SCIENTIFIC ABSTRACT MALKEVICH, M.S. - MALKEVICH, S.G.

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• Collection: Scientific Abstracts
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• Sequence Number: 16
• Publication Date: December 31, 1967
• Content Type: SCIENTIFIC ABSTRACT


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60-37 -4/(
AUTHOR: Malkevich, M. S.
TITLE: Atmospheric Cooling due to Radiative Heat Transfer
(Vykholazhivanlye atmosfery pod vliyaniyem luchistogo
teploobmena)
PERIODICAL: Trudy Geofizicheskogo instituta Akademii nauk SSSR,
1956, Nr 37(164), pp. 89-101 (USSR)
ABSTRACT: The author discusses the effect of radiative heat trans-
fer on temperature changes In the atmosphere, with time,
at different altitudes$ The selectivity in the absorp-
tion of long-wave radiation by vapor is taken Into ac-
count. The presence of cooled and heated layers in the
atmosphere Is shown to be due to long-wave radiation.
Other small-temperature fluctuations are connected with
the re-radiation of lon wave radiation. There are 2
tables, 6 figures, and 9-references, all of them USSR.'
AVAILABLE: Library of Congress
Card 1/1

K E U)
60-37-5/7
AUTHOR: Malkevich, M. S.
TITLE: _-Ta-r-i-ations in Air Temperature with Time due to Turbulent
-Mixing and Radiative Heat Transfer (Izmeneniya tempera-
_t.ury vozdukha so vremenem pod vliyaniyem turbulentnogo
peremeshivaniya i luchistogo teploobmena)
PERIODICAL: Trudy Geofizicheskogo instituta Akademii nauk SSSR,
1956, Nr 37 (164), pp. 102-119 (VSSR)
ABSTRACT: The author investigates a given distribution of air
temperatures, taking into account heat transfer in soil
and turbulent and radiative heat exchanges. A two-layer
problem is considered: the variable coefficient of tem-
perature conductivity (a linear function of height) and
the constants of air and vapor densities are taken for
the near-surface layer of air; in the free troposfere
the temperature-conductivity coefficient is constant,
and the densities vary exponentially with height. It Is
shown that in the boundary layer (2-3 km thick) tem-
perature variations are basically determined by the
Card 1/2 thermal effect of the subjacent surface and turbulent

6o-37-5/7
I Variations in Air Temperature with Time (Cont.)
mixing. Outside the boundary layer, temperature changes occur
mainly as a result of radiative heat transfer. There are 2
figures, 1 table, and 8 references, all USSF-i
AVAILABLE: Library of Congress
Card 2/2

60-37-6P
AUTHOR: Malkevich, M. S.
TITLE: Theoretical Computation of Solar Radiation Absorbed by
the Atmosphere During Various Time Intervals (Teoretich-
eskiy raschet solnechnoy radiatsli, pogloshchayemoy
atmosferoy za raznyye promezhutki vremeni)
PERIODICAL: Trudy Geofizicheskogo instituta Akademii nauk SSSR,
1956, Nr 37(164), pp. 120-131 (USSR)
ABSTRACT: Formulas are developed for computing solar radiation
absorbed by the atmosphere at various altitudes and any
given periods of time. After working out averages for
daily or other periods, it is shown that with elevation
the distribution of absorbed radiation hardly ever de-
viates from the exponential law. There are 5 tables,
and 3 references, all USSR.
AVAILABLE: Library of Congress
Card 1/1

M A L K L V I C ki,
XT) PHASE I BOOK EXPLOITATION sov/1685
Akademiya nadk SSSR. Kmitet po geodeziVi geofizik.e.
Teziiy doklAdov na XI GeuerallnoIy assambleje Me7lidim Lrodnogo, geodezicheskogo
I geotizicheskop soy=a* Hiezhdmai~o6aya assotsiatsiya meterologii
(Abitricts"'of R6pqrts at- the uth G~nerel* Meembli or the International
Uni& 'of Geodesy dad Geoybysics. The International Association of Meteorology)
Moscov,'1957.- -38 p. /Parallel texts in Russian a'adEnglish or French,
1,500 copies printed. No additional contributors mentioned.
PURPOSE: This booklet Is intended for meteorologists.
COVMVM: These reports cover varials subjects In the field cf meteorology. Among
thespecific st*divisions discussed are: the heat balance of the E~.rthls surface,
jet*st"ma, irwafer4nee of heat radiation, electric coagulatton of clqud partl-
cles, tilrbule t. diffusion . 61oud studies,'and others. Abstracts of all the arti-
C14s are tr6aslatedInto either French or English.ThOre are UO references given.
TABrZ OF COFTERM:
Budyko,,M.I. The Heat Balance of the Earth's Stxrface 5
Card V*3, ?-

AUTHOR: Malkevich, M. S. 49-5-8/18
TITLE: The scattering of light in the atmosphere, taking into
account non-uniformities in the underlying surface.
(0b uchete neodnorodnostey podstilayushchey poverkhnosti
v zadachakh resseyaniya sveta v atmosfere).
PERIODICAL: "Izvestiya Akademii Nauk, Seriya Geofizicheskayall
(Bulletin of the Ac.Sc., Geophysics Series), 1957, No-5,
pp. 628-643 (U.S.S.R.)
ABSTRACT: Most of the work which has been done up to now on the
propagation of radiation in a turbid medium is based on the
assumption that the medium is uniform in the horizontal
direction. Although this assumption simplifies considerably
the problem of propagation of radiation it is, nevertheless,
an idealisation for media such as, for example, the Earth Is
atmosphere. The presence of clouds in the atmosphere, the
variation in turbidity in the horizontal direction and also
the non-uniformity in the underlying surface, all make it
necessary to reject the above assumption in theoretical
studies of the radiational regime in the terrestrial
Cardl/3 atmosphere. The absence of experimental data on the intensity
of the radiation and considerable mathematical difficulties
contributed to the fact that,up to now, there has been no

49-5-8/1B
The scattering of light in the atmosphere, taking into
account non-uniformities in the underlying surface. (Coat.)
work done in this direction. Ambartsuayan, V. A. (1),
Chandrasekar, S. (2) and Kuznetsov, Ye. S. (3) have studied
special cases only. Approximate methods of solution of
equations of transport of radiation., the intensity of which
depends on the horizontal coordinates, were treated by
Jefferies (4 and 5). In the present work an attempt is
made to calculate the intensity of scattered radiation as a
function of one of the horizontal coordinates. The latter
expresses the variation in the albedo of the underlying
surface. The atmosphere is assumed to be uniform horizont-
ally and to scatter light equally in all directions. Its
upper layer is assumed to be irradiated by a parallel beam
of solar radiation and the underlying surface is assumed to
scatter light according to Lambert's law. It is shown that
the solution can be expressed in terms of functions of the
form: 00
exp, (- x~S_2_+02) Jo(mys) a ds n+1
Caxd 2/3 (82 + 02 2
(x > 0; n,m = 0,1,2 ... )

49-5-8/18
The scattering of light in the atmosphere, taking into
account non-uniformities in the underlying surface. (Cont.)
(these are generalisations, of Gold's functions). They occur
in solutions of a set of independent integral equations. It
is demonstrated that the problem of taking into account non-
uniformities of the underlying surface does not present any
fundamental difficulties compared with the problem of the
uniform surface and appears to be a simple generalisation
of the one-dimensional problem as developed by Kuznetsov (9)
for an isotropically scattering atmosphere.
There are 9 references, 6 of which are Slavic.
SUBMITTED: December 19, 1956.
ASS6CIATION: Ac.Sc. U.S.S.R. Institute of Physics of the Atmosphere.
(Akademiya Nauk SSSR Institut Fiziki Atmosfery).
AVAILABLE: Library of CongrtsS
Card 3/3

PHASE I BOOK EXPLOITATION SOV/2545
Feygellson Ye. M., M. S. Malkevich, S. Ya. Kogan, T. D. Koron-
atova, K. S. G14-zo-v-a-,-a-n-d-X.--W.-Xuznetsova
Raidiet Yarkosti sveta v atmoafera pri anizotropnom rasseyanii,
eh. 1 (Computation of Light Intensity In the Atmosphere in
a Case of Anisotropic Scattering, Pt. 1) Moscow, Izd-vo
AN SSSR, 1958. 101 p. (Series: Alkademiya nauk SSSR. Insti-
tut fiziki atmosfery. Trudy, nr 1) Errata slip inserted.
2,000 copies printed.
Ed.: 0. V. Rozenberg, Doctor of Physical and Mathematical
Sciences; Ed. 6f Publishing House: V. I. Rydnik.
PURPOSE: This book is Intended for physicists and scientists
engaged in the study of atmospheric ojbtics.
COVERAGE: This wcWk contains the results of computation on the
intensity of light scattered anisotropically in the atmosphere
under various physical parameters and functions of scattering.
The solution of integro-differential equations of the theory
of radiative transfer in an anisotropically se'attering medium
Card 1114,
3

Computation (Cont.)
SOV/2545
was obtained by the method of successive approximations.
The work was carried out by the staff members of the Labor-
atory of Atmospheric Optics within the Institute of Physics
of the Atmosphere, Academy of Sciences, U3SR. No personalities
are mentioned.' There are 23 references; 14 Soviet, 4 English,
4 German, and 1 French.
TABLE OF CONTENTS:
Introduction
Ch. I. Mathematical Solution of the Problem
1. Statement of the problem. Derivation of basic rela-
tionships
2. The zero -approximation
3. Selection of the first approximation
4. Computation of subsequent approximations
5. Accounting for the albedo of the underlying surface
Ch. II. Processing Observation Data
Card 21k
3
3
5
5
8
11
13
15
19

