ORIG. RUSSIAN: QUANTITATIVE INVESTIGATIONS OF ATMOSPHERIC MOTIONS BY MEANS OF RADIOACTIVE TRACERS

• Document Type: CREST
• Collection: General CIA Records
• Document Number (FOIA) /ESDN (CREST): CIA-RDP88-00904R000100100002-8
• Release Decision: RIPPUB
• Original Classification: U
• Document Page Count: 19
• Document Creation Date: December 22, 2016
• Document Release Date: August 12, 2009
• Sequence Number: 2
• Publication Date: May 1, 1964
• Content Type: STUDY

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Third United Nations
International Conference
on the Peaceful Uses
of Atomic Energy
Confidential until official release during Conference
A/CONF. 28/P/383
USSR
May 1964
Original: RUSSIAN
QUANTITATIVE INVESTIGATIONS OF ATMOSPHERIC
MOTIONS BY MEANS OF RADIOACTIVE TRACERS
Karol I.L., Malakhov S.G., Vilenski V.D., Dmitrieva G.V.,
.Krasnopievtzev Y.V., Kirichenko L.V., Ssissiguina T.I.
Introduction. The use of radioactive isotopes in meteoroldgical
investigations as air mass, cloud element and precipitation marks
was widely discussed in the literature (see for example C3,). Used.
as such tracers, natural radioactive nuclides (radon, thoron and
their decay products) arriving into the atmosphere from the ground,
or produced there by cosmic rays, possess ,a number of advantages
compared with artificial isotopes (nuclear explosion products).
Sources of natural atmospheric radioactivity are relatively well
studied. They are approximately stationary and so located, that
transport of isotopes in the troposphere and lower stratosphere
occurs both - upward (radon, thoron and their decay products) and
downward (cosmic-ray-produced isotopes). This permits besides the
quantitative study of air mass motions to estimate parameters of a
series of atmospheric processes.
In the present paper a series of such investigations, based
on measurements of radon and its decay product containedin air and
precipitation are summarized. These isotopes are used for estimating
vertical turbulent diffusion parameters in the lower troposphere
03) in the. stratosphere (?2) and also the rate of exchange through
the tropopause or between the stratospheres of both hemispheres
02). In ? 3 these isotopes are used for the determination of
washout rate of radioactive aerosols from the troposphere, and in
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11 4 they are applied together with some artificial isotopes for
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distribution 41J
for a best coincidence of the theoretical and measured concentration
P
parameter. The value of is then estimated from the condition
concentration distribution of Rh, or of its decay products, a
theoretical formula is usually developed containing //
g* rj e
? 1. Estimation of the vertical turbulent diffusion
coefficient from the vertical profile of radon and its short
lived decay product concentration
For the determination of Kga from the measured vertical
In the ground atmospheric layer, with the radon source assumed
stationary. Under certain boundary condition the solution of thA
concentration distribution may be considered one-dimensioral and
..~ ucvcLVFJliJ~j tt ineorezleal formula for the vertical volume
to be &- uniformly and continuously emanating plane, the problem
_r -
the law governing the K variation with 1tit d
s
expressions for the above considered distributions depending on
.equations for turbulent diffusion en gives the following
u e l,2' 3.4j :
b)-K 4 ?'- (-a) _ AE,'r /zK M A
When:
z(~~+Nko(x)~
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The following notation is used here: radioactive decay
constant; E - exhalation rate: q 0? E
W(XH)-ii(xoJ [Ko( ) "f(XH)J \~`z), ~~lx1
J
are modified Bessel functions: aC =,~ xh = x' =H ;
B - an arbitrary constant: 0 < n 4 3 and depends on the
ground layer stratification.
By use of these formulae the value of is estimated from
the radon concentration ratio at two levels, or from the ratio of
radon concentration at one level to the exhalation rate E [3],
For thel ground layer of the atmosphere the data of k!.
