Determination of Parameters of the Atmosphere and the Surface in a Clear Atmosphere - Short-Wave Solar Radiation in the Earth's Atmosphere - page 197

Fig. 5.9a,b. Results of the retrieval of the spectral dependence of the volume coefficients of
the aerosol scattering ( upper curves )andabsorption( lower curves )atthealtitudelevels
corresponding to atmospheric pressure 850 mbar: a from the data of the airborne sounding
16th October 1983 above the Kara-Kum Desert, b from the data of the airborne sounding
29th April 1985 above Ladoga Lake. Dashed lines indicate the relevant profiles of the a priori
models. ( Middle curve in Fig. 5.9a) - The aerosol absorption volume coefficient from the
airborne sounding 12th October 1983 under sand storm conditions
The irregular, indent shape of the vertical profiles was obtained in the
other studies (for example Krekov and Zvenigiriodsky 1990; Polyakov et al.
2001) from the remote sounding processing and it was also obtained from
the airborne direct measurements of the aerosols particle concentrations even
after the statistical smoothing over a big volume of data (Hudson andYonghong
1999). Thus, the retrieved serrated profiles of the optical parameters of the
atmospheric aerosols are not to be explained as an effect of only systematic
errors of the calibration and altitudinal conjunction, and they are likely to
reflecttherealprofileoftheaerosolcontentintheatmosphere.Thealtitudesof
the most probable formation of cloudiness correspond to the local maximums
in curves of Fig. 5.8 (Hudson andYonghong 1999). As is well known, the process
of the cloudiness formation is connected with the presence of atmospheric
aerosols as they serve the condensation nuclei.
In particular, the local maximum of the volume coefficients of the aerosol
scattering and absorption at altitude 1900m (corresponding to 800mbar)is