Computation (Co nt.) S011/2545
1. Review of Observation materials 1-9
2. Utili!zation of experimental data 22
3. Processing scattering functions 24
4. Change from optical thickness to the geometrical height 25
Ch. III. Computation Results and Certain Conclusions 27
1. Convergence of the series and of successive approxima-
tions 27
2. Relation between the intensity of scattered radiation
and the solar altitude, transpareny of the atmosphere
and the form of the scattering function 29
3. Light reflection from the Earth's surface 42
4. The flux scattered radiation 43
5. Comparison with a case of isotropic scattering 48
6. Significance of multiple scattering 50
7. Explanation of the tables 52
Table ,1 56
Table 11 97
Table 111 98
C ard 31W

AiJTHOR: MLal~kevi~ch~. S017/49-58-8-6/17
TITLE: The Influence of Horizontal Changes in Albedo of an
Underlying Surface on Light Scattering in a Homogeneous
Atmosphere (Vliyaniye gorizontallnykh izmeneniy al'bedo
podstilayushchey poverkhnosti na rassey.aniye sveta v
odnorod.noy atmosfere)
PERIODICAL: Izvesti-ya Akademii vauk SSSR1 Seriya Geofizicheskaya,
1958, Nr 8, pp ~95 - 1005 (USSR)
ABSTRACT: Expressions obtained in Ref 1 for intensity and flow of
radiation in a turbid medium can be used in a simplified
form when the atmosphere overlying the inhomogeneous surface
has the same optical properties at all heights. It is
assumecl (1) that there is a spherical scattering index;
2) parallel rays of solar radiation are incident on thE
upper boundary of the atmosphere; 3) the underlying
surface scatters according to Lambert's Law. Also, the
albedo of the surface is given by;
q(S) = q0 + q, sin ; (1)
(where is a dimensionless, horizontal co-ordinate
Card

SOV/49-58-8-6/1?
The Influence of Horizontal Changes in Albedo of an Underlying
Surface on Light Scattering in a Homogeneous Atmosphere
0 -
and qo, q, are certain numbers (qo + q,
qo - q, >,O)] . From Ref 1, it can be shown that the
source function, K(It 'S ) , an~ljlso the tensity of the
inward and outward radiation, I and 1 , have
the forms (2), (3) and (4) . ( Where le is the optical
thickness of a column of air at the given height,
and ~ are the zenith and azimuth angles of the
ection of propagation of the radiation; b = cFL
L
is a dimensionless parameter characterising the scale
of the horizontal inhomogeneities on the underlying surface
L -* for a fixed atmospheric scattering coefficient, a -
It is the total o tical thickness of the atmosphere.)
The functions ~p OA 3 R n(r) are defined by the integrai
equations (5), (6) and (7) (where ~ is the zenith
distance of the sun and the constants X n and Y n are
determined by the Bqs.(8) ). Thus, the basic task is the
solution of the integral Eqs.(5) and (6). Almost
Card2/9-
F

SOV/49-58-8-6/17
The Influence of Horizontal Changes in Albedo of an Underlying
Surface on Light Scattering in a Homogeneous Atmosphere
completely accurate solutions for n = 0 have been
obtained by Ye.S. Kuznetsov and B.V. Ovchinskiy (Ref 2)
and these are used throughout this paper. 1. qkn)
To solve Eq.(6) for n 1, 2 ..., the functioz k
were tabulated for b 0.1; 1; 10 (i.e. L = 1; 10;
100 km). The equations were solved according to the
method given in Ref 3 with an error 1-2% for '&V = 0.3
and 5% for 't-4 = 0.~6. As an example, Table 1 gives the
solutions of (6) for 't:*= 0.3; 6 = 0.12 10 and n = 1.2.
The constants Yol X n' Yn (n = 1.2) are determined from
the system of equations (8) with q 0 0.5; q, = 0.3
(the albedo changes from 0.2 for Tt-/2 to 0.8 for
0
=-nj/2). In future calculations, only the first three
(4) need be taken.
r
rms of the series (2)
The source function K(-e obtained from Eq.(2) for
3 = -1T/2-, 0; --j-e12 (corresponding to albedos,
q, = 0.21 0.5, 0-8) is compared with the analogous function
Card3/9-0'

SOV/49-58-8-6/17
The Influence of Horizontal Changes in Albedo of an Underlying
Surface on Light Scattering in a Homogeneous Atmosphere
C;
~O q(1~) taken from Ref 2 (calculations refer to 60 0).
Tables 2-4 show (the difference between K(t and
(Pq (-r) in percents which indicates that K(-,r, I (Pq(_0
for small values of albedo and K(C, t ) < (P q(e) for large
albedos. If the function (p q(Z) always increases and has
a maximum at the upper boundary of the atmosphere, then
K(le , 0 follows an analogous course only over large-scale
inhomogeneities, or over areas with small or average albedo
with small-scale inhomogeneities.
Over areas in which the average albedo is exceeded,
K(-e It ) dies away with height, reaching a minimum in the
middle of the scattering layer and then changing in a similar
f a&on to ~p q(--) -
As Ir, increases, K(-t,E for different t approximates
to K(-.- 1 0) or to ~o 0.5 (Z) i.e. the variation of the
underlying surface is smoothed out as the height increases.
Card4/'Q g,

SOV/49-58-8-6/17
The Influence of Horizontal Changes in Albedo of an Underlying
Surface on Light Scattering in a Homogeneous Atmosphere
Inhomogeneities are smoothed out less in the case of large-
scale variations than small ones - as can be seen from
Table 5, which shows the difference between K(-t , 5) and
K('b, 0) for ~ = I 1V/2 . Comparison of Tables 2 a7nd 3
shows that the difference between K(-d,t ) and ~pq(y)
diminished with increase of the scale.
ifigure 1 shows the horizontal variation of intensity of
the outgoing radiationet leyels Y., 01 0.161 0.30
0.1, 0.3 0 = 60 900) as calculated from
Eqs.(3) amd (4). 4he intensity variations at the given
levels can be in the opposite direction to that in surface
layer, and are gradually smoothed out with height. The
reason for the changes is obvious - in a fixed direction
of observation, the incident light can be reflected from
various regions of the surface. This is clearly shown in
Figure 2, where the continuous line represti~s the vertical
distribution of the rSdiation intensity I at the
point -1-r,/2(R = 60 900) and the dotted line gives
Card5/9-1~~

SOV/49-58-8-6/1?
The Influence of Horizontal Changes in Albedo of an Underlging
Surface on Light Scattering in a Homogeneous Atmosphere
the results obtained from Ref 2 for a vertical change,
I
IT') ' with a homogeneous surface of albedo 0.2 The
continuous curve in iigure 3, represents the vertical
variation in I(') at the point , in the direction
of the point I = - -11012 and the &ottoed line represents
I-(') for a homogeneous surface of albedo 0.2 It can
be seen that, for a comparatively transparent atmosphere,
the observed effect can react2j%o.
The brightness of the sky, 1 (9; e~,o 0 for the
given albedo variation law (0 = 60 1 90 ) deviates
slightly from that calculated for a homogeneous underlying
surface of average albedo q = 0.5 (Figure 4 - continuous
and dotted lines, respectively). The deviation attains
3-59/6 in places; hence, the variation in albedo can be
ignored to this order of accuracy.
The inward and out-ward flow of scattered radiation can
be calculated with the help of Eqs.(9) and (10). Table 6
indicates that the out~u-nrd flow of radiation increases
Card6/ over areas of the surface with small albedo and decreases

SOV/49-58-8-6/17
The Influence of Horizontal Changes in A-lbedo of an Underlying
Surface on Light Scattering in a Homogeneous Atmosphere
over areas with large albedo, reaching a minimum in the
middle of the layer and then increasing again. The
deviation of the flow F(l) from its average value
decreases with height (Figure 5). Figure 7 shows that the
inward flow of radiation F (2 always decreases with
height.
(1) (2)
Comparing F (-t , F with F (t)
(2)(,r) ( q
Fq calculated for a homogeneous surface from
Ref 2), it is found that, for areas with q(~) >, 0.5
F(l) F
(i = 1 2) , whereas the reverse holds true
for q( ) < 0.5 (Figures 6 and Figures 8 and 9 show
similar graphs f or an Etmo sphere with -0 = 0. 6 .
The change in total albedo with height cann now be
calculated from Eq.(11).
Table 7 and Figures 10 and 11 illustrate the variation
of albedo with height and along a horizontal for
cf = q 3, 0. 6 and 6 = 0. 1 .