(value of k . at the I m level) are given in Table I for the
ground inversion conditions and for H=IO m. For comparison
meteorological estimates of k1 are also given in Table 1. The
ratio -Y C m)/E as a function of ki is expressed in Fig. I as
result of measurements under convection conditions and of calculations
by means of formula /1.3/ for H=40 in. Good qualitative agreement
between experimental and theoretical data was obtained in both
cases, although sometimes essential quantitative disagreement was
observed -
In In the boundary layer of the atmosphere we carriedl~concentration
measurements at seven levels of the meteorological tower in the
layer 0-300 m. The estimates of Kz obtained by means of formula
/3.4/ under ground inversion conditions are given in Table IT [6]
In the free troposphere the aircraft measurements of vertical
profiles of short lived radon daughters in different regions of
the U.S.S.R. under the different 'erent meteorological conditions allowed
to obtain estimates of (C7 by means of formulae /1.4/ and
/i..i/. Some of them are given in Table III.
Systematic observations of Rn and its. short-lived decay product
concentration distribution are useful not only for estimating
but also for studying other meteorological pro c.esses, such as genesis
development and destruction of inversions, development of convection
atreama, etc. Average exhalation rates for regions with linear di-
mensions of 1-3 thousand km were estimated by means of radon con-
centration vertical profile integration in the troposphere. In
different regions of the U.S.S.R. these values vary from 0.9 to
8.0 10-13 cu/m2 sec.
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 We calculated the Rn concentration vertical profile distortion
in the ground layer of the atmosphere, caused by the spatial
inhomogenity of exhalation rate taking into account the average
wind speed and for K'z= k12 For the doubling of Rn
concentration at the I m level over the leeward boundary of the
high exhalation rate zone with E'r= IOE 2 ; 4 I I0-12 cu/m2 sec the
linear dimension L of this zone should be LNI km, for the same
effect at the 100 m level : L ti 50 km. Thus, with increasing
altitude the small inhomogenities in E are rapidly smoothed out.
. Estimates of average exchange parameters in the
35?N, I0?N, 40?S and at levels: 4,6; 7,6; 12; 15; 18 and 20 km inI
p
radon decay chain with T~t = 22,3 years was used. These concen-
trations were obtained by aircraft measurements at latitudes 70?N
mouthly concentrations of PbI0 (RaD) - long-lived isoto e of
the K2 value in the lower stratosphere. For this purpose the mean
coefficient K, propozed in ? T_ is Ann] i Pri hay-o- fni+ oo Fin,a+;,,n
stratosphere from its RaD Pb `l~ content measurements
The method of determination of the vertical turbulent diffusion
May 19 60-61 and in November 1960 [77 (Fig. 2).
and one dimensional, since as seen from Fig. 2 at the tropopause
stratosphere may as a first approximation be considered stationary
Tne mathematical problem of constructing a vertical profile
of the Ra D concentration in the upper troposphere and lower
latitude and was decreasing with altitude about equally during both
level and higher this concentration was almost independent of
gives the following expression for, the concentration c (z,w) per
ordinary differential equations with suitable boundary conditions
3 - the stratosphere, integration of a system of turbulent diffusion
washout by clouds and precipitation) ; 2 the upper troposphere and
the following layers: I-the lower troposphere (the layer of aerosols
For the stationary model of the atmosphere, consisting of
months of observations.
air mass unit of Re D atom ' fraction, which, is connected in the lower
stratosphere with aerosols having a gravitational velocity w:
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where F (w,....) and 5 (w, R, ....) are independent of z;
z = hT is the tropopause height-
It can be assumed that the distribution in the stratosphere
of the number of aerosol particles n(r) by their radii 'r has a
density
J'M/ d e"" =QK
(2.2)
where : A k =conat. ae4 = 0 for Luken nuclei with radii of the
order of Y. IO-c. G y' L r, = IO+ ; ae~ = 3 for large
particles (Junge sulphate particles) having r, r Z' k'
[7,8] Assuming that the average number of RaD atoms per aerosol
particle is about 8 rm ( B = const. and 3 4 m < 3), the following
expression of the summary RaD concentration over all fractions
of the stratospheric aerosol is obtained:
WL (M) N
CCU) = e- (31W) o~Q Q ~r,, r)= gr dr. (2.3)
The density QOM)/c N QN c d /AW of distribution having
a sharp maximum, corresponding to Y' = r, , W = W, , the
assumption of
-Xk
exPIP* (6-hJ] F c~w= exp[ , T)] F,
07w
W.
ft W-Z w, may be made with sufficient accuracy.
