SCIENTIFIC ABSTRACT LAYKHTMAN, D.L. - LAYKHTMAN, D.L.

• Document Type: CREST
• Collection: Scientific Abstracts
• Document Number (FOIA) /ESDN (CREST): CIA-RDP86-00513R000928830014-6
• Release Decision: RIF
• Original Classification: S
• Document Page Count: 62
• Document Creation Date: November 2, 2016
• Document Release Date: June 20, 2000
• Sequence Number: 14
• Publication Date: December 31, 1967
• Content Type: SCIENTIFIC ABSTRACT

Problems in the Physics (Cont.) sov/4641
experimental investigations given. Individual articles analyze the
temperature regime of the active surface of soil and the factors determining
the thermal conditions of the boundary layer. Results of fog investigation
are presented in two articles. In addition,..some problems of methods in
the experimental investigation of the near-surface layer are-elucidated. No
personv21ties are mentioned. References follow each article.
TAME OF COMNTS:
La7_kj&tmszT-DwL-. Yztrmulation of the Problem of the Stationary Structure
R-the Bo~ndary Layer 3
Tseytin, G.Kh., and L.R. Orlenko. Stationary Distribution of Wind, Tem-
perature, and Turbulent Exchange in the Boundary Layer Under Differeut
States of Stability 8
Ariyell, EA., and L.A. Klyuchnikova. Wind Under City Conditions 29
Klyuchnikova., L.A.., and F.N. Shekhter. The Role of Radiant aLd Turbulent,
Heat Exchange in the Formation of the Tempi-rature Stratification in the
Boundary Layer 33
C ard 2/41

8661,h
S/05Y60/000/012/002/005
054
AUTHORS.: Laykhtman,_D. L. Shnaydman,,Y. A.
TITLE:- Criteria for a Ste'adyj Turbulence in Jet Currents
FERIODIWI: Meteorologiya i, Sidrologiya, 'v960, No. 12, pp. 11 13
TEXT: Tha authors.describe %h e~relationship between the parametero of
turbulenc'e and the meteorological elements measured i 'n the aeroloGical
network.- They give a formuln. for the gradient wind-in the region of jet
currents-,--to-~ cal-culate-,'Uhe--turbul,-ne-le. coefficient k, the wind- tur ulence
2
cl U
and 'the-thickness 2H of the turbulence layer, they use the equations
of motion, as well as the equation for the equilibrium of turbul 'ence
energy given.in Ref-.2 (talking account of the dissipation of turbulence.
energy in heat). Fig-I bhows a diagram for 'uh6,,dimensionless ouantities
k.,~, H., and x. x is a parameter whilch can be determined from a trans-
2
a
k
.:cendental equation given here. k)~ :4 a nand H ' aH X 2n.
-i'T
z
.,,,-..,.Card 1/2

86644
Criteria for a Steady Turbulence in Jet S/050/60/000/012/002/00r-
Currents 3012/BO54
All',c.alculations can be made with ~he~ aid of this diagram. The authors
used the data of Ref.1, and calculated. the characteristics of turbulence
for the jet current in the area ofIL"eningrad. The results agree.with the
experimental datai n and x-are functions of a certain parameter M which,
in its physical meaning, approximately corresponds to Richardson's number.
n can also be determined from a transcendental equation givenhere. There
are I figure, 1 table, and 2 Soviet referenGes.
X
0~ X
Fig.1
1,0101
a
Card-2/2
-,Nr- 1.
1 2 3 z tv

LHUTMAN, D.L.; KAGAII,IZ.L.
Some problems associated with improved organization ofinow
surveys. Trudy GGO no.108:3-18 160. (MIRA 13:11)
Onow surveys)

uynnfa, David L'vovich; VIJZOVA, Yu.V.,.red.; SI)OVEYCHIK, A.A.,
tekhn. red.
[Physics of the atmospheric boundary layar] FAzika pogranich-
nogo sloia atmosfery. leningrad, Gidrometeor.izd-vo., 1961.
252 p. (MIRA 15:1)
(Meteorology)