SOV/49-58-8-6/1?
The Influence of Horizontal Changes in Albedo of an Underlying
Surface on Light Scattering in a Homogeneous Atmosphere
The magnitudes of the total albedo (Eq.(12)) are consid-
erably smaller than the corresponding values of q(T,
(reaching 50016 of 'q- Over areas with an albedo
exceeding the average (q = 0.5), the total albedo dies
away like F(l) (-t I ), whilst q(V, increases. For
Jo~ 0 (i.e. large akdos), q(,r-, k) if (t) , rvhilst
I = 0 (i.e. average albedo), ey practically coincide.
The results obtained require experimental verification
but show that, for example, in measurements of albedo,
from aeroplanes, the inhomogeneities of the underlying
surface must be taken into account.
The idealised model used in these calculations (i.e. homo-
geneous; isotropic scattering) can be applied to the
boundary layers of the real atmosphere for several km.
As is shown in Ref 8, isotropic scattering can be assumed
since the outward radiation depends only slightly on the
extension of the scattering index.
There are 11 figures and ? tables and 8 references, ? of
which are Soviet and 1 English.
Carr, d8/19-9-
Lilt_

WGUISON, Ye.H.; KALMNICK, M.S.
Calculation of light intensity and haziness coefficients In
antootropic scattering.. Trudy lab.aaromet. 7:37-44 '59.
(MIRA 13:1)
1. Institut fisiki atmomfory AN 555H,
(Photography, Aerial) (Atmospheric transparency)

s/o4g/60/000/02/012/022
E032/E414
AUT'11ORi Malkevich. M.S.
TITLE.- An Approximate Method for Taking into Account IforizontaJ
Changes in the Albedo of the Underlying Surface in
Calculations of the Scattering of Light in the Atmosphere
PERIODICAL;Izvestiya Akademii nauk SSSR, Seriya geofizicheskaya,
ig6o, Nr 2, pp 288-298 (USSR)
ABSTRACT: The present author (Ref 1) has shown that horizontal
changes in the albedo of the underlying surface have
only a slight effect on the corresponding changes in the
intensity and the flux of downward scattered radiation.
In practical calculations, it may be assumed as a first
approximation that these quantities remain constant
along the horizontal axes of coordinates. In this way,
one obtains a one-dimensional theory of scattering for
a certain average value of the albedo (either overall
average or local average). This approach excludes the
non-linearity in the boundary condition on the underlying
surface and enables a simplification to be made of the
method suggested by the present author in Ref 2 for
Card taking into account horizontal changes in the

s/o4g/60/000/02/012/022
E032/E414
An Approximate Method for Taking into Account Horizontal Changes in
the Albedo of the Underlying Surface in Calculations of the Scattering
of Light in the Atmosphere
albedo q(f) is a dimensionless horizontal
coordinate'. In fact one can replace the discrete
Fourier series for Ik)(-r. 1(;o,V~ K(z,j) in the
transport equations (1) and 2 , and the boundary
condition on the underlying surface (3). by the integral
functions (4) and (5), where I(1*)(,r,f, 0+ is the
intensity of upward radiation, 1(2)(T:G) is the intensity
of downward radiation, which is assumed to be independent
of 9 and the azimuth 41 and can be calculated
according to the method given in Ref 3, T is the optical
thickness of an air column of height Z, TX is the
optical thickness of the entire atmosphere, dw is a
surface element on a unit sphere, 0 is the zenith angle
of a ray, g is the zenith distance of the sun and
a =- aL is a dimensional quantity which, for a fixed value
of the scattering coefficient a , characterizes the
scale of irregularities in the underlying surface L.
Application of the transformations (4) and (5) to
Card 2/fil,,- Eq (1) and (2) and the boundary condition (3), leads to

s/o4g/60/000/02/012/022
E032/E414
An Approximate Method for Taking into Account Horizontal Changes in
the Albedo of the Underlying Surface in Calculations of the Scattering
of Light in the Atmosphere
Eq (6) and (7). The function Tqo(T) is borrowed from
Ref 2 for a mean value of the albedo qo- Bearing in
mind Eq (8), and the equation immediately above it, the
integral Eq (7) can be redu;,ed to the set given by
Eq (9) to (11), whose solutions do not depend on the law
of change of the albedo and are, in that sense, universal.
Eq (9) and (10), which are independent of n, can be
solved relatively simply by the method of successive
approximations. The solution of Eq (11) is complicated
by the fact that it is strongly dependent on n.
However, it can also be obtained by the mQthod of
successive approximations. Thus, if I(') and K are
determined with the aid of the two formulae at the
top of p 290, the inverse transformation need only be
carried out for the functions Q(n)(P3(-r, n) .
Consequently, the first approximation for the function K
is in the form given ~y)Eq (12). An analogous expression
C d 3 can be written for I If the function q( can be
Loo-~

s/o4g/60/000/02/012/022
E032/E414
An Approximate Method for Taking into A,ccount Horizontal Changes in
the Albedo of the Underlying Surface in Calculations of the Scattering
of Light in the Atmosphere
represented by an expansion of the form given by
Eq (13), the expression for is given by
Eq (15). It is then sufficient to solve Eq (11) for
integral values of the parameter n. Equally sim le
expressions can be obtained for the intensity I(" and
the vertical and hortlIntal cjmponents of the upward
flux of radiation F Fk For example Fi 1)(T,9)
is given by Eq (16). TFig I shows the function K
calculated from Eq (12) for the following values of the
parameters: V4 = 0-3; % = 600; a = 0.1i qO = 0.5;
pi =-0.3; ql qk =-pk = 0 (k = 2,3,-) and for fixed
values of I( - -"jT/2, 01 Tt/2) (continuous curves 1, 2
and 31 respectively). Deviations from the analogous
results (dotted curves) obtained in Ref 1, which are
practically exact, are of the order of 3%. Eq (15) and
(16) can easily be improved by determining the intensity
of the downward radiation using Eq (12), which is
Card initially taken to be independent of This leads

s/o4g/60/000/02/012/022
E032/E414
An Approximate Method for Taking into Account Horizontal Changes in
the Albedo of the Underlying Surface in Calculations of the Scattering
of Light in the Atmosphere
to an improved value for K. which is given by Eq (18).
This method for taking into account the changes in the
albedo is also used for the special cases defined by
Eq (20) and (21), where e is a small positive
quantity which is eventually made to vanish. This
applies to the scattering of radiation by an atmosphere
above two differently reflecting surfaces whose outer
boundaries are at great distances from the separation
boundary. When the change in the albedo of the
underlying surface can be represented by a step-function
and the scattering indicatrix is spherical, it is
suffJcient to consider changes over a band of 1.5 to
2 km an either side of the separation boundary.
Outside this bandq the scattered radiation is calculated
as for a uniform underlying surface. The method can be
extended to the case when the albedo is a function of
two variables. Acknowledgment is made to G.I.Marchuk.
Card 5/6-S There are 4 figures, I table and 3 Soviet references.

8/0~9/60/000/03/009/019
1032/9614
AUTHORs Malkevich, U.S.
TITL3s on the Effect of lion-Orthotropiam of the Underlying Surface on the
Scattered Light In the Alqqq_ phers
PERIODICALtIavestlys Aladenii nsuk BSSR, Sarlys geoft niches kap, 1960, Mr 3,
pp W-448 (MSR)
ABSTRAM' It is usually assmad that the intensity or radiation reflected from
the uiiderlying surface does not depend on the dpection (Lambert's law)
and reflecting properties are described by thellbAp, i.e. the ratio
of the flux of radiation reflected from the surface to the flux
incident on the surface. However, experiments show (Refs 2-5) that
natural surfacGs do not reflect radiation in accordance with the
Lambert-law. Their reflecting properties are ebAracterized by the
reflectance R(r,r'), ihich in defined as the ratio of the reflected
I-rtewity In a given direction to the Illamination of the surface and,
consequently, In geaeral it depends on the directions of the Incident
(ri) and reflected (r) rays. The reflectance of natural surfaces
Gard 1/3 depends on many factors which are unimown a priori. The present

3/049/60/OW/03/0,09/019
303"614
On the Xffect of Von-Orthotropiam of the Underlying Surface on the Scattered Light
In the Ataosphere
paper is concerned with estimating the function
f (T) - KR(T) -
which characterizes the difference between the scattered radiation
calculated for the direction dependent case and the pure Lambert's
law case. The analysis is based on the theory put forvard by
Kuzn4sov (Ref 6). A general expression is now derived for f(V)
(r,qa 4 to 9) . As an e=pls, the case defined by ScLe (10) and (11)
is considered. It is shown that the absolute magnitude of the
difference between KR and I depends an direction, and for those
directions r for whi-ch the. tu;n_;ities Kja and Kq are thowelves small,
the relative magnitude of the difference may be up to 20%.
Card 2/3 Conditions are foxmulated under vhIch the difference can-be regard~o

8/049/60/000/0-3/009/019
1032/19614
On the Eff act of Mon-Orthotropism of the Underlying Surface on the Scattered Light
in the Almosphere
as small. The nunerical results Obtained are summarized in
Tables 1 and 2. Acimowledpent is made to G.V, Rozenberg for
Important renarim. There are 5 figures, 2 tables and 9 references,
8 of which are Soviet and 1 ?Inglish-
ASSOGUTIOMAWoniya nauk SSSR, institut fiziki ats"fery (Academy of Sciences USSR,
Institute of Physics of the ktmosphere)
SUEWITTHD* FebmAry 14, 1959
Card 3/3

MAIRWICH. M.3.; GIAZOVA, K.S.
Tariability of some parameters used in calculating the flow of
scattered radiation. Izv. AN SSSR. Ser. geofiz. no.8:2246-1251
Ag 160, (MIRA 13:8)
1. Akademiya nauk SSSR, Institut fiziki atmosfery.
(Solar radiation)