From the average values of , which are determined from
the ratio. ofRaD concentrations, measured at two stratosphere
levels, values of ks ~ shown in Table IV are obtained for Y?, =0,0 ~
0,3,tc and 0,3 as the range of variability and the most
probable value of r,, respectively {8.J .
Table IV shows that maxima values of ~" are observed in
spring in temperate latitudes of both hemispheres, and the minima
ones - in the equatorial zone This corresponds to the existing
qualitative picture of seasonal and latitudinal variatious of
in the strato-phere, which is obtained from the observations of
the nuclear explosious debris propagation [7] The order of
magnitude of K is close to the estimates obtained in 171
though its value is a .little lower,
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the northern hemisphere being three times that of the southern one,
Rn enters the stratosphere mostly in the northern hemisphere
producing there RaD. The comparatively long residence time of RaD
in the stratosphere leads to the levelling of its content in both
hemispheres and a summary withdrawal of RaD from the southern
hemisphere stratosphere occurs.
The annual mean values of all the Rn and RaD fluxes were
calculated as arithmetic means of their values for May and November
in extratropical latitudes. Values of R. and these fluxes obtained
from measurements in latitude 70?N are considered to be valid' for
the. belt 90?- 50?N, those from latitude 35?N for the belt
a free atmosphere permits to find the average rates of Exchange
through the tropopause and between the stratospheres of both
hemispheres. Fig.2 shows that the meridional distribution of RaD
concentration at the 4,6 km level is similiar to the land area
distribution over the entire zonal belt area. The land area in
here and in ? I together with the estimates of the average radon.
exhalation rate E and above mentioned RaD concentration data in
The values of ~a in troposphere and stratosphere obtained
50 0-200NO and from 40?S for the belt 20-90?S. The fluxes of Rn
The following notation is introduced here: I V (Ia) - annual
mean number of RaD atoms in the stratosphere of the northern
(southern) hemisphere (in the layer between the tropopause hr
and~n~ T t I levels)
r 'ff annual Rn atoms influx in the stratosphere of
T-!IV t-+S
.r (R0. B) (R0.D) northern (southern) hemisphere;
(Trs ) - annual 3,1% decrease of RaD in the stratosphere
and RaD through the tropopause of belt 20?N 20?S are considered
to be negligibly small because of the strong stability of the
tropical `stratosphere (this is supported by observations of the
stratospheric fallout of nuclear bomb debris [7D.
1' a - annual summary flux of RaD from the stratosphere
J,C
or the northern (southern) hemisphere due to
(R D) radioactive decay;
or tae .northern to the stratosphere of the
- annual outfiux of ReD from the stratosphere to
11 t~T
Nab) southern hemisphere;
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From the obvious balance equations for the stratosphere of
the : a/ northern hemisphere; b/ southern hemisphere
a .~.(Rf) .1,(Rd) .r.(RCl) ) ~) .~-j-(RaD) + 1T(R"~ - .(RID) (RaD) = 7T
r-+4 t4 n~ -rs nl -+s S s -~ r
and for the three groups of the Kz values given in Table IV
the values of these fluxes are obtained and listed in Table V.
The values of
(k,) (RQD) (RaJ)
L4_ =Td/ "HT-+W s^ "S/ 3'j-T ; w-~S_ Lq /R,,-).s
residence time of the ReD atoms in the stratospheres of both
hemispheres are also given in Table V. These values are obtained
under the assumption that as a first approximation the exchange
between these reservoirs obey first order kinetics laws . ~, ZS
and are close to one anothr and also to the known estimQtes
of air mass exchange rates between the tropospheres and stratospheres
of both hemispheres [7,9]..