S/169/61/000/012/064/OC9
D228/D305
AUTHORS. and Utina, Z. M.
TITIE: Influence of macrometeorologic condition.~ or
the structure of the boundary layer in the
atmosphere
PER70DICAL: Referativnyy zhurnal, Geofizika, no. 12, 19F'~
46, abstract 12B282 (Tr. G1. .-eofiz. observ.,,
1961.. Tio. 107, 14-20)
TEXT: The distribution of the main meteorologic elements
and turbulence characteristics in the boundary layer was ob-
tained by means of solving the joint system of the equations of
movement, heat inflow, water-vapor diffusion, and ground ther-
moconductivity. To close the system, the equation of the tur-
bulence energy balance was used in an integral form for the
whole boundary layer. The coefficient of turbulence is as3i,-,r-.-
Card 1/2

S/1169/61/000/012/064/080
Influence of macrometeoroiogic..0 D228/D305
to thellmodel with a fracture." On the basis of the derived
formulas, appraisals are given for the changes in the profiles
of meteorologic elements in the boundary layer and in the com-
ponents of the heat balance during the variation of the radia-
tion balance, and also for the degree of humidification of arn
active surface and its roughness. Z-Abstracter's note,- Com-
plete transiation.2
Card 2/2

KLYUCHNIKOVA, L.A.; IAYUT,'4AN$ D.L.
Some characteristics of dli-nal wind velocity variations according
-to the data of the 14%khtaly Expedition. Trudy GGO no*107:52--54
161. (MIRA 14-.10)
(Winds)

IAYKHTM&N.,.D.L.; KAMAN., R.M.; UTINA, Z.M.
Experimental determination of radiant flow of beat into the
lower atmospheric layer. Trudy GGO -no.107:112-115 161.
(MM 14:10)
(Atmospberic temperature)

43068
S/531/62/0('-`--V/006/007
1053/1253
AUTUORS: Lay'khtmans D,Lop Dritnero E,lt,,
T ITITZ: The problom of titrbulonoo In the free atmosph;re
S OURCE Leningrad. Gltsnaya goofizicheskaya observatori"ao Trudye
no. 127o 962. Fi,7,11ca prizarmogo sloya vozdukha, '122-126
TEXT: A totn]. exprejaion is obtained for 'the -mind speed In a jot
stroam In terms of an arbitrary law conc6rnIng the change of the
iorizontal pressure gradient with sltitnide - z9 The vertical pro-
f Ilen of t'hr rilne. ard its degree of Vistiness when f (z) = b(z) and
the c-ise of the presence of a strong leap In horizontnl grad-
lant, of pressiire over a narrow interval of altitudes when u (z)
b(,-.),, ire calculntedo According to the-formulne obtained, Sthe
vn2uo,.j of the coefficient of turbulence k and of wind ustlness.oi
typie,,sl of the jet stream.. wore found to be k 500 m /a ec and
a
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LAYKHTYAN,,-D.L., doktor fiz.-matem. nauk, red.; MRONENKO, Z.I.,
red.; IVKOVA, G.V., tekhn. red.; ARONS, R.A., tekhn.red.
[Transactions of the All-Union Scietific Meteorological
Conference] Trudy Vaeroiuznogo nauchnogo meteorologiche-
skojtp soveshchaniia. Leningrad, Cidrometeoisdat.
Vol,,7. [Physics of tho surface layer] Fizika prizemnogo
sloia. Pod red. D.L.Laikhtmana. 1963. 319 P.
IMIRA 16:11)
1. Vaesoyuznoye nauchnoye meteorologichaskoye soveshchaniye,
Leningrad, 1961. 2. Glavnaya geofizichaskaya observatoriya
(for Laykhtman).
(Atmosphere)

