By Alexander A. Kokhanovsky
In Aerosol Optics, Alexander Kokhanovsky offers a complete evaluate of obtainable concepts for the distant sensing of aerosols. even supposing as a rule satellite tv for pc distant sensing is taken into account, ground-based options also are mentioned. The paintings is based at the stable foundation of radiative move conception, coupled with Maxwell thought for the calculation of the scattering houses of small debris. specifically, the writer describes thoughts for the decision of the column focus of aerosol debris and their optical sizing utilizing spaceborne optical instrumentation. the vast majority of the options defined during this publication use a so-called "library method". this system depends the precalculated top-of-atmosphere reflectances (TOAR) for vaious atmospheric aerosol varieties. The comparability of measured and calculated TOARS permits one to represent the optically-equivalent aerosol state.
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Extra resources for Aerosol Optics: Light Absorption and Scattering by Particles in the Atmosphere
2006) gave the following parameterization of the asymmetry parameter with respect to b: g ¼ 0:9893 À 7:143889b3 þ 7:464439b2 À 3:96356b: This expression was derived for the special case of the Henyey–Greenstein (HG) phase function given as pð hÞ ¼ 1 X ð2j þ 1Þgj Pj ðcos hÞ j¼0 or in the closed form: pð hÞ ¼ 1 À g2 ð1 þ g2 À 2g cos hÞ3=2 : Here Pj ðcos hÞ is the Legendre polynomial. 6 for g in the case of atmospheric aerosol. The HG phase function or linear combinations of these functions with different values of the asymmetry parameter g are used frequently for studies of radiative propagation in the aerosol media.
These equations allow for the following physical interpretation. Let us assume for the simplicity that g ¼ 1. Then it follows: Zs0 I# ðs0 ; g; n; fÞ ¼ Bðs0; g; n; fÞ expðÀðs0 À s0 ÞÞ ds0 : 0 Taking into account that the difference Ds ¼ s0 À s0 is equal to the optical thickness from the bottom of the layer to the level with the optical vertical coordinate s0 , we conclude that the diffuse light intensity of the downward propagated light is determined by the summation of source functions Bðs0; g; n; fÞ at levels s ¼ s0 weighted by the exponential attenuation factors expðÀDsÞ describing the attenuation of light from the level s ¼ s0 to the lower boundary of an aerosol layer.
22 at 440 nm for biomass burning events in Zambia. 07 for Cape Verde at the same wavelength. 02 at remote clean marine environments (Hawai, 1995–2000). The main absorbing component of the atmospheric aerosol in the visible is soot. Therefore, locations with small fractions of soot in atmospheric air are characterized by smaller light absorption levels. Polarimetric techniques use an approach similar to that just described. , 1998; Kokhanovsky, 2003). The technique is highly sensitive to the refractive index of atmospheric aerosol.