The last column of Table V shows, that the annual increase
of RaD atoms in the stratosphere of the southern, hemisphere from
the decay of Rn of this hemisphere is about 20% of their influx from
the stratosphere of the northern hemisphere.
? 3. Estimation of the mean remouval rate from the
troposphere of natural radioactive aerosols by
clouds and precipitations
The simultaneous measurements of Rn and*its long-lived decay
product content in the ground-level sir gnd in the precipitations
are used for the determination of the mean remauval rate of these
substances from the atmosphere. This quantity characterizes the
remouval rate of aerosols being carriers of the isotopes under
consideration [I] .
The average residence time `C of natural radioactive aerosols
in the atmosphere is usually determined by the disturbance of the
radioactive equilibrium relation between the concentrations of radon
decay chain elements measured in ground air and in precipitation
It can be shown that no significant amount of RaD atoms enters
the stratosphere from the troposphere.
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 from the following equality:
means of formula (3.1) in different points of the globe. In
Till recently the value G was- incidentally estimated by
in the ground air layer. The obtained results are given in Table
1959.1960 near Moscow an attempt was made to find the seasonal
variations of L from measurements of radon and ReD concentration
should be mentioned.
tine minimum values observed in February, September and October,
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A
+
in which $I - is the, concentration Ofthe chain isotope
decay constant, r, A L. - average residence time of element
in the atmosphere [I,
3.1)
expressed in atoms per unit volume, A ? - its radioactive
VI. No distinct seasonal variations of G have been detected. but
troposphere LIIJ
and aerosol washout by clouds and precipitation in the lower
difrerent isotopes estimated by mesas of formula (3.I). appears to
be different, what is obviously not true for the aerosols carriers
of these isotopes. We proposed the model which permits as a first
approximation to find a separate contribution to G from two
fundamental processes; turbuleht aerosol diffusion in the troposphere
The use of formula (3.I) for estimating the average removal
rate of radioactive aerosols gives unsatisfactory results, since
the obtained estimate describes quattitatively the resulting
effect produced by different processes removing aerosol from
different atmospheric layers II . Thus the residence time of
and having a constant average washout coefficient 6 throughout
radioactive aerosol occurs, following the first order kinetics law
.iii usion coefficient K-z throughout the entire troposphere. It is
further assumed that in the lower layer stationary removal of
In the proposed model a horizontally homogeneous twola
er
y
troposphere was assumed A having a single constant vertical turhnl An+
tine entire layer. As a first approximation the washout of the
considered to be in radioactive equilibrium with radon.
snort-lived isotopes was not taken into account and they were
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T1 2 3.85 days); I) Rai (P121? TI/2= 22.3 years); 2) RaE(sjl o
TI/2' = 5.0 days) and 3) Ra F (0' o , T I/2 = 138 days).
Vertical distribution of volume concentration q, 4 ( ~)
( L= 0.., 2, 3) of these isotopes is found in [J I] by solving a
system of ordinary differential equations of turbulent diffusion
with suitable boundary conditions at ground level ( Z = 0 ), Z-+0"10
and at the boundary separating both layers ( Z= n ). The specific
activity ratio for a pair of decay chain isotopes at a level T< ii
expressed by:
i 21 ~ r X), k > I?, (3.2)
KJ
was found to depend on radioactive decay isotope constants Ai
and on dimensionless parameters:
(3-3)
The value of is determined from measurements of the isotope
concentration ratio in the ground layer and in precipitation. The
following two extreme assumptions are made in the last case: A)
the specific isotope concentration ratio in rain water was equal
to the average concentration ratio in air over layer 0< B < n :
h
CK)
)=/kkQk/ALQL; Oi
(3.4)
This means that radioactivation of rain drops occurs about equally
throughout the entire washout layer. B) The ratio of the specific
isotope concentrations in rain water was equal to - he ratio, of
k
these concentrations in air a level of Z = k : ( i k ~ 12e~
i.e. radioactivation of rain drops occurs mainly in the upper
part of the cloud layer ITT] .