UYUTMAN., D.L.
Diffusion of pollution from point sources in the lowest
atmospheric layer. Trudy Lan. gidromet. inst. no.15-.3-9
1630 (MIRA 17:1)
-5~

LAYKHTMAN, D.L.; KAPLAN, S.N.
Calculation of annual mean concentrations and the met-soro-
logical basis for selecting the height of factory chilmeys.
Trudy Ian, gidromet. inst. no-15:32-36 163. QURA 17:1)

WTZWt
LAYKHTMAN D,L GISINAp P.A.; KAPLAN, N.
Calculation principle of meteorologkoal conditicms in
planning industrial enterprises. Trudy Len. gidr6meti inst.
no.15:37-46 163. (MIRAI-17-.1)

ACCESSION NR: ~AR4015475
SOURCE: RZh- Geofizika, Abs. 12B300
AUTHOR: Laykhtman, D. L.; Shnaydman, Y. A.
TITIE: Turbulence in the ngion of jet streams
8/0169/63/000/012/BO54/BO54
-CITED SOURCE: Sb. Materialy* Nauchn. konferentsii po aviats. meteorol. M., Gidrome-
teoindat'. 1963, 43-52
.TOPIC TAGS: jet streams, geostrophic wind, turbulent pulsations, turbulence coef-
-Xicient, turbulent layer, temperature gradient, atmosphere, equations of motion
TW=TION: Equations establishing motion and equations of energy balance are
Aerived. The solutions of the equations of motion are constructe4 for the following
cases:'l) the velocity of Vne geostrophic wind does not depend on altitude, but is
'different'(changes by leaps) in the region of the jet streams (thickness 2h) and
above and below it; 2) the geostrophic wind is an.exponential t0unction of the alti-
itude. In both cases the pressure gradient is constant with altitude along the
direction of motion. -The atmosphere is assumed to be infinite in extent upwards and
rom the jet stream axis. Formulas are obtained for the coefficient of
downwards f

ACCESSION im: A'Wi5475
T.Lurbulence, the mean square velocity of turbulent pulsations and the thickness of
the turbulent layer (at the boimdary of this layer, from determinations, the vind
'~forthe first time attains the direction of the geostrophic wind). Graphics are
constructed for the computation of these values. All of these depend, in addition
to-the velocity-of the geostrophic vind an the vertical temperature gradient
determined in pract7kee, on the para_____ vhich, is proportional to the value of
the turbulent energy diffusion in the adjoining layer and its dissipitation into
heat. L. Matveyev.
ACQ i 09LTan64 SUB COM AS) PH ENCL: 00

LAYKHIY.AN, D.L.; BUTNER, E.K.
Determination time of the stationary, distribution of concen-
trations from a point source. Trudy Len. gidromet. inst. no.15:
97-102 t63. (MIRA 17:1)

MOM,
Scattering of passive particles from a point source in a
heterogeneous medium. Trudy Len, gidromet,.inst.-iio-&15:130-
136. 163.~ (MIRA .17: 1)

KAGAN', R.L.; LAYKfilliAN, D.L.
Optimum snow suinieying methods. Trudy GGO no. 112:78--86
163. (MIRA 17:5)

IAYXHTMAN, D.L.; ORLENNO, L.R.
Program and methods for observations nade during the
expedition. Trudy GW no.144:3-8 163. (MIRA 17:6)

LAYKH24M, D.L.; ORLENKO, L.R.; TKACHFITKO, A.V.
Dispersion of the turbulence energy in the lowest layer
of the atmosphere. Trudy GGO no.144:2E~-33 163,
(MIRA 17:6)

