By R. M. Goody, Y. L. Yung

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**Extra info for Atmospheric Radiation: Theoretical Basis**

**Sample text**

95) yields for - 1 ^ ^ < 0 . 99) are valid for 0 =£ T ^ TI . 99) can be employed in the form given. 3), and if the source function is isotropic. Isotropy of Jv(t) enables us to perform angular integrations in terms of exponential integrals of order n (see Appendix 6), From Fig. 8, an element of solid angle is, and the angular integration runs from § = +1 to § = 0 in the positive hemisphere and £ = 0to|; = — l i n the negative hemisphere. 9) can now be written FIG. 8. Evaluation of the flux.

For atmospheric pressures between these two values, the water vapor rotation band would pose a formidable problem were it not for photochemical decomposition. A pressure of 10~3 dyne cm~2 corresponds to a level of about 150 km and few water vapor molecules exist above this level. Planck's source function is a good approximation for all levels at which water vapor is important. 5. 4 are often used in atmospheric calculations. However, the level populations n(u) and «(/) can be influenced by radiative and collisional transitions to and from other states, and involving other molecules; these possibilities were generally indicated by the level k in Fig.

4) is the transformation law for the components of the vector 18 ATMOSPHERIC RADIATION The sun's disk subtends, on the average, an angle of 32' at the earth's surface; for most practical purposes sunlight can be regarded as a parallel beam of radiation. The above definition of intensity is unnecessarily general for this case. Let us suppose that the sun's direction is that of the vector s®, and let its disk subtend a solid angle dco& at the earth. For unmodified solar radiation, IV(P, s) is only nonzero if s is very close to s©.