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Seasonal variations in the semi-diurnal tide in the upper atmosphere as determined from radio meteor observations
Journal of Atmwpherlc and
Seasoual
Terreatrhl
Phyaica, 1971,
Vol.SS,pp.807-814. Pergamon Prcua.Printed InNorthern Ire&ad
variatim in the semi-diurnal
in the upper atmomhere
tide
as determined from radio meteor observations G.
M. TE~TIN and V. M. STAROS~
Radioastronomy
Department,
State University,
Kasan,
U.S.S.R.
(Received 23 April 1970)
Ab&ac&Cormctions to the wind velocity for finite width of aerial polar diagram, and for non-uniform sensitivity of the radio meteor method to dif%rent values of velocity, have been calculated for eight stations in the northern hemisphere. The corrected wind data are used to study seasonal changes in phase and amplitude of the semi-diurnal tide in the upper atmosphere. These seasonal variations are analysed into harmonic components of periods 12, 0, 4 and 3 months; the component of period 12 months is found to have the largest amplitude. Similarities of seasonal behaviour are &dent at all eight stations. 1. INTRODUCTION
number of stations carry out systematic measurements of winds at altitudes of 80-100 km uaing radio observations of drifting meteor trails. However the results obtained with equipments of different characteristics are widely different, because of systematic errors in determining the wind. Important contributing factors are the non-uniform sensitivity of the radar method to wind velocities of different magnitudes, and the finite widths of the aerial polar diagrams. A typical characteristic of station sensitivity to wind velocity is shown in Fig. 1. The influence of the finite width of the aerial polar diagram has been discussed elsewhere. Corrections to wind velocities were carried out by the method described by TEPTIN (1969) and POPISHEV and TEPTIX (1971). Data from the following eight stations in the northern hemisphere was used: AT PRESENT
1. 2. 3. 4.
a
Jodrell Bank Shejield Kiev Kharkov
(NEUFELD,
1960; GREENHOW
(LYSENKO,
1963;
1967; KASHEEV
5.
Obninsk
and NEIJFELD, 1961).
(M&ER, 1966). (FILLLKO, 1969; LYsENK0,1969).
(KASHEEV
KASHEEV,
LEBERDINETS
and LACXJTTN,
and LYSENKO, 1967).
and LYSENKO, 1967; AREFEJEVA, 1966; LYSENKO,
1969). 6.
7. 8.
Karen Frunze Dudmnbe
(ZADORINA et
al., 1967)
(LYSENKO, 1969; BIBOSUNOV and KARIMOV, 1966). (SHAMSUTDINOV and CHEBOTAREV, 1969).
In the present paper the corrected values of semi-diurnal tidal wind velocities for the above stations are analysed. 2. RESULTS work on the Fourier analysis of the diurnal change in wind velocity have shown that for most stations the semi-diurnal component (12 hr) haa the largest amplitude, followed in magnitude by the diurnal (24 hr), which is followed in turn by the 8-hr component (e.g. ROPER, 1966; POCKROVSKY and TEPTIN,1970). The standard method of analysis (GREENHOW and NEUFELD, 1966) presents the Previous
807
G. M. TEPIXN
808
and V. M. STAROSTIN
Fig. 1. Typical characterietic of radar station sensitivity to wind velocity (Kazan, continuous line--phase-time velocity
registration,
dashed line-sector
registration).
values V observed during 1 month in the form V(t) = 7, + V, sin 15’(t + yI) + V, sin 30°(t + ya) + V, sin 45’(t
+
YJ
where V,, V2, I’, are the amplitudes and vtyl,ya, ws are the phase of the first (24 hr), second (12 hr) and third (8 hr) harmonic components, and V, is the prevailing component or monthly mean. This analysis is carried out separated for the NS nd EW components of velocity. In the present paper we consider only the semi-diurnal component. Even the earliest observations showed that the amplitude Vv, and phase ys, of this component change appreciably from month to month. Figure 2 gives typical observational results for Sheffield as a ‘harmonic dial.’ The distance of each point from the origin represents V,, and the angle (measured anticlockwise from the x axis) represents yz. The points are numbered 1-12, one for each month of the year. A question arises as to whether these changes from month to month are real, or whether they are to be ascribed to experimental errors. To investigate this point, the monthly values of amplitude of the semi-diurnal tide were analysed as a power spectrum over the range of periods 2-14 months, using data from Jodrell Bank (195358), Kharkov (1961-65) and Frunze (1964-65). As a result it became clear that the values are not random, but have a clear 12-month periodicity. The same analysis was carried out for the phase of the tidal component, and again the predominant period was 12 months. These results are illustrated for Jodrell Bank in Fig. 3. The calculations of the power spectra were carried out as described by BLAUKM and TUKEY
(1958).