.-ACCESSION NR: AT4028745
S/2331/631000/144/008110084
AUTHOR: Laykhtman, D. L.; Kozakov, L.:,A.; Melentlyeva, I.
iTITLE: Experimental investigations of!the vertical changes of turbulence intensity
the boundary layer of the atmouphere
JRCE. Leningrad. G1. geofiz. observ. i Ukr. n.-i. gidrometeorol. inst. Trudy*,
no. 144/40, 1963. Fizika pogranichnogo sloya atmosfery* (physics of the atmospheric
boundary layer); Dneprovskaya exTeditsiya. GGO i UkrNIGMIj 81-84
~TOPIC TAGS: boundar layer, turbulancii. wind velocity, Dnieper expedition
~ABISTRACT: An attempt is made to evaluate the properties of the characteristic
vertical profile of turbulence based on pilot balloon observations. Information is
ipresented on the:vertical profile of wind gust velocity of the atmospheric boundary
!layer; certain dependences of the profile on the stability characteristics are
of spedally
.pc~jnted out. Experimental data were obtained by conducting a seriez
orkanized balloon.observ*ations from 6~bases. The results of the observations are
;presented in graphs.' Ustially, sharp changes in the gradients of wind velocity or
!temperature.(caused.by cloudiness or the passing of frQnts) strongly distort the
*.vertical profile of Wad pulsation., Pulsation mwdLm= is observed at an altitude of
1/2

'ACCESSION NR: AT4028745
ab,,>ut 2.5 km. A;minirm- of wind gusts,is observed in the layer from 750 m to 1500 m.
The elimination of pulsations above this level is obviously explained by the com-
parativelstabilit ~e 3 km. However, one should not draw conclusions
;y of layers aba
about the single,valued connection of turbulence in thelayer with the PIchardson
inumber at this le'vel. Such a connectipn can be substantially disrupted by the energy
Idiffusion of the turbulence of the upper and limer line layers. It is possible to
expecL that a satisfactory connection can be observed if thermodynamic uniformity
exists in. an adequately thick layer. ~A separate analysis of each series will be
conducted in one of the future articlei. Orij. art. has: 4 figures.
~.*ASSOCXMON: Leningradskay;4 glavaa.geofixicheakaya:observatoriya (Priuciple
Geophysical. Observatory of Leningrad)
SUBKMTED.% .00 .,DATE ADQ: 16Apr64..,,, ENCL: 00
;SUB CODE: AS 'NO REF SOV: OTHER: 000
Card 2/2-

JAYKEUMUx D - L. , PODOLSKAYA, E. L. * SHEKHTER I F. N.
"Radiative heat exchange in the boundary layer of the atmosphere."
report presented at the Atmospheric Radiation Sbyrap, Leningrad, 5-12 Aug 64.

ZILITINEEVICHY S. S.; LAYKETMAN, D. L.
"Turbule.Lt transfer in multiphase media."
report submitted for 2nd All-Union Conf on Heat & Transfer, Minsk, 4-12
I I may 1wi.
Voyeykov Geophysical Observatory

LAYKHTMAN, D.L., doktor fiz.-mat. nauk, prof.; RABINOVICH, Ya.s.
'04.4
Spraying toxic chemicals an'd ferUllzeru from airplanes. Meteor. i
gidrol. no.11:12-15 N 164, (MIRA -17:12)
1. Leningradskiy gidrometeorologicheskiy institut.

,,,LAYKHTMAN, D.L.; ORUENKO, !,.Ii.
Stru.-ture of the bouna"ary j~-Ye-- I
I . ~X the atm-"qphen e-, 'll ff,erent
lpti.lades. Iru6y GGO no.150.U"-10 16~. 17-.71)

- ~.f~YKHTMANP D.I.; BYU'PN-!:f?, RfK.
I.- - -
Turbulence -in J--t st-reams in the presence of -r- w-ind
sh!lfL. Trudy ~,iGO no.150t63-68 164. --17,7)

LAYKHTMkN, D.L.; RABINOITICH, Ya.S.
A Problem of thermal condufAivity. Trudy Len. gldrcmst. iMst
no.17:113-11-7 164. - (~aRA igso)

ZILITINKEVICH., S.S.; U.11MMAN, D.L.
Heat conduction and moisture excban-e in a turbulent atmosphere
a
in the case of phase transitions of moisture. DokI. Ali SSSR 156
no. 5:1079-1082 je 164. (MI'RA 17:6)
1. Glavriaya geofizicheskaya observat6ri7a im. A.I.Voyeyk-ova.
Predstavleno akademikom Yf.K.Fedorovym.

