be described by one of the following equations:
ys -~s r ~ k A+~ k 1 (4)
ET(K~~ ~~~V~� K L,* ~.TK ~
E ~ ec F. y~ K'~s Lt ~K/
!~L ~c ~ (5) '
r t T ~ (
~t ~w3 .
~ , (6)
E7 ~r~ ''~s ET t'~ K+. L(? L ~~,K , ,
~onsidering that LT>Lt, Lt, Lt~; at LTK�1 these formulas reduce to expression (1),~~
at LTK�1 and at LTK or L~C, L~� 1 we get the "power of negative three interval,
as represented by formula (2), and at L~f, LtK or L~K�1 we get one small-scale
turbulence interval or the other. In those cases where scale L* is found to be
greater than the typical scales of defozmation of inean temperature and velocity
fields--L.~, the buoyancy interval would be absent from the temperature nonuniformity
spectrum, and the general interpolation formula for Et(K), describing a succession
~f intervals with powers -2, -3, -5/3 and -1 with growth in K, would be written ir.
the form:
-S'3 ~f!' L~R~ lalek~ +/LtK~~s,~~7)
~~~C, f~L~TE ~'i' ~ t ( t K~ \
where Le' ~~~~~e~ ~ti ~ and '~`~~~~y, --K'�lm�gorov's scale. Depending on the x.ela-
tionship between the sizes of scales LT, Lt and LE in spectrum Et(K), both the
finestructure subinterval, where EttiK-3, and the inertial-convective interval may
be a.bsent. Tlie r~sults of comparing these formulas with the experimental data
showed the pcissibility of their use to describe Et(K) spectrums in an ocean thermo-
cline.
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We should note i.n conclusion that if we take the approach indicated above in our
analysis of the spectrums of vertical finestructure nonuniformities in the velocity
- field, then at K"1>LT spectrum Eu(K) may have the form:
E~,(~ ~ ~~z K-2 ~ (e)
' where c is a certain constant. The available in�orn~ation on Eu(g) spectrums calcu-
lated on the basis of ineasurements of the finestructure of the ocean's velocity
field, indicate~ that at K'1>8-10 meters, in a nuaiber of cases we observe a scale
intezval for which Eu(K)tiK-2. Inasmuch as LT is close to 10 meters, use of expression
(8) to describe Eu(K) may probabl~ he justified in these experiments.
BIBLIOGRAPHY
1. Lozovatskiy, I. D., "The Spectrum of Vertical Nonuniformities in the Tempera-
ture Field of the Ocean Thermocline," IZV. AN SSSR, P'A0, Vol 15, Ido 11, 1979.
2. Lozovatskiy, I. D., and Ozmidpv, R. V., "Statistical Characteristics of the
Local Structure of Developed Turbulence in the Kuroshio Current," OKEANOLOGIYA,
Vol 19, No 5, 1979.
3. Lozovatskiy, Z. D., and Ozmidov, R. V., "The Relationship Between the Character-
istics of Small-Scale Turbu~ence and the Paran?eters of Water Stratification in
the Ocean," OKEANOLOGIYA, Vol 19, No 6, 1979.
4. Gregg, M. C., "Variations in the Intensity of Smallscale Mixing in the Main
Thermocline," J. OF PHYS. OCEANOGR., Vol 7, No 3, 1977.
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A Particular Nbdel of Turbulence Interstratification
M. M. Lyubimtsev
Signals representing variables (pulsations in velocity, temperature and so on)
measured in experimental research on ocean turbul~nce are recorded by low-inertia
sensors in the form of a succession of pulses (of varying shape and width) separated
by noise intervals of irregular duration. Such pulse modulation of ~ignals is the
consequence of turbulence interstratification. An elementary model is suggested
for description of such signals. It is used as a framework for exar,~,:.zing the
influence of interstratification parameters on some statistical characteristics
of small-scale turbul.ence.
Let us examine random process ~(t), which is the produ~t of stationary random
process u(t) with a mean = 0) and pulse process I(t), in which the time of
arisal ti and duration AZ of the i-th pulse (i = 1,2,...) of unit amplitude are
random. Process I(t) may be represented in the form I(t)=EI2(t), where IZ(t) is
the i-th pulse located randomly on the time axis. Then pro~ess ~(t) may be written
in the form _ , . .
- ~ ~;,(t) t( t=~`=} ~ ~ ~c~~)~~ ' ~ iI~
, ~e~ .
, .
Here' j(x)~ ?~(x)-'w(x-1), 9G(x) is. Heavi"side's unit function. Argument x= (t-t2)/62
was selected in such a fashion that as t varies from t2 to t2 + Au -that is, within
the limits of the 2-th pulse, x varies from 0 to 1; in this case I(x) = 1. Outside
the limits of pulses, I(x) = 0. We will tr2at process ~(t) as a model of a uini-
dimensional section of the turbulence field.
To calculate the statistical characteristics of process ~(t), we would need to
introduce a number of hypotheses on its probability structure: 1. The probability
that exactly n pulses would arise in time interval T depends on T but not on the
position of this interval on the ~:ime a~cis--that is, uniformity of the pulse
process is presupposed. 2. The number of pulses arising in nonintersecting time
intervals is independent of random variables--that is, there is no "after-effect".
3. The probability that more than one pulse would arise in a sma11 time interval
dt is one order of magnitude less than dt--that is, as dt-+0, this probabilxty
becomes equal to 0(dt). From a physical standpoint this means that arisal oF
_ two pulses simultaneously is impossible. 4. All tti(t), tZ and 62 are statistically
91
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independent from one another, and their probability distrinutians do not depend on
the pulse number. It may be shown that under these conditions the probahility
- P~(n) th~t n pulses will appear in time T wou~d be desc~ibed by a Poisson distribu-
tion wit-h intensity a =