87978
s/o49/6o/ooo/olO/Ol3/ol4
E032/E4i4
AUTHOR: Malkevich M S.
TITLE: An Approximate Method for Solving the Equation of
Radiative Transfer in the Atmosphere
PERIODICAL: Izvestiya Akademii nauk SSSR, Seriya geofizicheskaya,
1960, NO-10, PP-1541-1546
TEXT: The equation of transfer for plane-parallel, purely
scattering atmosphere can be written down in the'form
Eq. 1 . Cos 0 (.r. ') + I (T, -') T,i(T; r', r) +
Eq.2. + 1(2) (r, r') y, (T; r', r)] A)' (i = 1,2);
C
](2) (T', 7) = nS6 (r - re); F(1) (0) = qF(') (0), (2)
C
Card I/

87978
S/049/60/000/010/013/014
E032/E414
An Approximate Method far Solving the Equation of Radiative
Transfer in the Atmosphere
where I(l) 1 1(2) are the intensity of upwar4 and downward total
c
(directeand scattered) radiation respectively, v is the optical
thickness of the given layer of the atmosphere, 0 is the zenith
angle, is the azimuth angle, y is the normalized scattering
function (indicatrix), TM is the optical thickness of the entire
atmosphere, ITS is the solar constant, q is the albedo of
the underlying surface, a(r-re) =0 when r=O= ro and
Yb(r - r. )do = I and finally
FW (T) IW (T,r)cos 0 do
c c
where the integration is carried out over a hemisphere of unit
radius. Kuznetsov (Ref.1) has shown that one of the principal
difficulties in.1giving these equations is the complicated
dependence of cX (T,r) on r In the case of anizotropic
Card 2/X 6

87978
S/049/60/000/010/013/oi4
E032/E414
An Approximate Method for Solving the Equation of Radiative
Transfer in the Atmosphere
scattering in the atmosphere, the functions* M(i) r (i) will
c c
depend not only on vX and q but also on the zenith distance of
the sun I , and on the scattering function. The dependence on
can be partly reduced, and the dependence on q entirely
excluded, if the contribution due to direct solar radiation is
removed from Eq.(I) and the scattering of radiation reflected from
the underlying surface is considered separately as was done by
Feygellson et al (Ref.4). On this approach, Eq.(I) can be split
into two independent systems of equations of the same form, one of
which is
COS 0 Ij (T, r) +(T. r~) -r1j (-r; r', r) +
Eq-7- 12 (-r, r', r)) dw'+ -L emp -'r) see 7.j (T; r.0
('c; 4 r) (i = 1, 2) (7)
Card 3/7,L

87978
S/049/60/000/010/013/014
E032/E4i4
An Approximate Method for-Solving the Equation of Radiative
Transfer in the Atmosphere
with the boundary conditions
12(,gXr) = 0 11(0,r) = 0
This equation determines the intensity of scattered radiation for
a perfectly black underlying surface. The second equation is
oT
(7 1)1-' cog 01 (T, r) + (T. r') rIj (r, r', r) +
4a
Eq.8
,i(,r;r',r)jdw' (i=i,2) (8)
with the boundary conditions
II(0,r) == I 1 2(T r) 0
Card 4/q(;

679T8
S/049/60/000/010/013/oi4
E032/E4i4
An Approximate Method for Solving the Equation of Radiative
Transfer in the Atmosphere
and describes the scattering of the reflected radiation. The
intensities and fluxes of the integral radiation are then given'by
(T, r) r) +CT, (-r, r)+.tS(i -1) 6(r-rO)eXPr-(T* -T)SeC 01,
C
PO) rj (T) + CV, (-o + -S (i - 1) "'P I- (T* - T) see C) Cos
C = q aS CXP T'Ser, ~) Cos t + F2(0)
I - qF2 (0)
For each of the systems given by Eq.(7) and (8) one can obtain
equations of the form given by Eq.(3). The functions given by
Card 5/'V(,

87978
5/049/60/000/010/013/014
E032/e4i4
An Approximate Method for Solving the Equation of Radiative
Transfer in the Atmosphere
Eq.(4) and (5) will in the case of Eq.(7) be less strongly
dependent on *S , while in the case of Eq.(8) they will be
independent of both q and % . These functions are determined
by the present author by an approximate procedure. Mi(-r) and
r'i(T) are approximated to by mi(T) and yi(T), which are
obtained when in Eq.(4) and (5) 07.q uses the intensity of singly,
scattered radiation instead of Ic ). The scattering function is
expressed as a series of Legendre polynomials, and mi and yi
can then be expressed by analytical formulae. If it is then
assumed that mi and yi are sufficiently close to the true
values Mi and ri, then one can obtain a reasonable approximate
solution of Eq.(3) by replacing Mi, ri by mi, yi. It is found
that this procedure gives quite a good fit, and the calculated flux
found-on this approximation is not in error by more than 10 to 15%.
There are 3 figures, 4 tables and 7 Soviet references.
5 ~7
C
Card 6/~C

S/169/62/000/003/057/098
D228/D301
AUT.'-.-OR Malkevich, Ill. S.
TITLE: An approximate method of taking into account t*-e ho-
rizontal changes in the albedo of the underlying sur-
face in the problem of light scattering in the atmo-
sphere (Theses)
PERIODICAL: Referativnyy zhurnal, Geofizika, no. 3, 1962, 27-28,
abstract 3B224 (V sb. Aktinometriya i atmosfern. optika,
L., Gidrometeoizdat, 1961, 260-261)
TEXT: A method is proposed for approximately solving the problem
of light scattering in the atmosphere, with allowance for the arbi-
trary changes of the albedo of the underlying surface alona one of
the horizontal coordinates. Two examples are considered. / Abstrac-
tor's note: Complete translation.-7
Card 1/1

Q-/!69/r2/000/003/058/098
D228/D301
AUTHOR: Dlalkevich, M. S.
TITLE: The influence of the anisotropy of light reflection by
the underlying surface on light scattered in the at-
mosphere (Theses)
PERIODICAL: Referativnyy zhurnal, Geofizika, no. 3, lj62, 28~,_a Ib-
;1 "-ka
stract 3B225 (V sb. Aktinome'riya i atmosfern. o L
L., Gidrometeoizdat, 1961, 261-262)
T--:7'XT: The particular problem of radiation transfer in the alumo-
sphere is solved. The differences between the quantities, characte-
r~.zing sky radiation when the surface is orthotropic and does not
reflect according to Lambert's law, are determined. It is estab-
lished that the albedo depends on the brightness coefficient and
the opLical characteristics of the atmouphere, and a meano of ap-
proximately calculating the albedo, if the brightness coefficient
and optical parameters are known, is suggested. /-Abstracter's no-
te: Complete transiation.-7
Card 1/1

ATROSHENKOO V.S.; GLAMA., 4A.;,HALOVEHI H.S.- FEYGELOSON,. Ye.M.;
Prini-14 uchastiyes KIM ~~~~OXASHOVA L. studentIna;
ROZZIBMG., GA.,, prof., doktor fiz.-maten.nauk, otw.red.;
fERKIYAP N.VI, red.izd-va; SWHIEOVA., L*A*, tekhnered.
[Calculation of light intensity in the atmosphere during
anisotropic scattering* Part 2) Haschat iarkosti oveta v
atmoafere pri anizotropnom rasaelanii. gast' 2. Moskva.,
Izd-vo Akid.nauk SSSR, 1962. -222 p. (Akiademiia nauk SM.
Institut fiziki atmosfery. Trudy,, no*3). [MICROFILM] (KEPA 15:8)
I* Moskovskiy gosudarstvenrqy universitet (for Kim, Tomashova).
(Idght-Scattering) (Atmosphere)

3
AUTHOR: Malkevich, M. S.
U831
3/560/62/000/014/OOP,/Oll
A001/A101
TITLE. The angular and spectral distribution of radiation reflected by
the Earth into outer space
SOURCE: Akademiya nauk SSSR. Iskusstvennyye sputniki Zemli. no'. 14, 1962,
30 - 48
TEXT: Intensity of radiation outgoing from the Earth's atmosphere upper
layer into outer space can be directly measured by Earth's artificial satellites
and space rockets. Also the problem of angular distribution of reflected short-
wave radiation can be solved by means of receivers with small angular resolution, VY
mounted on satellites or rockets, scanning the visible portion of the Earth
along various directions. This problem can also be solved in a theoretioal way,
by solving the equation of radiation transfer for various atmosphere models and
reflecting surface. The problem of analyzing the angular and spectral variation
of outgoing short-wave radiation represents the purpose of the article. To
solve the radiation transfer equation, the author uses the plane-parallel model
Card 1/3