,LAYKEDIAN.-D.L., doktor fiz.-matem.nauk, Prof.; KAGAN, B.A.
Scheme Df precalculating the hydrologic characteristics at the
6;)a surface& Meteor# i gidrol, no,5t7-23 Mv 165.
(MIRA 18:4)
1, Glavnaya geofizicheskaya observatoriya i Leningradskiy
I Sidrometeorologicheakiy institut.

eAl Fiztka -1:
zv Y& atm6dery. a~,:v,~J;--now 21 1965, 150-156
4
Iii6-ttiibul6nd A.Za.
e. rdized Karnyin
-htmoaDherld krow veri!1jrene
fifimii~i -rese 66
numerous 10i ii-164:11ilvisfigat6d the meteorological
conditions Of the ground layer of the atmosphere (see, A. S. Monin, A. m. obukhov
S Monin, Izv. AN SSSR,
GeGfI,z In-ta AN SMR, _ no.-24(151), -1964; A. B. Kazanskiy A. Tr.

--7-7-77-
-77-
t
4- j di 10 --ana,pi of
--proc bsds.., es_-i-quan, if- by Ii 6 wt 3 selected parame ers.i
t
properly,
ende 6Z the'mean square wind- gust -
the:physicall6p n6y,
_Ui ubon'physlciia: 06 :W* adil d ~di
-quantiti hich.may:be'rL
y,~dValuate A scussion of the
*LS .:giveh'a-hd U,',f2- i"s.written-fas a.hinotion, of six dimensioned
paraw, ers.j
_72
to
Sp
P
-is--the-vertidal -di ah-o-,wavwparameter
2
h
sea lev6I_and h15-the niean-
_-hehei hlo
Z. b
e 1g:Lon:,a 61- The.var'db e:z-,is t
M - -the Moiifitgin
c a paramete c ~is- e
OM' th, ind-A/16 th
fr e bri Ii radiation
Z_
_4 X~
theit i i~ t, The functioifal equation is transp-
--and.. Aal, nommi. orm
Par ~9-r-
-thermal c
briked-Abi;c h_t6~isid6rat oils of t ct" iti onveotion*
ondistin atifl:66ti6n-and
t atd:-from h64 hak- 1962 :of-- GGO 'NIIGVF NGUO and TsAO in
ue. d
g
xori~alation ahalysis. The. Authors only -that the
r ea,-.
atioil~AO: not-w 0" r the"valid. ty
1 'table
an
fij ati6ris i
2 ;uresj~ 5_,-! equ

"ACC:.NR
5024882-
'TH F
8m CODE i~ SUBM -DATE-t.. - oc/ ORIG REP 0051 G Vi
'001

ZILIT114MMO BVO*Lj!~MMA~& ~#~.
Ca3p2stlM tbo Watom of equoitim of turmUmt motAm for
tbiD surfaae bwndary Wwo TruV M nooUM4448 165a
(MIRA 1981)

LAYKHDIAN, D.L.; NADEZHINA, Ye.D.; SIMONOV, V.V.
Effect of a change in external conditions on the tr. Efc,=Iata,~~n
of low clouds. Trudy GGO no.167.-67-72 165. (mT.RA l U) -., 3 )

LAYMiTYJII,, D.L.; SHNAYDMAN, V.L.
1-11-11-1 -,.- -'.
Wind and turbulent excbange near frontal surfaces.
Trudy GGO no.167:205-210 165.
(MIRA 19:1)