The fact that the predominant period found is 12 months, suggests the use of harmonic analysis of the seasonal changes, using harmonics of periods 12, 6, 4 and 3 months. Such an analysis was carried out using the method described by SIEBERT
Seasonal variations in the semi-diurnal tide in the upper atmosphere
809
Y
2 4 mkec -
9 >
/_ x
Fig. 2. Mean month velocity values of semidiurnaltides (Sheffield,noncorrected values, N-S). (1961). Consider one component of the wind, say the NS component. The amplitude and phase of the semi-diurnd tide in this component can be represented by the sum of a constant vector and a series of ellipses which are traversed with periods of 12, 6, 4 and 3 months. The largest ellipse is, of course, the one of 12 month period, as this is the predominsnt seasonal component. A similar analysis can be carried out for the EW component. The data was corrected for non-uniform sensitivity to wind velocities and for aerial polar diagram as explained earlier. In order to confirm the validity of the harmonic expansion, the average deviations of the sums of the mean snnual value and the four harmonics from the actual experimental points were calculated. Most of the deviations only slightly exceeded the errors of individual measurements and were always considerably less than the major semi-axes of the ellipses. For example, for Sheffield (Fig. 2) the average deviation was 4.9 m/set. This analysis shows that almost without exception the annual term predominates for all stations (Fig. 4 and Table 1). The next term in order of magnitude is the 6month component. Components of periods 4 months and 3 months are smaller and are roughly equsl in magnitude. These results hold for both NS and EW components. A number of features common to all the annual ellipses can be noted. Thus the angle vO between the major axis of the annusl ellipses and the mean annual vector tends to be about 80’ (see Table 2). Also, the magnitude of the major semi-axes of the annual ellipses are roughly the same for all stations, irrespective of time and geographic coordinates. The most noteworthy feature, however, is the time of
810
G. M. TEPTINand V. M. STARORLTN
_? .---L--Ad._
3
4
56
8 .r,
12
15
months
(4
80,000
3
4
6 8 T, months (b:
12
Fig. 3. The power speotre,of semidiurnal tides (a) amplitudes, (b) phases (oontinuous line-zonttl,dashed line-meridionalcomponentfj,Jodrell Bank).
Seasonal variations in the semi-diurnal tide in the upper &mosphere
lomlsec &xfrell Bank Sheffield Kiev
811
Kharkov
T= 12 mo”
T=L)man
T’3
man
T=l2mon
T=6mon
T-4
mon
T= 3 mon
Fig. 4. The seasonal variations of semidiurnal tides.
maximum deviation from the annual mean value. This always occurs in winter and summer, most frequently in January-July, more rarely in December-June, still more rarely in Feb~a~-Au~st. The phase difference between the NS and EW ~m~nents for the annual variation is in most eases close to 7~12. We have been unable to detect any obvious latitudinal or longitudinal vkations in the annual change. Semi-annual (&month) ellipses also tend to show at least one common feature. Thus the directions of the major semi-axes of the annual and semi-annual ellipses tend to be the same. However no other common features have been detected for the B-month, 4-month and 3-month ellipses. This may be due to the actual behaviour of the upper atmosphere, but is more probably due to insufficient accuracy in the determination of the monthly tidal parameters. These are frequently calculated on the basis of a few days data, in spite of the fact that there are known to be appreciable changes in these parameters from day to day in the course of a month. The method of analysis can be extended if data are available for a su~~iently long period. We have analysed the results of 5 year’s observations at Jodrell Bank
812
G.
M.
!FEPTIN
and V. X.