S/56O/6P_/OO0/O 14/002/011
The angular and spectral distribution of ... AOO1/A1O1
of atmosphere and assumes that the Earth's surface reflects radiation according
to Lambert's law. Various factors affecting the distribution are considered.
The factors analyzed are the following: the degree of atmospheric turbidity;
characteristics of the underlying surfaces which are divided, according to their
optical properties into 4 categories: 1) orthotropic and "gray" objects, 2) 11Y
orthotropic but not-gray formations, 3) horizontally heterogeneous orthotropic
and "gray" surfaces, and 4) un-orthotropic surfaces whose brightness coefficient
depends on the direction of incidence and reflection of radiation. It is con-
cluded that variations of ~lbedo of reflecting surfaces affect the variations of
angular and spatial distribution of outgoing radiation in a considerably higher
degree than variations of the atmospheric optical properties. The distribution
of cloudy formations, upon which depends mainly anisotropy of outgoing radiation,
can be determined on the basis of statistical processing of radiation measure-
ments. On the basis of solution of transfer equation, one can determine the
spectral composition of outgoing radiation for various conditions of atmosphere
illumination and reflection of terrestrial objects. The main difficulty of this
determination consists in that relations of optical thickness and scattering
indicatrix of turbid atmosphere to the wavelength are poorly known. It is pos-
Card 2/3

a/56o/62/ooo/o14/002/011
The angular and spectral distribution of... A001/A101
sible, varying scattering indicatrices, to evaluate their effect on the spectral
variation of outgoing radiation intensity. Reflecti6h of natural surfaces, such
.as water, several types of soil, snow cover, and also clouds depends slightly on
the wavelength in the spectrum region considered. Therefore, the data presented
6n the variation of spebtral composition may have a direct application to inter-
pretation of measurements of radiation characteristics from satellites and rack-
ets. In particular, these results can be used to distinguish snow cover from
clouds in the case of equal neutral reflection of these objects. Another practi-
cAl application is determination of the upper boundary of clouds. This method is
based on the fact that the ratio of intensities of outgoing radiation, correspond-
ing to short and long waves of the spectrum range considered (0.35 - 0.75 mlerms)
will vary with the altitude of the reflecting boundary of the cloud. This alti-
tude can be also determined by measuring outgoing radiation in absorption bands
of those atmospheric gases which are distributed uniformly over the height, e.g.,
carbon dioxide and the band of molecular oxygen centered on 0.76 /.4. In conclu-
sion the author discusses the effects of heterogeneity and non-orthotropism of
the reflecting surfaces and points out that to solve the equation of radiation
transfer, one can at first suppose that incident radiation does not depend on
coordinates x, y and Fourier transformations can be employed. There are 8 fig-
ures and 4 tables.
Sulm S March 7. 1962
Card 3/3

MALUVICH, M.S.; POKRAS, V.M.,- YURK07VA, L,I.
Measurements of the radiation balance from the Explorer-7
satellite. Isk.sput.Zem. no.14:105-132 162. (14UU 15:11)
(Artificial satellites in meteorolcgy)
(Atmosphere)
(Heat-.--Wiation and absorption)

_FNIR I .

MALKEV IGH, M. S.
"Some problems of interpretation of radiation measuremnts from satellites."
report submitted for 15th Intl Astronautical Cong, Warsaw, 7-12 Sep 64.

:ACOWSION MRs AP4030341 a/0049/6W000/0Q3/039V"7
AUTHORS I Malkrdoha MI ... P. I ROOM# A@ So I FAvanberap GeV,
,'TIT19i The three dimensional structure of a radiation field as a cource of
-!meteorological information
SOME$ AN SSSR- Isy- Ser- goofis., no. 3, 1964, 394-4o7
:TOPIG TAWI artificial satellites, weather forecasting, radiation field., tropor
';spheres stratosphere
AB MIGT: The authors have pointed out the importance of world-wide ~bssrvations
in order to make satisfactory weather predictions, and they have found the use af
:artificial satellites for collecting meteorological data to offer both economy
band geographic distribution of observational points. But, though the amount and
universality of the information is increased, the type of information in qualita-
tively altered. The single source of informatioa (for the lower layers of the
;atmosphere-the troposphere a~d stratosphere) Is electrical radiation of various
,wavelengths refloated or emitted by the earth's Mwfaca and the surrounding atmo-
Mheree Easentially the problem become a matter of spectral analysis of radiation
i/12

!ACCFMION URt Ap4wAl
!being lost by the planqt. The authors describe the connection between structure of
,a radiation field and meteorological and other processes that have some effect on
the radiation fields They describe the inhomogeneities of various scales in the
!radiation field and outline the physical origin of these inhomogeneities as well as
:the contribution they make in the recorded streams of radiation. They propose a
.method for comput4ng atmospheric distortion when recording the structure of the
.underlying surface, and they also furnish definite recommendations for a method of
;observing the radiation fieid~ from artificial satellites. This involves principally
I
,a hemispherical receiver turned toward the earth and a device with the proper solid
;angle of view, Orig. art, has, 5 figures and 18 formulas.
;LSMIATION: Akadeddya nauk SM Institut fiziki atmeaferyo (Acadeaq of Sciences
~SWR, Institute of Physics of the Atmosphere)
I -
ISUMUTTEDs 2OJUn63
DATE AGQs 29ApA
ENCL a 00
IMB CCDZI F's
Card2,/2
NO REF SOVS 009
OTIiRl Ooo

MAIZEVICH
Some aspects of the interpretation of the Olel.j of radiation
leaving the earth Part 1* Determining the temperattire of the
0 W,
underlying -surface'. and the' upper ~-Ioud limit GGn nal.166:
102-116 164, 04"'.
Some aspects of the interpretation of the fie2d of rad-.latAon
leaving the -Lrth-~ Part,2. Distinction of clouds on the back-
ground of mtural'surfaCes i4 lbid-.,:11?-127 164. (MIRA 17:11)

I ~A T
r-bor-ne de!. a;.a s
s r i. t. r Ji y

KOPROVA, L.I.; MALKFVICH, M.S.
Thermal radiation of a spherica! atmosphere. Kosm. isal. 2
no.6:881-900 N-D 164. (;41PA 17- 12)

KONDRATIYEV, K.Ya., dok'or fiz.-matem, nauk, prof.; Xkl- VTCH' M.S.,
u I ~KE. I kand.
fiz.-matem. nauk
The 15th International Congress on Astrona!:tics ("Meteorological
Satellites Systems" section). Meteor. _4 gii-oll. nn.3:38-41 Mr 165.
NIR.A 18-2)

la.d

KOPROVA, L.I.; 14ALKEVICH., M.S.
Empirical orthogonal functions for the optimm parameterization
of the temperature and humidity profiles. Izv. AN SSSR. Fiz. atm.
i okeana 1 no.1:27-32 Ja 165. (MIRA 18:5)
1. Institut fiziki atmosfery AN SSSR.

KONDRATIYEV, K.Ya.; MALKEVICHt M.S.
I - - - .., I ----- - --
The 15tb International Astronautical Congress. Jzv. AN SSSR. Fiz.
atm. i okeana 1 no.1.122-124 Ja 165. (KIRA 19:5)

ev, B-. F*;! Malkevict -14 S Feraponova Gwl__~
lapynciq: Katulin~-V _A,,,,Kozj;r
.Rozenberg
(Professorl
T_"rTUU..'- A-irplane eVI
-d ice. -for -measuringrr -radiation balance and some results of
measuri~,,jients
SOURCD. Mazhvedomstvennoye~ sovesM~hdftive -'~o akti nometri i - i optike. atmosfeiy- 5th
_Z3T 0m CST;
MO S c ow, --19 Aktin, etriya optika -a&tmosfery (Actinometry and'atm, -ospheric opli
Trudy. -soveshchaniya. Moscow, lzd--t6 11-.~~uka, 1964, 55-59.
TO= ITAGS radiation pulsation, radiation thermoelectric element, terrestrial
-ad-' atmospheric -radiation, ~upweil ing radiation,,~downwelling radiation, albedo
Ful5ations of shortwalie and lqr~gwave -radi tion: fluxe s have been measured
a ~M- ail vacuum, hermoelectric -radiometerb-irith a 180* scope. This device
M-11E.sul s-31-ar, chortwav and terre5tria_l and atmo~;pheric ongw~Lle radiation. Regions
.:af -L- nr abqorption by-water vapor were 'ou~',d and ueparat-d. IITI-,e device measured
0
~Ilinz and downwell4 lation fluxeo during airplane rliots above steppe
ing rail
an z4a ~regians withi clear and claudy- skies. A decrease in the dovriwellingflux was
~observ'ed iii the Atmn:;-oheric layer 1-3 1-nalonve both regions, -A -v~7. 4ghtclecrease in_the
Card

L r,2

iM -AQCESSI0_Tr_NR:.' -AT50111'6-
_
_
do
Vnwell ing~. ~flux. was
-obsez-ved. above the clouds in the 3--_ 5-km atmospheric--layer. Al-
--decrease in' -
the-upwellIng flu;k -was also observed _ia_thiS__ Iayer._~=gjasa- --ot--c

Lt
P

EG)

t5socr lo
IAT
Institut- fiziki atmos All, SSSR
Moscow

Institute of the Physitu'of'
-the Atmospbere, AN nsp)

BMITTE-D.-
251'Iov64-
ENCL: 00 SUB CODE:

TO RZ
, -F
1

05 OTHER: 000

TD PRL,SS.- $009

Card

AUTHOR: Malkevi 4h,, M. S.; Mal kov. I. P.; Pakhomova, L..' A.; Rozenberg, G. V.;
Faraponova, G. P.
TITLE: Determination of the statistical characteristics of radiation fields over
clouds
SOURCE: Kosmichaskiyo Issledovanlya, v. 2, no. 2, 1964, 257-265
TOPIC TAGS: meteorology, cloud, atmospheric radiation, radiation field
ABSTRACT: A study has been made of the possibility of applying statistical ana-
lysis to flel ds of outgoing radiation for determining the structure of cloud forma-
tions. Computation of the structural parameters of the cloud cover is accompl!sh-
ed using aircraft measurements of radiation with narrow- and wide-angle Instrumenq.
The following conclusions are drawn from this preliminary investigation: 1. Sta-
tistical characteristics of the Intensity of reflected radiation can be used for
an objective analysis of clouds of various types and a reliable identification can
be made on the basis o~ the full set of statistical parameters. 2. The most in-
formative-paramp-ter-is the spectral density,of fluctuations of brightness, which
is quite sensitive to a difference In the character of nonhomogeneities of dif-
_fei:ent oud types and at the same time is statistically stable. 3. An investi-
Ca rJ

