By Alexander A. Kokhanovsky
In Aerosol Optics, Alexander Kokhanovsky presents a accomplished evaluation of obtainable recommendations for the distant sensing of aerosols. even if generally satellite tv for pc distant sensing is taken into account, ground-based ideas also are mentioned. The paintings is based at the sturdy foundation of radiative move idea, coupled with Maxwell conception for the calculation of the scattering houses of small debris. particularly, the writer describes innovations for the choice of the column focus of aerosol debris and their optical sizing utilizing spaceborne optical instrumentation. nearly all of the ideas defined during this ebook use a so-called "library method". this technique depends the precalculated top-of-atmosphere reflectances (TOAR) for vaious atmospheric aerosol forms. The comparability of measured and calculated TOARS permits one to symbolize the optically-equivalent aerosol state.
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Additional resources for Aerosol Optics: Light Absorption and Scattering by Particles in the Atmosphere
1), valid as x ! 1 and vx ! 1. Oscillations seen in Fig. 5 around the size parameter 10 are due to interference effects. They damp down at x ¼ 20 because in this case the attenuation of the electromagnetic waves on the diameter of a particle cannot be neglected for the range of v shown in Fig. 5. Generally, the absorption increases with the refractive index. 1). This leads to the decrease of the portion of energy, which can penetrate into particles and be absorbed 30 2 Optical properties of atmospheric aerosol Fig.
We will assume that the aerosol layer is situated in vacuum over a black underlying surface. This means that the diffuse light has no chance to enter the top of the layer ðs ¼ 0Þ from above and the bottom of the layer ðs ¼ s0 Þ from below. Therefore, boundary conditions can be presented in the following form: p I ð0; W; W0 ; uÞ ¼ 0 at W < ; 2 p I ðs0 ; W; W0 ; uÞ ¼ 0 at W > : 2 The differential equation for the diffuse intensity given above can be solved analytically. The answer is: eÀs=g I ðs; g; n; fÞ ¼ g Zs 0 Bðs0 ; g; n; fÞ es =g ds0 at g > 0 0 for the downward intensity and es=g I ðs; g; n; fÞ ¼ g Zs 0 Bðs0 ; g; n; fÞ es =g ds0 at g < 0; s0 for the upward intensity, where we accounted for boundary conditions and g ¼ cos W; n ¼ cos W0 .
The same as in Fig. 10 except for f34 . close to the oceanic aerosol model. Also it follows that the behavior of scattering matrix elements differs for continental and maritime aerosol considerably (especially, in the backward hemisphere). This can be used, for example, for the identification of the aerosol type. It follows from Fig. 15(b) that the degree of circular polarization vanishes, for example, at 175 degrees for maritime aerosol. This, however, does not mean that the light becomes completely unpolarized.