STAROSTIN
Table 1
Station
12 mon
Major semia;xis 6 mon 4 man --_
3 mon
N-S
71
8.8
4.8
3.*1
2.7
E-W
70
7.2
3.4
5.0
3.5
N-S
68
E-W
60
X-S
35
E-IV
75
K-S
51
8.0
8.1
5.6
3.8
E-W
75
9.1
6.9
4-l
5.9
N-S
63
45.2
4.6
2.2
3.8
E-W
88
7.9
5.6
5.1
4.0
N-S
88
8.5
2.7
2.8
2.9
E-W
79
4.2
5.7
6.5
l-6
N-S
74
E-W
89
N-S
75
E-W
82
N-S
64
7.7
4.6
3.1
2.0
E-W
25
5-3
4.8
2.8
4.2
N-S
31
7.4
4.4
2.1
2.7
E-?V
38
5.5
I.8
2.9
4-o
N-S
63
6-B
4.2
3.6
3.9
E-W
50
8.4
4.5
4.6
1.6
N-S
73
6.0
6.2
3.7
2.7
E-W
85
6.3
3.0
f-6
3.9
Jodrell Bank
Sheffield
Kiev
If.aarkov
1900
1962
1965
Obninsk
1964
1968
-lZ.WJ%ll
Dwhambe
Frunze
1964
1966
813
Seasonal variations in the semi-diurnal tide in the upper atmosphere Table 2 fp0
O-10
10-20
20-30
30-40
40-60
60-60
60-70
70-80
80-90
0
0
1
3
0
3
4
8
6
Number of occasions
Table 3 Number of harmonics
1
2
3
4
6
6
7
8
Period T (mon) Major N-S &&axis E-W
48 2.31 1.84
24 3.95 2.4
16 1.66 2.28
12 9.9 9.64
96 1.2 4.24
8 2.8 4.24
6.9 2.1 1.98
6 6.76 4.28
Number of hrtrmonics
9
10
11
12
13
14
16
16
Period T (mon) Major N-S Semiaxis E-W
6.3 2.3 2.8
4.8 1.8 2.06
4.36 164 4.2
4 6 6.08
3.7 1.3 3.12
3.4 2.71 6.32
3.2 1.1 1.76
3 2.26 3.2
using 16 harmonic components,
and some of the results of this analysis are given in
Table 3. Again, the annual component is found to predominate. 3. CoNCLTJsIoNs From the results of this work we may draw the following conclusions:(1) There is a clesrly defined time variation of the parameters (amplitude and phase) of the semi-diurnal tide at heights of 80-100 km. (2) The predominant variation of these parameters is annual (12-month period). (3) There are also other periodicities of tidal changes, of which the most noteworthy is semi-annual (6-month period). (4) The variations show no clear pattern as a function of latitude or longitude. (5) As far as the annual variation is concerned, the following features have been observed : (a) The greatest deviations of phase and amplitude from the annual mean occur in winter and in summer. (b) The angle between the ma,jor semi-axis of the annual ellipse and the mean annual vector tends to be close to 80’. REFERENCES ARXFEJEVA
A.V. etal. B~BOSUNOV I. B. and KAR~XOVK. A. BLACKMAN I.B.and TTJKEY I.W.
1966 1966 1968
FIALKO E. J. et al.
1969
GREENHOWJ. S. and NEUFELD E. L. GICEENEOWJ. S. and NEUFELD E. L. KASHEEV B. L., LEBEDINET~B. N. end LAQUTIN M. F. K~LEIHEEv B. L. and LYSENKO J. A. LYSENKO J. A.
1966 1961 1967 1967 1963
Geowwg.& Aeronomy 6, 4. Met. raqr. t-ad. 34, 273. The Meaaurem of Power Spectra. Dover, New York. I&&a of meteor train di+ft ob,wvations in Kiev &wing IQSY. Vestnic Kievskogo Universiteta. Phil. Trans. 48, 649. Q. J. R. met. Sot. 27, 472. Meteornye Javlenija in Atmosphere Zemly. Moskva. J. Atmosph. Tew. Phya. 80, 6. A&. Zh. 40, 1.
814
G. M. TE~TIN and V. M. STAROSTIN
LYSEN~O J. A. et al.
1969
MILLER H. G. NEUFELD E.L. POCEROVSKY G. B. and TIWTIN G. M. PUPISEEV Yu. and TE~TIN G. M. ROPER R. G. SEAMSUTDINOV SH. 0. and CHEBOT~EV R. P. SIEBERT M. TJWTIN G. M. ZODORINA E. K., POCKROVSKY G. B., SIDOROV V. V. and TE~TIN G. M.