ACCESSION NR: AP4034796
gatjon of the statistical characteristics of radiation fluxes, considered as ran-
dom functions, makes it possible to take into account fluctuations of the radiant
flux of.heat under conditions,of arbitrary cloudiness. In this case spectral
density makes it possible to obtain the distribution of radiant energy by fre-
quencies and determine those scales of nonhomogeneities which make the principal
contribution to the flux of radiation heat. 4. The spectrum of fluctuations is
similar to comparable spectra,of fluctuations of wind velocity and temperature ob-,
tained in investigations of turbulence in the surface layer of the air. The spec-
trum was displaced into the region of somewhat lower frequencies, evidence of an
increase in the scales of the eddies responsible for the nonhomogeneity of cloud
'-formations. Orig. art. has: )0 formulas, 6 figures and I table.
ASSOCIATION: none
SUBMITTED: 230ec63 DATE ACQ: 20May64 ENCL: 00
SUB CODE: ES NO REF SOV: 009 OTHER: 003
2/2
Cird

ACCESSION Mi AP4034793 0/0293/64/004NOP/0246/0256
AUZU01ts Halkovich, H. Go
TMS: Certain problems in the interpretation of radiation measurements from
artificial satellites
SOURCE: Kosmicheskiye iseledovaniya, *. 2. no. 2, 1964. 246-256
TOPIC TAGS: artificial satellite, atmospheric radiation, cloud, cloud boundary,
earth satellite
ABSTRACT: This article describes methods for determination of certain physical
parameters of the atmosphere and underlying surface from measurements of radiation
in different parts of the spectrum obtained using artificial satellites. The pro-,
posed methods for solution of the corresponding inverse probleme (determination of
the temperature of the underlying surface and the atmosphere, the masses of mattee
absorbing radiation and the height of the upper cloud boundary) are illustrated
examples. The paper consists of an introduction, description of the method for
determining the terVerature of the underlying aurfaceg the procedures for deter-
mining the vertical temperature profile, the method for determining the mass of
absorbing watter, a discussion of the characteristics of the rodom radiation
~;4jejj,and certain conclusions* The principal conclusion drawn from the stuV Is

ACCESSION NR.: AP4034795
that in the interpretation of radiation measurement data from satellites it to I
necessary, to use certain determined physical dependences between thd characteris-!
ties of the radiation field and atmospheric parameters, using statistical rela-
tionships for this purpose. A problem of the greatest importance is selection of
physically sound methods for taking the absorptivity and emissivity of the atmos-
phere and underlying surface into account; this is particularly important in the
solution of inverse problems. In solution of such problems it also is very im-
portant to find algorithms ensuring the stabifity of solution of the inverse prob-i
lem. With respect to the use of statistical methods the most important problem is
determination of the parameters of radiation fields, thereby making it possible
to use the most economical and an-ary methods in describing the enormous voluxe
of data obtained from satellites. The solution of these problems is dependent an
improvement of experimental methods and increase in the 4ensitivity of measure-
ment instruments. "In conclusion the author thanks G. V. VAtenberi for "Inable
comments during disoussiou of the problem dineusaed In the paper"6 Origo art.,
has: 5 for=lax, 6 figures and I tables
ASSOCIATIONs
SUDHITTEDs MeoO DAM ACQt 2OH464 ENCLi 00
SM COM AA NO MW Govi 014 on=: 009
card W2

L -21?56-65 EWT (1) /~WG (v-) /FdG/FWA (h) Po-!+/Pe -'w5/Pq'4/Pa e -2/1'ta.10/pe b/Pi4
ACCESSION NR: AP5000170 S/0293/64/002/006/0881/0900
AUTHOR:-. ~K
ORTO
-TITLED- The-'therm
aLradiatiorf-of :a -iPhtAcal, at:mosphere~~
SOURCE- -Kosmiches1d &'issledovaniya,~v. 2, no. 6, 1964, 881-900
Y_
4dj_Ajjqn, -ozone,
TOPIC TAGS* atmospheric thermal radiation zjt~ ~o Lvq~c.2~otng__r
mesosphere, water vapor absorption band
ABSTRAM The authors have solved the thermal radiation transport equation for the
ca,~-,e of a spherically symmetrical atmosphere. The -solution is expressed bythe traw-
-sior r
is rt f1mation, averaged for individual spectral interval An app oximation of the
m
transmisaion function'ta proposed which ensures its reliable extrapolation Into Uie region
W,
arg.- masses of absorbing matter. The authors have also derived expressions for
determination of the Intensity flux and indrem, ent of radiation e ng
scapi from the upper
Eo -unvca r-Y -.0 f
for &.eir random Variations. In addition, the authors hw,,e computed the angular.varlation:
of the intensity of th ermal- radiation In different parts of the spectrum escaping from the
upper '~oun4viry of a pherically symmetrical atmosphere, Also considered is the variability_
Card 1 /3

?56.~6
A(~ C LSSIGN XR: AP5000170
-of the field of outgoingradiation, determined by variations In the temperature of the unde ~r,
ly, ng purface* and, -atmosphere, cloud cover and-other factors detarinining outgoing radiation.
Although. It Is noted -that -the r Cal field-.of the earth's radiation is not spherically symznetrIc2l
and that the trandmission function has, not been computed sufficiently-reliably for large-
masses of absorbing-niatter- the results presentedin.the paper- lead -to -the- foll6wing:bas'"Id
conclusions. The flield of -radiation escaping, from the upperboundary of the atmosphere
Jinto.- universal Space,16 most hon-vogeneous and Isotropic in-the parts -of the spectrum.corre-
spondi.,Cr to the central-p-a-r-t-s- oUthe, absorption bands. -In In 6
r t rvals of atmospheric trans-
parency. the radiation field is -less homogeneous and Isotropic and most clearly reflects the
temperature pattern of the underlying surface. The Intensity of outgoing radiation
for broAd spectral intervals decreases with- approach of the direction of sighting to the
harizon Cdarkenlng!l of the limb of the planetary disk); In the central parts of the absorp--
tion bincla,, on the otherhandi-there-is. VIbrightening!.1-1of the-limb. --JAn exception Is-the
iLbs-o- d__ V___t-ozone in which -the'radiation intensity- decroa-3es---- to'Ntr-ard the Umb and has
a noticemble jump on the eartl~__ atmosphere discontinuity. The angular distribution of the
intenstty of otttgoing rWation is not sufficiently sensitive to variations in the vertical dis-
tribution W atmospheric temperature for it to be used for determination of temperature
profiles. The therm,-d nonhomogeneity of- the underlying surface and -cloulds, -which
-CC-rd _W3~

IP7,
L 21?
ACCESSION 14R: AP5000170 Ll

adiati6ri.,-~'Th,e-tadizition-bfth6 Mesbsph6rblt~elf an Apprec e contribution n -M_
M field of tIhe~absorpti-oA Uands of,Iwater _i4p6i nd carbonId1wdde, ff In concl
usion~:the authors
ek-iress ide'ep appreciation. to.-G. V.- koze_6e~~ lor: dWdusSiOn of -Alertai-n of the results of
thi study and.al fd'V.G Ics_ L. V. edvedevi
M and
so, e eyqv L. 14 -:-Markina or preparation
-IT -fit hai.
of the program and malting calculations on the Jral computer, Orig.' art. 3'o
30 formdas,. 8 figures and. 2 tables.
ASSOMATrMh. None
D- 7 SUB CODE; ES
SUBMITTE I Mat'64 -ENCL::.'-06
NO REFI_SOV.-,~,010 -:.OTHER,, 010.

-MALMICH, M.S.
Relation between the ctarac-,eristics cX the vertical atructure of the
long-wave radiation field &r-d the temperatur, and h-midity fields.
Im, AN SSSR. Piz. atn. " okeam 1 no.10OLC39-1049 0 165.
.4TR.A 18~,-y'j
1. Institut fiziki amosferly Q1 SS6R.

