The albedo depends upon spectral band, snow thickness, ice thickness and surface temperature. Snow and ice spectral albedos (visible , wavelengths and near-infrared , wavelengths ) are distinguished, as both snow and ice spectral reflectivities are significantly higher in the band than in the band. This two-band separation represents the basic spectral dependence. The near-infrared spectral structure, with generally decreasing reflectivity with increasing wavelength  is ignored. The zenith angle dependence of snow and ice is ignored [63,56], and hence there is no distinction between downwelling direct and diffuse shortwave radiation. The approximations made for the albedo are further described by Briegleb et al. .
Here we ignore the dependence of snow albedo on age, but retain the melting/non-melting distinction and thickness dependence. Dry snow spectral albedos are:
For bare non-melting sea ice thicker than 0.5 m, as is the case for all sea ice prescribed in CAM 3.0, the albedos are
The horizontal fraction of surface covered with snow is assumed to be