1966 1960 1970 1971 1966 1969 1961 1969 1967
Izv. Akad. Nauk SSSR-l%. Atmos. i okeana 5, 9, 973. Planet. Space Sci. 14. Jo&e11 Bank AWL 267-273. Izv. NaukSSSR-Fiz. Atmos. d Okeana 6,2. cfeomag. & Aeronomy (In press). J. geophys. Rea. 71, 2. Bull In&. astr. AN TSSR 49, 13. Adv. Cfeophys. 7, 105 il;ew York. Met. rampr. rad. 6, 206. Izv. Akad. ?X’auk ~‘%%‘R-Piz. Atmos. Okeana 3, 1.
i
Seasoual
Terreatrhl
Phyaica, 1971,
Vol.SS,pp.807-814. Pergamon Prcua.Printed InNorthern Ire&ad
variatim in the semi-diurnal
in the upper atmomhere
tide
as determined from radio meteor observations G.
M. TE~TIN and V. M. STAROS~
Radioastronomy
Department,
State University,
Kasan,
U.S.S.R.
(Received 23 April 1970)
Ab&ac&Cormctions to the wind velocity for finite width of aerial polar diagram, and for non-uniform sensitivity of the radio meteor method to dif%rent values of velocity, have been calculated for eight stations in the northern hemisphere. The corrected wind data are used to study seasonal changes in phase and amplitude of the semi-diurnal tide in the upper atmosphere. These seasonal variations are analysed into harmonic components of periods 12, 0, 4 and 3 months; the component of period 12 months is found to have the largest amplitude. Similarities of seasonal behaviour are &dent at all eight stations. 1. INTRODUCTION
number of stations carry out systematic measurements of winds at altitudes of 80-100 km uaing radio observations of drifting meteor trails. However the results obtained with equipments of different characteristics are widely different, because of systematic errors in determining the wind. Important contributing factors are the non-uniform sensitivity of the radar method to wind velocities of different magnitudes, and the finite widths of the aerial polar diagrams. A typical characteristic of station sensitivity to wind velocity is shown in Fig. 1. The influence of the finite width of the aerial polar diagram has been discussed elsewhere. Corrections to wind velocities were carried out by the method described by TEPTIN (1969) and POPISHEV and TEPTIX (1971). Data from the following eight stations in the northern hemisphere was used: AT PRESENT
1. 2. 3. 4.
a
Jodrell Bank Shejield Kiev Kharkov
(NEUFELD,
1960; GREENHOW
(LYSENKO,
1963;
1967; KASHEEV
5.
Obninsk
and NEIJFELD, 1961).
(M&ER, 1966). (FILLLKO, 1969; LYsENK0,1969).
(KASHEEV
KASHEEV,
LEBERDINETS
and LACXJTTN,
and LYSENKO, 1967).
and LYSENKO, 1967; AREFEJEVA, 1966; LYSENKO,
1969). 6.
7. 8.
Karen Frunze Dudmnbe
(ZADORINA et
al., 1967)
(LYSENKO, 1969; BIBOSUNOV and KARIMOV, 1966). (SHAMSUTDINOV and CHEBOTAREV, 1969).
In the present paper the corrected values of semi-diurnal tidal wind velocities for the above stations are analysed. 2. RESULTS work on the Fourier analysis of the diurnal change in wind velocity have shown that for most stations the semi-diurnal component (12 hr) haa the largest amplitude, followed in magnitude by the diurnal (24 hr), which is followed in turn by the 8-hr component (e.g. ROPER, 1966; POCKROVSKY and TEPTIN,1970). The standard method of analysis (GREENHOW and NEUFELD, 1966) presents the Previous
807
G. M. TEPIXN
808
and V. M. STAROSTIN
Fig. 1. Typical characterietic of radar station sensitivity to wind velocity (Kazan, continuous line--phase-time velocity
registration,
dashed line-sector
registration).
values V observed during 1 month in the form V(t) = 7, + V, sin 15’(t + yI) + V, sin 30°(t + ya) + V, sin 45’(t
+
YJ
where V,, V2, I’, are the amplitudes and vtyl,ya, ws are the phase of the first (24 hr), second (12 hr) and third (8 hr) harmonic components, and V, is the prevailing component or monthly mean. This analysis is carried out separated for the NS nd EW components of velocity. In the present paper we consider only the semi-diurnal component. Even the earliest observations showed that the amplitude Vv, and phase ys, of this component change appreciably from month to month. Figure 2 gives typical observational results for Sheffield as a ‘harmonic dial.’ The distance of each point from the origin represents V,, and the angle (measured anticlockwise from the x axis) represents yz. The points are numbered 1-12, one for each month of the year. A question arises as to whether these changes from month to month are real, or whether they are to be ascribed to experimental errors. To investigate this point, the monthly values of amplitude of the semi-diurnal tide were analysed as a power spectrum over the range of periods 2-14 months, using data from Jodrell Bank (195358), Kharkov (1961-65) and Frunze (1964-65). As a result it became clear that the values are not random, but have a clear 12-month periodicity. The same analysis was carried out for the phase of the tidal component, and again the predominant period was 12 months. These results are illustrated for Jodrell Bank in Fig. 3. The calculations of the power spectra were carried out as described by BLAUKM and TUKEY
(1958).