-the d
y - prof il6g durihS e-
T_ IT LE T~e-ro_l_e_-of._Ver4,qal_,-tem hti6iidit
perature and

8u
torminatiowof-thelEarth'� rf ace - temperature from outgoing radiation

atm -no. 7, 1965,
SOURCE: A14 SSSR. lavestiya, Fizika osfary L okeana, v. I
703-714

TOPIC T-A G -S weathet-satellite. window- transparency mea!;urement,
atmospheric
temper t pheri6 humidit ' atmo8pheric radiation -absorption
Y2
ABSTRACT-- Satellites of the "Tiros" Series clarried -out measurements of the
-ace -radilltion leaving the Earth throup tic
Farth va u r temperature utilining
p -range. owever.,~_ dwe to
n
aabso' 'ti- - it effects ~tha errors of. such measur--ments -m-av be as high. -as_
rp q 2
-a method for t ;h edetermirwtion of the- trt..--.,,nurface tempera_
oa~sequently,
-lation is proposed. It i r, based
ture frorl satellite meanlure'ments of autgoing race._ 4
,
--
-
-
'
l
-
it,-~_structure 7
Folloving
an
z~tl rtlcal-te _humld
le_ U
te-ve
t
-theory.. the autho~~a -presents some- e~xajh, Les~ such-profilea-and
owt~lina of the
1/2
Card

4105 '65 E",;j 4 1
-ACC&SSION RR t AP501567Z t)'F~/0293/65/r)03/003/044-4/04,c6
I
551,524,7t629,195.2:551.5

zz
pq 244.
RS f -_-YAII_3tIzh 't -so; -TA S

-rile of tho' tinospho bj~m6a~~--

1,17134, ning the-vertical temparature c Cz re
Deterld I
002 absorption bandy issuing -thie -up boundary
uringr 'the radiation) in the from per
Of tb-A dt~nosphere

SOURCE: -Koamic a ovanJy
h skiye iasl6d a,,ve 3;,no*--3~ 1963t 4,4-4-7456
-
7- .
-
~
-
-
`
- t
Nr
ti
t
t
t
b
W
1 --
-
z -
TOPIC --TA
on neasureman
band
uro
adia
sorption
empera
1pp a
mosph
er are, a

AMPACT; -.A;- method is p6ued~ for determinirie-the tmpga Profile of the
pro
l
--T-1 satellit s)- in the-CO2,abs
aLz~osi-e~e ~measuremqnts (by means of artif id 0 orp-.
t:Lon band afradiation issuin ph-are. The
g from thG upper, boundax-y of the atmos
r,!)Uhad 4-5 based on analy-ais of thei desired ter-merature profile b7 umiqg. a statis_-
tical orthogonal system of fanotions of the tonmerature field. For ary desired~
Precision of appromirm-tion.the numbe.- of awlytical members may be reduced to -q
-inimum and maj thun dirAnInh thQ effect of instability wban aolvirg the recip-

-,61 -:-
-obal a bleia. o statistical ~wopoxtios of the vorttepl
Gomputation -of th,
_
Cci,d itY

L 34808-66
F~CC _NR, P
I.AWHOR:
EWT(1)/FCC GWMS-2
Gorchakova, I. A., Malkevich, M. S.
ORG: Institute of Physics of the Atmosphere, AN SSSR (Institut fiziki atmoefery
AN SSSRY-
TITLE: Change in outgoing rad~iation in the 15 V carbon dioxide absorption band
SOURCE: AN SSSR. Izvestiya. Fizika atmosfery i okeana, v. 2, no. 6, 1966,
585-594
TOPIC TAGS: temperature distribution, spectral absorptivity carbon
dioxide, integral equation,' atmospheric temperature, upper
atmosphere radiation, atmospheric pressure, band spectrum
ABSTRACT: Vertical tep4w
xAture-diatxibutipa-i-n-th-e--a-tn2s-ph-tre is computed mathe-
matically on the basis of the pressure and the radiation entering space from the
upper surface of the atmosphere, which is measured in the 15 v spectral band, kncr4a
as the carbon dioxide absorption band. The outgoing radiation is computed using an
integral equation containing Planck's radiation function, and the absorption function
is determined from an exponential integral equation. The heterogeneity of the at-
mosphere is compensated for by the effective mass of carbon dioxide,which is intro-
duced. The absorption function, computed under such conditions, is represented
graphically. This function depends upon the values of the parameters used. A
table in the original article shows temperature values at various pressure levels
computed using various absorption functions. Changes in the spectral distribution ofl
C~_-_4 112 UDC: 551-521.3

L 34808-66
ACC NR: AP6022217
.outgoing radiation depend not only upon temperature variations in the vertical
section, but also upon the changing concentrations of carbon dioxide and water vapor
in the atmosphere. Bands of carbon dioxide absorption overlap water vapor bands.
This superposition was computed in order to correct the temperature at certain
pressure levels. Orig. art. has: 2 tables, 9 figures, and 7 formulas. [EGI
SUB CODE: 04/ SUBM DATE: lOFeb66/ oRiG REF: 002/ OIM REF: oo4l kTD Mssj5~~3(j

L 09183-6_? EWT (I) GW_
ACC NRi U)7002320 SOURCE CODE: UR/O362/66/C02/0O4/C)67/0)79
AUTHOR: _&Jj~evich M. S.
.'PAM
CRRG: Inatitut-e- of --Physic 3.. of the.Atmosphere (Institut fiziki atmosfery AN S53R)
i TITLE: Spatial structure of the field of terrestrial long-wave radiation,
SOURCE: kN SSSR. Izvestiya. Fizika atmosphery i okeana, v. 2, no. 4, 1966, 367-379
TOPIC TAGS: cloud cover, earth radiation
ABSTRACT: M. S. 14ilkevich has determined the relations between the statistical
characteristics of the spatial structure of the field of terrestrial long~'-iave
radiation and the temperature, humidity and cloud cover fields. He describes
the mechanisim of filtration -of high-frequency variations of nonhomogeneities of
i meteorological fields during the transmission of radiation in the at"mosphere and
with averaging for directions. Orig. art. has: 2 figures and 31 formulas.
IJFFZ: 36,2851
SUB CODE: 04 / SUBM DATE: 11Nov65 / ORIG REF: 006
Card 1/1 nst UDC: .5-51-.521.

LIFOVSKIYO ytlt-l # kand.tel:hn.muk; IMLSHIllp A.S.;
F.P.
The Z-15-1.4 exca-w-tor, 'L-!Ol:h. st:-oi. IE no. 2:25 F 161.
1. G-lavleningradshoy.
(L.-curating mchinez7)

-3-,
T
879-2-0
3/19 00110001004100'10'1~
B0 I 6XBO'58
AUTHORS- Plalkevich. S. a--. Chereshkevich, L. V.
TITLEt Fluorostyrenes. Report I. Synthesis of p-F_'u:)ro3tyrcne and
2,5-Difluorostyrene
PERIODICAL: Plasticheskiye massy, 1960, No. 4, PP- 1-4
TEXTt The authors report on the synthesis of styrenes fluorinated it'. the
ringt p-fluorostyrene and 2,5-difluorostyrene, as well as on their poly-
merization to polyfluorostyrenes. In their experiments they wanted to fend
out how this method of fluorination affects the properties of the polymers.
For this purpose, they synthetized the initial and intermediate prcducts,
fluorobenzene was obtained by the diazonium fluoroborate method from
aniline (Ref. 20). The yield amounted to 54% related to anillne; p-difluoro-
benzene was produced in several stages vla p-nitrofluorobenzene--.)p-fliaoro-
aniline--+ diazonium fluorophenyl fluoroborate. The synthesis of the inter-
mediate products was carried out as followsi p-nitrofluorobenzenet from
fluorobenzene by nitration with KNO -H2SO 4_ mixture; p-fluoroanilineg from
p-nitrof'Luorobenzone by reduction with irt) .1 furnings and HC1. The yield was
Card 1/2

87920
Fluorostyrenes. Report I. Synthesis of S/19 60/000/004/001/015
p-Fluorostyrone and 2,5-Difluorostyrene B016X,3058
79% related to nitrofluorobenzene. The oonversion of p-fluorean"line Irit~
p-difluorobenzene was also obtained by the diazonium fluoroborate method
and did not notably differ from the production of p-fluorob,-nzene from
aniline. The yield was 44% related to fluoroaniline. p-fluorostyrene and
2?5-difluorostyrene were obtained from fluorobenzene and p-difluoTobenzena,
respectively. These were converted into acetophenones which were subsequent-
ly reduced to carbinols. p-fluorostyrene and 2,5--difluorostyrene, respect-1ve-
lyg were formed by dehydration of the carbinols. The authors describe next
the synthesis of the p-fluoroacetophenone of 2,;-difluoroacetophenone (fo-r
the first time), of p-fluorophenylmethyl 3arbino'l, 2,5-di-fluorophenylmethyl
carbinol (for the first time), 2,5-difluorostyrene (for the first time),
and difluorobromobenzene (for the first time). The constants and propertiee
of all substances were described. A. V. Pavlova is thanked for her partilcl'-
pation in the studies. There are 20 references. 6 Scvlz:t, 10 US, and
6 German.
Card 2/2

87877
B004/BO64
AUTHORS: Malkevich, S,, G., Chereshkevich, L V,
TITLE: Fluoro Styrenes, Informatirn II Polymerization :f
Parafluoro Styrene and 2,5-Difluoro Styrene
PERIODICAL: Plasticheskiye massy, 1960, No. 5, pp, 3 - 5
TEXT: This paper discusses the block- and emulsion polymerization of
p-fluoro styrene and 2,5-difluoro styrene, and compares the properties
of these polymers with those of polystyrene and poly-2,5-dichloro styr~-n---
Block polymerization took place at 500 and 700C in s-~aled glass ampuls
with initiator (benzoyl peroxide) or without initiator. Solid, colorless-
transparent polymers were obtained which externally did not differ from
polystyrene and polydichloro styrene, With respect 'c th--'r rate of
polymerization, the compounds studied showed the following crder: dichloro
styrene) difluoro styrene> fluoro styrene, styrene The molec-.:-.,ar wei*'-~ts
depended on the polymerization temperature. Emulsion polymerization took
place in water with 0.2 %- ammonium persulfate as initiator, ani I ~~
sodium oleate as emulsifier, The ratio between monomer and water was
Card 1/2