EWT(l)/FPC GW/iqS-2
ACC NRv AP6021510 SOURCE CODE: UR/2531/66/000/187/0115/0121
AUTHOR: Laykhtman, D. L.
ORG: none
_jcal conditions in lower atmospheric
~TITLE: Usinp. radiation to_Sh~~2~jog
layers oF
SOURCE: Leningrad.-Glayngya geofizichaskaya nhaPrXatnrjyA,_Trudy, no. 187, 1966.
Fizika pogranichnogo sloya atmoafery (Physics of the atmospheric boundary layer),
1i5-121
TOPIC TAGS: radiative energy, terrestrial atmosphere, radiption balance, albedo,
cloud dissipation, effective radiation
ABSTRACT: Solar radiative energy reflected from the terrestrial atmosphere and
clouds is very great, amounting to 70-106 million kw.' This energy can be used to
change climatic conlitions on the Earth. It must be clarified which gain or loss in
the radiation balance is utilized in artificial chznges of the radiation process.
Radiation balance may be changed by: 1) changing the albedo of the active surface,
2) smoke clouds in upper and lower layers of the atmosphere, and 3) artificial dis-
sipation of clouds. The increased radiation balance may be computed for each region,
taking its climatological conditions into consideration.' At middle latitudes the
maximum balance can be reached if clouds are totally dissipated in the daytime and
2

L -3201-6u_
ACC NRi AP6021510
shortwave radiation Is increased, and the whole sky is covered with clouds at night,
If decreasing the effective radiation. An inverse effect is reached when the whole sky
is covered with clouds in the daytime and it is clear at night. Formulas were
developed and used for computation of the radiation balance at various latitudes
Computational results are represented graphically in the original article. Tile area
in which the artificial balance change occurs must bE at least 100 km wide. Formulas
-prove that the increase in heat flux and evaporation is proportional to the increase
in the radiation balance. This indicates that an additional flux of radiative
energy to the active surface is distributed between turbulence and evaporation.
COMPULations show that change of the rad4.ation balance can markedly affect evapora-
tidn,.which is very important in arid regions and during dry winds. The dibsipation
of radiative fogs, which are formed after sunset on clear nights, can be accomplished
by changing the radiation balance. Orig. art. has: I figure, 1 table and 17 for-
mulas. '[EG1
SUB CODE: 04/ SUBM DATE: none/ ATD PRESS:15~

AP7004566
AUTHOR s Laykhtrians D. Le (Professor); Kopanovo L, D. (candidate of (pographical
scionco
ORG: Main Geophysical Observatory GlavrAya goofizichoskigra obeervatoriya)
\Y
TITIZ: Basis for a snow surveying mothod
SOURCE: 119teorologiya i g1drologiya, no* 8, 1W. 22-15
TOPIC TAGS: snow, hydromDtoorology
ABSTRACT: In *recent years the Main Geophysical Observatory' has -,bean
developing the pAnciples of a method for carrying out ne4,work snow
surveys. The results of this work are describedp it being shown that
the depth of the snow cover is a random function of coordinates and
time*
Formulas hawe been derived for computing the' parameters of snow
ring the necessary accuracy in measurement of the charac-
:surveys,* ensu
taristics of the snow cover (5-10%)o It hareboen found that in the USSR
A(excluding mountainous regions) In nrder to achiove this percentage of
Accuracy in determining depth and density it is necessary to have the
'snow-measuring profile parameters given in Table 2 (tor open areas).
'Th!~J~ulated.l data- were obtained from.. 17 *bAnistratione of the lfyd~ t
UDG: 5-%.Y78.467(018
LCard 112
7