The calculated graphs, given in L11J show/the dependence of
the dimensionless washout coefficient = 6/ A, on the ratio
of spe? fic ac ivities of RaD/Rn. RaF/R iD RaE/ReD? in gr o 5nd level
air l~ . (-a= 0) in precipitations: x (case A), :kCJl)(case L B)
for a number of parameterzvalues. From these graphs and published
results of such measurements of these is-otopes specific activity
ratios values ofwere determined. The values of obtained for the
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same value of Zr` for different :isotope pairs appeared to be
close to one another and the values of t 4/6'', 5.5G/f (days)
close to the residence time of aerosols in the lower troposphere
'(1-10 days), calculated by means of a formula of the form (3.I).
With measured R&E/Ra D ratios and the assumption B) the values
of 6" obtained for all values of 8e , are unreally overestimated
and coincide with the estimates of its "instantaneous" values
during the rain [12]
The single-valued determination of and requires
simultaneous concentration measurements in ground air for at least
three of the above mentioned isotopes. The results. of such measu-
rements carried out in. Freiburg (FRG) in summer of 1957 and in
Moscow district at the end of 1963 together with the corresponding
values of d? and are listed in Table VII. The obtained values
of e are of the same order of magnitude as the estimates of
the radioactive aerosol washout coefficient made by different
methods I1, 12 .
Knowledge of the average radon exhalation rate E from soil
in the region during the ground concentration measurements permits
to estimate the remaining parameters of the model - ez and t~ .
In the cases listed in Table VII these estimates were obtained
from the relation Q o ( o) E/ following from (I.I) and
from formula (3.3), with the average value of E = 40 atoms/cm2min
They are for Freiburg - k2 = 25 sq.m/sec; k= 3.8 km; for Moscow
district = 4.2 - 8.3 sq.cm/sec; h = 0.7 - I.I km.
These are very rough estimates since in the assumed model
the decrease of W2 with decreasing 2 in the ground layer, where
measurements were carried out, was not taken into account and the
measurements of E were inaccurate and quite insufficient in
number (? I).
Estimates of washout coefficient 6" of radioactive aerosols
containing RAl almost coinciding +x th the above estimates, were
obtained for a three-layer model of a horizontally homogeneous
stationary atmosphere described in ? 2. Making use of the estimates
of the vertical turbulent diffusion coefficient ~, in the troposp-
here obtained in ?, It it is possible to find unambiguously rather
close limits within which the washout coefficient 6'
and the
height of the washout layer h should lie, in order to obtain the
measured value of the RaD concentration at the tropopause level 11
__ 3 8.3 . _ _ - -- - r. ?
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For these concentration values given in Fig. 2 at measurement
points, in latitudes 70?N and 35?N, the following values, are
obtained: G= 3.2 4.4xI0`6 sec-I) and = 7 9 km. The latter
value corresponds to the average level at which the upper cloud
edge of the upper cloud layer is situated, which thus also takes
part in the removal process of aerosol from the troposphere.
? 4. The use of radioactive isotopes in synoptic
investigations
Radioactivity of air and precipitations can be used in
synoptic investigations of vertical and horisontal transport,
interaction and transformation of air masses. The problem to be
considered and the conditions of the study determine the choice
of isotopes (or their combination) as a tracer. it is convenient f.
inst. to use isotopes of stratospheric origin (natural coemogeni c
isotopes, or nuclear bomb debris during periods free of nuclear
weapon tests) in the study of stratospheric air transport into the
troposphere. Transfer of tropospheric air into the stratosphere can
be determined by the change of radon and its decay product content
in the stratospheric air samples.
