The Earth receives radiant energy from the sun and emits infrared radiation also termed longwave or terrestrial radiation, outward in all directions into space. To have stable conditions, there must be a balance between the net absorbed solar radiation and net outgoing terrestrial radiation. At the surface, an energy balance exists due to the additional transfers of sensible and latent heat to the atmosphere (Barry & Chorley 2003). The albedo or reflectivity of sunlight from the Earth’s surface is indicative of and related to, the absorption of radiation by that surface. A surface with a high visible brightness is heated much less than one with a low visible brightness. 
There are 342 Wm-2 of solar radiation occurrence at the top of the atmosphere annually. Of this, 77 Wm-2 (22.5%) are reflected by the atmosphere, as in gasses, clouds and aerosols, and 30 Wm-2 (8.85%) are reflected by the surface. This gives a total of 107 Wm-2 (31.3%) reflected back into space, and 235 Wm-2 net solar radiations absorbed by Earth. The rate at which the surface temperature changes from absorption of solar radiation depends on solar intensity, the surface and atmospheric reflectivity, the atmospheric absorption of solar radiation and the layer depth of the ocean.
The difference between the quantity of radiation received and lost by a surface at any place determines the net radiation that remains at that surface. It can be calculated by using the following formula:
342 Wm-2 = 107 Wm-2 + 235 Wm-2
Rn = Rs – Rs(a) – RL(t) + RL(c)
where Rn is net radiation, Rs is incoming solar radiation, a is the albedo, RL(t) is outgoing terrestrial radiation, and RL(c) is the counter radiation.
Globus Green 