ACC NR: AP7006056 SOURCE CODE8 UR/0362/66/002/010/1017/IG25
AUTHOR: LaYkh~~2~D Laikhtman* D. L.
ORG., Leningra Hydrometeorological Institute (Leningradskly gidrometeorologiMeakiy
institut)
TITLE: Dynamics of the boundary layers of the atmosphere and seavith
allowance for interaction and nonlinear effects
SOURCE: AN SSSR, Izvestiya. Fizika atmosfory I okeana,, v. 2, no. 10,
1966, 1017-1025
TOPIC TAGSt surface boundary layer, turbul-int flow, friction coefficient
SUB CODE: 04,20
ABSTRACT: On the basis of a closed system of equations for a stratified
turbulent flow proposed by S. S. Zilitinkovich and D. L. Laykhtr-ian the
author now has considered the dynw-nics of a system consisting of the
boundary "Layer of the atmosphere and the boundary layer of the sea. For tho-
roughness of the discontinuity he uses the analytically derived formula
7-0-v.,%; roughness thus is considered as an internal characteristic flow.
Its -alue is fvund in the process of solution of the problem as A function
of external parameters. The article includes a table of the -numerical values
of the friction coefficient, the wind coefficient, wind velocity at A height
of 10 m and roughuess for different values of the geostrophic w1n4. Mie
computed values agrae satisfactorily with ex
C. perimental data. Orig. arto has$
4 figures, 21/, formulas and I table* JPIGI 3991807.
Card 1/1 met 551.465.7:551.554

-77,-
1410516
pi AP7003077 SOURCE.:
tP
Laykhtmans D. L~; AlIte -zalik, TU. Zho
leningrad teorologica Institute (Leningradekiy gidromiteorologiche
..institut)
alkbkaft tufWlence bi the 'free''
TITIZ: Use 6f aerologIcal datafor detemini
atmosphere
SOURC E AN'SWRi:Izvestiyas~',Fizika"atmc)sfery i oheana, ve ~20-.~n6; .%J9 ,6p, 61
:70PIC TAGS.i': atmospheri ary
c tuAul6riee..~ surface bound layer'
,ABSTRACT: Turbulence intensity at different heights in the free atmos h reN
Me-re
Is an, iropDrtznt characteristic of n1ght "Con, ditiono-o" "At' 'Vo-U-9-6,
Itempts
have not
-the Richardpon number as a criterion of turbulonca intensity
4had gooA resultwee Numerous computations have revealed a poor c-
'tion between the Richardson number.and aircraft turbulence, Me- paper
IS based on the ideas,used in developing a'system of equations for so-;,.;
0
.-lution of tho problea~ of th
wind and temperature diatribution in
vbquhdar~t,~ lay sod I~C~ S..] S*.-- Zilitinkovich and Do L, LaykItman (Tr,-'
IN5)0, 7h9 deri~aiion. of the equations'in this paper Ili
J~aieed`l don'- the tonowing: a), the turbulent flux is " statiorw.
'CO
IWO S "1-551-;55
Caid :lk~~

V; i
--,L iw57-67
ACC NRi AP7DD3077

Jeati~el~ br two'param;ters turbulence sicale
1 and the kin"ic enew .
.
lof. turbulence b- and all other turbulence characteristica are- funo-
tions of these tw parameters; o) the turbulence scale is for a; stratm.'
..ified flow in which-both velocity aind direction change from layer to....-
ilayer and can be obtained by generalizing the Karman formul- Three
'fo.-=Ias are derived ter the turbulence characterist and b0
ice KO
,:7,ie foraAaas, then were investigated to determine their validit,,)r in
It is demonstrated
Umating the intensity of aircraft turbulence.
that there ie virtuaDy Yin correlation between the Richardson nl=bb-.
%
,
At-the same time
9 the value of the kinetio
fend aircraft turbulence,
-
.
t
:;enerLw of turbulence b jemputed:using.the same rmologLeal datap..'.'
t
%Ith, a1mraft
correlates veU
Uwbalence and W be, used for
.
.
'basis 6f 'as
urbulence-on.the- rolb~gjcFa -data;~7"The'-aV-t'
nateriaL"t-
-~'9 16
, OrIg.: art'* has 12',. fIg*es:jud;
providing th6- necepsary
1
.
'
LJFRS,
: '37 7101
.
'
:
SUDI
DATE t:
L%M
ODIM 04 MMFaws

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