The gross beta, activity of fission products was chosen as the
stratospheric air tracer in the study of synoptic conditions for
stratospheric a it transfer into the troposphere. The daily fields of
grass beta activity of artificial origin in ground level air over
a wide territory in temperate latitudes were compared with the
300 mb isobaric surface charts and weather charts. We consider the
suddenly appearing and Sharply outlined regions of high level
ground air radioactivity as having been formed by air masses of
recent stratospheric origin so the conditions for their appearance
being favourable for the penetration of stratospheric air into
the lower troposphere.It was found that: I) In an overwhelming
majority of cases the "radioactive spots" near the ground appeared
behind the cold fronts in the rear of the well developed cyclones,
2) The appearence of these "spots" was often accompanied by the
formation of a ridge in the lower troposphere; 3) During the following
days such a "spot" was usually moving along the ridge periphery
to the south-western then western and north-western directions up
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to the moment when conditions for condensation and ascending
motions arose; The above considered synoptic situation was
usually accompanied in the upper troposphere by an intersive trough
of a sharp profile and very high wind velocities on its periphery;
5. As a rule the length of such troughs was about several thousand
kilometres, but ground level radioactive "spots" most often appeared
under the southern part of the trough, where on its axis, to the
left of the jet steam a sharp decrease of baric gradients and wind
velocities was observed.. In many cases in this part of the trough
formation of a cut-off upper cyclone occured.
The revealed conditions of the atmospheric process development
in the lower and upper troposphere under which penetration of
stratospheric air into the ground layer takes place, permitted
not only to understand better the mechanism of this transfer and
of the radioactive fallout patterns but also to come near to
forecasting the appearance of high radioactivity level regions in
the surface air.
Different radioactive characteristics of the ground level air
(Rn, RaD, Sr90 and gross beta activity concentrations.) obtained
in summer 1960 at_ a research ship on its passage from Odessa to
Vladivostok combined with the results of synoptic studies permitted
on the one hand to show the influence of atomospheric processes
on global distribution of radioactive isotopes in the tropical
regions and on the other hand to refine the analysis of the atomosp
heric processes from radioactivity characteristics. The high levels
of long-lived fission product concentration to the north and low
ones to the south from the tropical convergence zone, connected
with the axis of the soutern Asia summer depression (Fig,3).
snow its role as a barrier to the interlatitude air mixing.
The most significant increase in radioisotope concentration
in the equatorial zone coincided with the change in wind direction
when the ship passed from the air current system of the northern
hemisphere into that of the southern hemisphere. These increases
and the observed Weather conditions permitted to assume the
existence in the equatorial region of the Indian ocean of a second
convergence zone, separating the low radioactivity level air of
the northern part of the Indian ocean from the higher radioactivity
level air arriving from the southern hemisphere (see fig-3). DurUg
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the period under consideration in the southern (winter) hemisphere
synoptic conditions existed for the penetration of stratopheric
air into the lower toposphere over the Australian region and for
its further displacement over the Indian ocean towards the
equatorial zone.
Observations of fresh fission product spreading carried out
in fall and winter of 1961-62 at a research ship in the troposphere
of equatorial Pacific permitted to estimate its meridional
velocity.
The value of this velocity (I,0 km/hour) was found to be
close to its estimate 1,3 km/h, obtained from the observations
carried out on the 80OW meridional network of stations for the
same period [13]
Conclusion
From the above given brief survey of meteorologic investigations
by means of radioactive isotopes the breadth and fruitfulness of
this new trend in meteorology can be seen. It occupies an important
place in the new branch of atmospheric physics-nuclear meteorology.
Further developments in this direction require a sharp
increase in the number of measurements of natural radioactive
isotopes particularly in a free atmosphere during different seasons
in different geographic regions, as well as a close cooperation
of physicists and meteorologists in obtaining and interpreting
the results of such measurements.