The fact that the predominant period found is 12 months, suggests the use of harmonic analysis of the seasonal changes, using harmonics of periods 12, 6, 4 and 3 months. Such an analysis was carried out using the method described by SIEBERT
Seasonal variations in the semi-diurnal tide in the upper atmosphere
809
Y
2 4 mkec -
9 >
/_ x
Fig. 2. Mean month velocity values of semidiurnaltides (Sheffield,noncorrected values, N-S). (1961). Consider one component of the wind, say the NS component. The amplitude and phase of the semi-diurnd tide in this component can be represented by the sum of a constant vector and a series of ellipses which are traversed with periods of 12, 6, 4 and 3 months. The largest ellipse is, of course, the one of 12 month period, as this is the predominsnt seasonal component. A similar analysis can be carried out for the EW component. The data was corrected for non-uniform sensitivity to wind velocities and for aerial polar diagram as explained earlier. In order to confirm the validity of the harmonic expansion, the average deviations of the sums of the mean snnual value and the four harmonics from the actual experimental points were calculated. Most of the deviations only slightly exceeded the errors of individual measurements and were always considerably less than the major semi-axes of the ellipses. For example, for Sheffield (Fig. 2) the average deviation was 4.9 m/set. This analysis shows that almost without exception the annual term predominates for all stations (Fig. 4 and Table 1). The next term in order of magnitude is the 6month component. Components of periods 4 months and 3 months are smaller and are roughly equsl in magnitude. These results hold for both NS and EW components. A number of features common to all the annual ellipses can be noted. Thus the angle vO between the major axis of the annusl ellipses and the mean annual vector tends to be about 80’ (see Table 2). Also, the magnitude of the major semi-axes of the annual ellipses are roughly the same for all stations, irrespective of time and geographic coordinates. The most noteworthy feature, however, is the time of
810
G. M. TEPTINand V. M. STARORLTN
_? .---L--Ad._
3
4
56
8 .r,
12
15
months
(4
80,000
3
4
6 8 T, months (b:
12
Fig. 3. The power speotre,of semidiurnal tides (a) amplitudes, (b) phases (oontinuous line-zonttl,dashed line-meridionalcomponentfj,Jodrell Bank).
Seasonal variations in the semi-diurnal tide in the upper &mosphere
lomlsec &xfrell Bank Sheffield Kiev
811
Kharkov
T= 12 mo”
T=L)man
T’3
man
T=l2mon
T=6mon
T-4
mon
T= 3 mon
Fig. 4. The seasonal variations of semidiurnal tides.
maximum deviation from the annual mean value. This always occurs in winter and summer, most frequently in January-July, more rarely in December-June, still more rarely in Feb~a~-Au~st. The phase difference between the NS and EW ~m~nents for the annual variation is in most eases close to 7~12. We have been unable to detect any obvious latitudinal or longitudinal vkations in the annual change. Semi-annual (&month) ellipses also tend to show at least one common feature. Thus the directions of the major semi-axes of the annual and semi-annual ellipses tend to be the same. However no other common features have been detected for the B-month, 4-month and 3-month ellipses. This may be due to the actual behaviour of the upper atmosphere, but is more probably due to insufficient accuracy in the determination of the monthly tidal parameters. These are frequently calculated on the basis of a few days data, in spite of the fact that there are known to be appreciable changes in these parameters from day to day in the course of a month. The method of analysis can be extended if data are available for a su~~iently long period. We have analysed the results of 5 year’s observations at Jodrell Bank
812
G.
M.
!FEPTIN
and V. X.
