As the air descends on the leeward side, it is warmed by adiabatic compression at the dry adiabatic lapse rate.
2.
The lapse rate, dry adiabatic lapse rate ( DALR ) and moist adiabatic lapse rate ( MALR ), are obtained.
3.
The difference between the dry adiabatic lapse rate and the rate at which the dew point drops is around per 1, 000 m.
4.
The dry adiabatic lapse rate ( for unsaturated air ) is 3 �C ( 5.4 �F ) per 1, 000 vertical feet.
5.
The temperature decreases with the dry adiabatic lapse rate, until it hits the dew point, where water vapor in the air begins to condense.
6.
This decrease is constant for Earth's atmosphere, and is approximately per kilometer ( 0.62 miles ); this is known as the dry adiabatic lapse rate.
7.
The climate becomes colder at high elevations this characteristic is described by the dry adiabatic lapse rate is 10 �C per km ( 5.5 �F per 1000 ft ) of elevation or altitude.
8.
Once the CCL is determined, the surface temperature necessary to raise a mass of air to that height can be found by using the Dry Adiabatic Lapse Rate ( DALR ) to determine the potential temperature.
9.
The dry adiabatic lapse rate accounts for the effect of the expansion of dry air as it rises in the atmosphere and wet adiabatic lapse rates includes the effect of the condensation of water vapor on the lapse rate.
10.
In the Himalayas, the rate at which an air mass's temperature falls per kilometre ( 3, 281 ft ) of altitude gained ( the dry adiabatic lapse rate ) is 9.8 �C / km.
