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B
a)
O
2
H
2
O
3
O
2
H
2
H
2
H
2
O
3
O
2
O
2
H
2
H
2
O
3
O
3
O
2
Fig. 3.14a,b.
Examples of typical values of the radiative flux divergences in the atmospheric
layer 1000-500 mbar;
a
above the Kara-Kum Desert, the airborne sounding 16th October
1983, solar zenith incident angle 51
◦
, sand surface;
b
aboveLadogaLake,theairborne
sounding 29th April 1985, solar zenith incident angle 48
◦
, snow surface. There are three
curves in every plot, average values and ranges of the 1SD interval
specified in Fig. 3.14. These results completely agree with values obtained
before (Kondratyev and Ter-Markaryants 1976; Vasilyev O et al. 1987).
It is important to mention that the clearer the atmosphere the less the
radiative flux divergence and the more complicated is satisfying the conditions
of its non-negativity. A large number of non-informative points in the spectrum
of the sounding above Ladoga Lake is the usual situation. The best data are the
sounding results presented in the article by Vasilyev O et al. (1987). It can be
thought that the certain transformation of the molecular absorption bands in
thespectrumofthesoundingaboveLadogaLake(Fig.3.14b)iscausedbythe
same reasons.
The non-selective part (the constant level) in the irradiance spectra is to
be attributed to the aerosol absorption essentially varying in the atmosphere.
Aerosol absorption above the desert is about an order of magnitude higher
than absorption above the water surface. In addition, it is possible to trace
the specific features of aerosol absorption in the spectral dependence of the
radiative flux divergences above the desert. Figure 3.15 illustrates the radiative
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