R e f e r e n c e a
I.I{apo,n, Y.JI., MaJraxoB C.r., C6. cTaTeP1 "Bornpoo& flAepHog McTe
opoxormm" , IbcaToMHSAaT /I962/, 5-42
rax,uxx JI. C. , Co.noBei ux P.3. M8B AH CCCP, c eni re CdPI3xgecxax
9 7 /1960/, 1077-1081.
3 ? raxAHH ConoBei nc P.3. TpyAx i3cecoFo3Horo HaygHoro
McTeopoxorggeclcoro CoBeuiaxr x, YII /1963/, 179-187.
4. Ma.naxoB c.r., M3B. AH CCCP, cepR reo ix3necxaH, 5 9 /1959/,
I344-I352.
5. KxpI exxo JI. B. C. oTaTe2 "BonpocH . epxoR McTeopoxorHM"
IbcaTOMia3AaT /1962/, 75-103.
383
13 -
M
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6. Cnrczrmm '1'.14. 143B. AH CCCP cep.reo- )N3 . A 3 /1964/ 414-421.
7. Stebbins A. (Ed) Second special report on high altitude
sampling program. DASA 539 B (1961). U N document A/AC.82/G/L.
741.
8. Junge C.Chagnon C. Journ. Meteor., I8, No I (1961), a1-108.
9. Junge C., Journ. geophys. Re s . , 68, No 13 (1963) , 3849-3862.
10. Fry L. Menon K. Science, 137, No. 3534(1962)994-995
ii. Kapojm M.J1. 1/:3B. AH CCCP, cep, reo Y3Ntiecxax, If 11.(1963),
17I8-1729.
12. Ma.naxoB ".r., ComAxxHFia JI.r't. C6. cTaTeli "13oppoca uepxot
McTeopoxomm" rooaTOMYl3AaT /I962/, 151-162.
13. KpacxorieBuee :0.3. "?4eTeo oJIorBR x rmzpoj orHA" ! 4 /1964/ 3-8.
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 Approved For Release 2009/08/17: CIA-RDP88-00904R000100100002-8
Table I. Vertical turbulent diffusion coefficient
at I m level k, (m2/sec) for ground inversion conditions
Date and time
_1n)
Meteorological
of measurements
E
(sec/m)
1
from (I.3)
estimates of ki
13/VIII 21h 30m
I.7xI0
0.01
0.003
14/VIII
Ih OOm
2.9x103
0.005
0.009
14/VIII
5h 00m
6.4x103
0.0008
0.0015
15/VIII
20h 30m
I.7x103
0.01
0.0024
16 /VIII
Oh OOm
4.2x 103
0.001
0.0024
16/VIII
4h 30m
6.0x103
0.0008
0.0015
Table II. Vertical turbulent diffusion coefficient V.
(m /eec) in layer 0-300 m and under ground inversion
conditions
Date and time of
measurements
inversion oT in invers-
altitude (m) k,, k Z in layer
( C)
6/Ix 22-23h I00
IO/VIII 21-22h 75
3 /IX 20-2 Ih 75
21/IX 19-20h. 75
0.003 -4
/to 25m/
0.04 3.0 -7.3
0.0054 - -2
0.051 0.48 -2.9
Table III. Vertical turbulent diffusion coefficient
2
m- Jsec in the troposphere from aircraft measurements
Meteorological Region of Levels of Number values
conditions measurements measurements of measu- ~Tt~T~00 Tro"4O+4f171
(km)
Stable stratified U.S.S.R. 0,05-I,0 12
troposphere territory I,0-5,0 12
In the convection Europian
layer part of USSR 0,05-I,5 9
Middle 0,05-4,0
Asia
3 0,4-30
50 20-1000
5 0-3 000
50-I04
0
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 Approved For Release 2009/08/17: CIA-RDP88-00904R000100100002-8
Table IV. Turbulent diffusion coefficient u~ of natural
radioactive aerosols in the stratosphere (m /sec)