STAROSTIN
Table 1
Station
12 mon
Major semia;xis 6 mon 4 man --_
3 mon
N-S
71
8.8
4.8
3.*1
2.7
E-W
70
7.2
3.4
5.0
3.5
N-S
68
E-W
60
X-S
35
E-IV
75
K-S
51
8.0
8.1
5.6
3.8
E-W
75
9.1
6.9
4-l
5.9
N-S
63
45.2
4.6
2.2
3.8
E-W
88
7.9
5.6
5.1
4.0
N-S
88
8.5
2.7
2.8
2.9
E-W
79
4.2
5.7
6.5
l-6
N-S
74
E-W
89
N-S
75
E-W
82
N-S
64
7.7
4.6
3.1
2.0
E-W
25
5-3
4.8
2.8
4.2
N-S
31
7.4
4.4
2.1
2.7
E-?V
38
5.5
I.8
2.9
4-o
N-S
63
6-B
4.2
3.6
3.9
E-W
50
8.4
4.5
4.6
1.6
N-S
73
6.0
6.2
3.7
2.7
E-W
85
6.3
3.0
f-6
3.9
Jodrell Bank
Sheffield
Kiev
If.aarkov
1900
1962
1965
Obninsk
1964
1968
-lZ.WJ%ll
Dwhambe
Frunze
1964
1966
813
Seasonal variations in the semi-diurnal tide in the upper atmosphere Table 2 fp0
O-10
10-20
20-30
30-40
40-60
60-60
60-70
70-80
80-90
0
0
1
3
0
3
4
8
6
Number of occasions
Table 3 Number of harmonics
1
2
3
4
6
6
7
8
Period T (mon) Major N-S &&axis E-W
48 2.31 1.84
24 3.95 2.4
16 1.66 2.28
12 9.9 9.64
96 1.2 4.24
8 2.8 4.24
6.9 2.1 1.98
6 6.76 4.28
Number of hrtrmonics
9
10
11
12
13
14
16
16
Period T (mon) Major N-S Semiaxis E-W
6.3 2.3 2.8
4.8 1.8 2.06
4.36 164 4.2
4 6 6.08
3.7 1.3 3.12
3.4 2.71 6.32
3.2 1.1 1.76
3 2.26 3.2
using 16 harmonic components,
and some of the results of this analysis are given in
Table 3. Again, the annual component is found to predominate. 3. CoNCLTJsIoNs From the results of this work we may draw the following conclusions:(1) There is a clesrly defined time variation of the parameters (amplitude and phase) of the semi-diurnal tide at heights of 80-100 km. (2) The predominant variation of these parameters is annual (12-month period). (3) There are also other periodicities of tidal changes, of which the most noteworthy is semi-annual (6-month period). (4) The variations show no clear pattern as a function of latitude or longitude. (5) As far as the annual variation is concerned, the following features have been observed : (a) The greatest deviations of phase and amplitude from the annual mean occur in winter and in summer. (b) The angle between the ma,jor semi-axis of the annual ellipse and the mean annual vector tends to be close to 80’. REFERENCES ARXFEJEVA
A.V. etal. B~BOSUNOV I. B. and KAR~XOVK. A. BLACKMAN I.B.and TTJKEY I.W.
1966 1966 1968
FIALKO E. J. et al.
1969
GREENHOWJ. S. and NEUFELD E. L. GICEENEOWJ. S. and NEUFELD E. L. KASHEEV B. L., LEBEDINET~B. N. end LAQUTIN M. F. K~LEIHEEv B. L. and LYSENKO J. A. LYSENKO J. A.
1966 1961 1967 1967 1963
Geowwg.& Aeronomy 6, 4. Met. raqr. t-ad. 34, 273. The Meaaurem of Power Spectra. Dover, New York. I&&a of meteor train di+ft ob,wvations in Kiev &wing IQSY. Vestnic Kievskogo Universiteta. Phil. Trans. 48, 649. Q. J. R. met. Sot. 27, 472. Meteornye Javlenija in Atmosphere Zemly. Moskva. J. Atmosph. Tew. Phya. 80, 6. A&. Zh. 40, 1.
814
G. M. TE~TIN and V. M. STAROSTIN
LYSEN~O J. A. et al.
1969
MILLER H. G. NEUFELD E.L. POCEROVSKY G. B. and TIWTIN G. M. PUPISEEV Yu. and TE~TIN G. M. ROPER R. G. SEAMSUTDINOV SH. 0. and CHEBOT~EV R. P. SIEBERT M. TJWTIN G. M. ZODORINA E. K., POCKROVSKY G. B., SIDOROV V. V. and TE~TIN G. M.
1966 1960 1970 1971 1966 1969 1961 1969 1967
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