87877
Fluoro Styrenes. Information Il. Polymerization S11911601000/00--l-02/020
of Parafluoro Styrene and 2,5-Difluoro Styrene B004/BO64
between 1:5 and 1:10.. Powdery polymers had a molecular weight -if between
100.000 and 230,,000, and could be molded into transparent, -,lorless
plates. Colored polymers of low molecular weight were obtained with ~hq
use of hydrogen peroxide as initiator and "Mopanzine sulfoni~: aci-I" as
emulsifier. As in block polymerization, polystyrene and polydIfluoro
styrene had a considerably higher molecular weight than pclyfluoro styrene
and polydichloro styrene. The heat resistance according to Vicat depenic-
on the monomer content of the product.. In this respect, fluorlne-,Lontainl:~--'
polymers were not superior to polystyrene, and did not reach the same b~a
zesistance as poly-2,5-dichloro styrene, The authors thank A V
for her collaboration, There are 7 tables and I Soviet referen--f-
Card 2/2

5" st so
83411
S/19ij6o/000/006/003/015
B004/BO54
AUTHORS: Valkevich, S. G, Tarutinap L. I., Chereshkevich, L. V.
TITLE: Spectroeopic linves Tig tion of the Structure and Thermal
Aging of the Copolymeriprom Tetrafluoro Ethylene and
Ethylene
PERIODICAL: Palasticheakiye massy, 1960, No. 6, pp.
T L.: The authors studied the thermal stability of the copolymer
CF ~H Films 60-80 p thick or powdered copolymer were
2-rs 2-CH2-)n'
hea to 200, 240, 275, and 290 C in the presence of air or in vacuum
(10- torr). The structural changes were observed by means of an infra-
red absorption spectrum taken on an MAC.-I 1 (IKS-1 1 ) apparatu.- r. %b N&CI
prism, At 2000C, the spectra were not changed even after 500 h, The au-
thors found that the copolymer samples exhibited differently strong branch-
ing which became evident in the intensity of the 1190 m-1 band (deforma-
tion Oocillaticno 0, iil;, -711, group)(Fig.1). After 1; h of heating to 2750C,

634u
Spectroscopic Investigation of the Structure S/191/60/000/006/003/015
and Thermal Aging of the Copolymer From B004/BO54
Tetrafluoro Ethylene and Ethylene
branched samples lost in weight up to 4%. Fig. 2 shows the weight losses
as a function of the intensity of the 1390 am-' band. Unbranched samples
were stable. Fig. 3 shows that the weight loss depends on the extent of
the contact area with air. Half an hour of milling of branched samples
at 1500C accelerated agingt the weight lose rose to 10%. whereas un-
branched samples remained unchanged even after 1 h of milling. The dif-
ference between branched and unbranched samples becomes obvious at 2400C.
While the latter show an unchanged spectrum, the spectrum of branched
samples shows new bands (Fig. 4): 1615 am-', 1780 cm-' (acid groups),
1755 cm-I(C-0 valence oscillations of the carboxyl group), and a not
identified 1677 am-' band. Beating to 2900C accelerates the oxidation
process (Fig. 5) while hydrogen fluoride is set free. The separation of
HP becomes evident in new absorption bands: 1720 cm-1 (C-C stretching
vibratiozis)f 1850 cm -1 (dehydrogenated fluorine groups)p and 5116 am-'
(stretching vibrations of the -C-H group); thus, the authors assume a
Card 2/3
83411
Structure S/191/60 /000/oo6/003/015
Investigation of the B004/BO54
spectroscopic Copolymer From
d Thermal Aging Of the es evident in a
an Ethylene and Ethylene
Tetrafluoro The destruction also becOO g tem-
ring of the SOften'n
_CF.CH- groups, d a love in vacuo'
formation of viscosity of the melt an ved when heating
reduction Of,,,). V0 double bonds were obser . The authors thank Osity
perature (Tat tg temperature increased
A. garakhonOT for Visc and
,scosity and softenit r advice~ I*
ation ~ap~repal&t'ons't&ble,
'j~
u~
V. Chul anovskiy fo for Prc are 5 figures'
professor oruiushina There
r_-_1 ~-Ao__rul e spectra-
deterainatiOnSO ~~tktiCngg ~e 1 British.
_f__ i 'US
La ot'nikoVa or I and
G. 1_-~ ~no ""-~_.2 30vietO
and ences.
4 er~
VA
'A .1

21136
MO 220S,1172 I akao 1043, ILI 11 8/190/61/003/004/011/014
B101/B207
AUTHORS: Kabin, S. P., Mikhaylov, G. P., Sazhin, B. I.
Smolyanskiy, A. L., Chereshkevich, L. V.
TITLE; Study of the dielectric losses and polarization of some fluoro-
plasts
PERIODICAL: Vysokomolek4arnyye soyedineniya, v- 3, no. 4, 1961, 618-623
TEXT: This paper studies the effect of crystallization upon the dielectric
constant 6 and tan 6 of the dielectric losses. Substances with the following
parameters were studied:
Substance: Denotation d200P g/cM3 E, 10 cps, tan 6, 105 melting
00C cps, OIC point, OC
polyvinylidene flu-
oride F-2 1.86 7.0 0.19 180
copolymer from tetra-
fluoroethylene and
fluorovinylidene 1:4 CF-1 1.s6 6.4 0.18 145
Card 1/7

Study of ...
21136
S/19 61/003/004/011/014
B1 01 YB207
Substa-ace: Denotation d2000 9/0M3 6, 105 ope,tan 6, 105 melting
OOC cps, OOC point, OC
ditto, ratio CF-2 1.91 a.6 0.09 16o
1:2
ditto, ratio CF-3 1.96 8.0 0.08 205
1 -. 1
6 and tan 6 were measured between -1500C and melting point of the polymer at
frequencies of 5-Io7 cps on 0.1-0-5 mm thick samples according to a method
described in Ref- 4 (G. P. Mikhaylov, B. I. Sazhin, Vysokomolek. soyed.,
.1, 9, 1959; Zh. tekhn. fiz., 25, 2186, 1955). The maximum error was less
than IW6. Fig. 1 shows F- and tan 6 as a function of temperature. The
maxima occurring therein which are caused by relaxation, were also observed
when tan 6 was a function of frequency. Since tetrafluoroethylene has a
symmetrical molecule with small dipole moment, the increase of E and tan 6
in the copolymers, is due to the polarity of vinylidene fluoride. Three
ranges of dielectric losses owing to relaxation were observed. 1) hivh-
frequency relaxation at CF-2 and CF-3 in the range of from -180- -1000C
Card 2/ 7

21136
Study of ...
S/190/61/003/004/011/014
B101/B207
(maximum of tan 6); 2) medium-frequency relaxation in all substances investi-
gated in the range of from -50- +500c, and 3) low-frequency relaxation at
+100--+2000C in all substances. Experiments carried out with hardened CF-3
showed a falling of high-frequency relaxation and a rise of middle-frequency
relaxation as compared to the non-hardened polymer. Fig. 4 shows the
frequency of the maximum of high-frequency and medium-frequency re-;axation
as a function of 1/T. 'The discussion of the experimental data led t o the
following conclusions: 1) The dielectric properties in the range of from
100-2000C cannot be explained by relaxation only. The structural transforma-
tions must also be taken into account. 2) The maxima of low-frequency re-
laxation lie close to the melting point of the polymers concerned, thus due
to thermal motions in the crystalline phase. 3) The dielectric losses de-
crease with the degree of crystallization of the copolymers. 4) Orientatio
of polyraers, i.e., increase of the degree of crystallization, may be ac-
companied by a considerable increase of E. There are 4 figures, 1 table,
and 11 references: 8 Soviet-bloc and 4 non-Boviet-bloo. The 2 references
to Eriglish-languaGe publications read as follows: M. E. Convoy et al.,
Rubb. Age, JAP 543, 1955; A. H. Willbourn, Trans. Faraday Soc., 54, 717,
1958-
Card 3/7

21136
S/19 61/003/004/011/014
Study of Bi 01 YB207
SUBMITTED. August 17, 196o
Fig. 1. Dielectric constant E and tan 6 of fluoroelasts as a function of
temperature. Legend: a) F-2; E: ) 2-1o4; 4)8-io5 cps;
1) 500; ?) 5-10.); 3
tail 6: 1) 500; 2) 2-1o4; 3) 6-10; 4) 8-10t) cps; CF-1-~- 1) 500;
fl 2.104 3 ) .10) ; tan 6: 1) 500; 2) 2-1o4; 61l~4;*4) 1-5-1o5;
5 1 ~6 68 -cps c ; 3) 1-5-1o5 cps;
.5-1 ; ) 1.2 io7 ps; 6) CF-2; E: 1 10; 2) 2- 04
tan 6: 2 22-1o4;12~ 6-10; 3) 1.5-1o5; 4) 1.5-106; 5) 1.2-10 cps; 1) cF-3;
I
C: 1) 10 ; 2- 0 3) 1-5-1o5 cps; tan 6: 1) 500; 2) 5-103; 3) 6-104 cps
r!Abst%-,racterls note: The original provides no data for curves 4)and 5)-'-
4
Card 4/7

ZO
4
1 1

Study of .,,
46
- 40
-30
8
23-136
3/19 61/003/004/011/0*14
B101%207
0.3
0,2 1 i -~,6 1
1 1
1 ~ I I i ~~ I c,-.-t-
1 ..
I
A
I
y
Card 5/7