Latitude
=0.03 ,
rt =
0.1 P.
r1 = -0.3
May
November
May
November
May
November
70?N
0.087
0.045
0.18
0.11
0.38
0.27
35?N
0.13
0.068
0.24
0.I4
0.47
0.22
10?N
0.044
0.044
0.I2
0.I2
0.29
0.29
40?S
0.054
0.13
0.13
0.22
0.30
0.46
Table V. Rv, and V.aD atom fluxes (I022 atoms/year) and
their average residence timeT(years) in the stratospheres
of the northern and southern hemispheres
-1-'N'
6.3 I022at:oms
Mal)) _ _- 0.20
.[.r cs 0.19
?, TS 6. 10
]. 22 atow+s
rs
'9 (aw)
ni
TlaaD~
L At
S
11 (RV,)
(RaD) I--
L
~
is
:. L
~j lR"1'
~
T-+N
N-,S
-+
T--PS
S
S-.T
cL
?T-4S
0.3
4.1 I.6
3.9
1.6
0.8
4.5
1.3
I.4
0.22
O.I
3.0 2.1
2.8
2.3
0.6
3.2
I.9
2.0
0.22
0.03
2.2 2.8
2.0
3.I
0.5
2.3
2.6
2.7
0.22
Table VI. Monthly average Rvt and 12a-D concentration in
ground layer of the atmosphere and value of r from
measurements in Moscow district (1959-1960)
II LII IV V VI VII VIII IX X XI XII
Rn concentration
in. IO-IOcu/m3- 1.2 0.6 0.7 0.4 0.3 0.4 0.6 0.8 0.6 I.0 I.0 -I.6
RaD concentration
in10-15cu/m3 11 .6 3.9 8.7 5.0 4.7 4.2 7.6 8.3 4.67.320.4 12.5
L (days) 1-1 0.8 1.4 I.5 I.8 1.2 1.4 1.2 0.9 0.8 2.3 1.0
383
-I6-
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 Approved For Release 2009/08/17: CIA-RDP88-00904R000100100002-8
Table VII. Washout coefficient 6 and average residence
time L in the atmosphere of long-lived radon decay products
Locality and Ratio of ac r1. (days) for ratio 6 -I
time of mea- tivities for ratio sec
surements
RaD
4E
RaD
Rae
RaD
12aE
4,
RaD
Rvv.
Ra)
V, V"
RaD
Moscow
district
X-XI-63 fi7/x
I.IxIO-4
0.47
1.3
8.4
0.37
9.5
9.1 I.9xI0:5
Moscow
district
XII-63 / /x)
0.9x10-4
0.32
1.0
4.5
0.70
6.3
2.2 I.4x10-5
Freiburg
Summer 57
I.9XI0-4
0.07
2.I
21xa
1.1
2.2
2.3* 4.7xI0-6
x) The brackets indicate the number of measurements used in
averaging.
xa) These values are determined for the activity ratio aF'/'RaD.
383
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 Approved For Release 2009/08/17: CIA-RDP88-00904R000100100002-8
Al 0.4 14 R1 I,0 li
Fig.I. Calculated and experimental values of as functions of ki
(convection conditions),
ro
s
7
2
culta,
I4 ae
W, '~o~tal. kotC11
Jr
0 1015 Z/110
1020
1015
sr eo? 'r~ e0 s0? 16 w' 20' i0 r r 20 J0? I0 s0' a
N
Fig.2. Meridional distribution of Ra D conoent`ration (d.p.m.per kg of air) in
May of 1960-61 at levels: of 4,6 km; of the tropopause (hT); of 3 km below the
tropopause (hT 3km); of 2,5 and 8 km above, the tropopause (hT+2km etc); and a
hystogram of the land area percent in the zonal belt.
`-~ lam
darn/ka r..;r_
a
1020 /0/5 /0/0 /0/0 /015
/0/5 /0/O
Fig.3. A synoptical chart on July 16 of 1960 and the supposed situation of the
second convergence zone (dotted line) in the equatorial region; m= - the
dividing zone,oonneeted with the South-Asia depression and ? - the ship's si-
tuation. 3B3
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