Lifted condensation level

Method of finding

Meteorologists determine the LCL on Tephigram, as follows:

1. Start at the initial temperature (T) and pressure of the parcel and follow upward the dry adiabatic lapse rate line if the air is not saturated. Otherwise, the parcel is already at or above LCL.
2. From the dew point temperature (Td) of the parcel, follow upward the mixing ratio line at that point.
3. At the intersection of the two lines is the LCL.

While the ideal gas law). Since the air parcel does not lose matter either, the mixing ratio of water vapor to dry air remain the same until the temperature has reached the saturation. Then condensation occurs, and if the lift continues the parcel will form cloud.

More simply, as an relative humidity is 100%.

The LCL is the level where a parcel rising dry adiabatically from the surface (the dew point depression (T-Td) results in a lower LCL. High low-level moisture content and low cloud bases are conducive to tornadogenesis. One can approximate the LCL without a sounding, using surface data, with the following formula:

h_LCL = 120 (T - Td)

where h is pressure height of LCL, T is temperature in degrees Fahrenheit, Td is dew point temperature in degrees Fahrenheit.

Relation with CCL

Without mechanical lift, cloud will form at the pressure) usually lead to a lowering of the cloud base.

A lower difference between the LCL and LFC (LCL-LFC) is conducive to thunderstorms and tornadoes. One reason for this is that a parcel requires less equilibrium level (EL). A lower LCL-LFC difference also means thunderstorms can initiate sooner, requiring less left, since they'll reach their LFC more quickly and easily.

See also

• Atmospheric thermodynamics

References

• M K Yau and R.R. Rogers, Short Course in Cloud Physics, