. Collected reprints / Atlantic Oceanographic and Meteorological Laboratories [and] Pacific Oceanographic Laboratories. Oceanography 110 GEORGE A. MAUL AND HOWARD R. GORDON. f = f = .05 500 550 600 WAVELENGTH (nm) as f«o 700 FIG. 8. Theoretical spectra computed for three fractions of the sea surface covered with white caps, foam, or specular reflectors. Solid line uses the ratio of particle scattering to water only scattering of 128; dashed line uses 32 for the ratio. Yellow substance absorption coefficients used were and for the solid and dashed lines, respectivel
. Collected reprints / Atlantic Oceanographic and Meteorological Laboratories [and] Pacific Oceanographic Laboratories. Oceanography 110 GEORGE A. MAUL AND HOWARD R. GORDON. f = f = .05 500 550 600 WAVELENGTH (nm) as f«o 700 FIG. 8. Theoretical spectra computed for three fractions of the sea surface covered with white caps, foam, or specular reflectors. Solid line uses the ratio of particle scattering to water only scattering of 128; dashed line uses 32 for the ratio. Yellow substance absorption coefficients used were and for the solid and dashed lines, respectively. This represents summer (low solar zenith angle) conditions at the latitude of the Gulf of Mexico. strongly dependent on wavelength, Sau- berer and Ruttner (1941) have shown that for zenith angles less than 40°, p is essentially nondispersive. Therefore, Anderson's (1954) value of p = is adopted for zenith angles <40°, and it is assumed constant for the 400-700 nm interval of interest. The upwelling irradi- ance from the ocean above the sea surface (//(0,+)) is the sum of the diffuse component from beneath the surface (R(jH(0,-)), and the surface component (pH(0,-)). Cox and Munk (1954) have shown that for solar zenith angles less than 70°, FresnePs law is valid in a Beaufort 4 wind (~8 m sec-1). As white caps and foam cover larger areas of the sea sur- face, however, p will be altered because these features are approximately Lam- bertian, nondispersive, and have an albedo of 1. Thus, they contribute uni- form irradiance above the surface (/• H(0,-)) where, as before,/is the fraction of the sea covered by these diffuse reflectors. Therefore //(0,+) =RdH(0r) + WW) +f)H(0r). 06) The computed spectrum of upwelling irradiance for solar zenith angles less than 40° as a function of / is given in 504. Please note that these images are extracted from scanned page images that may have been digitally enhanced for readability - coloration and appearance of these illustrat
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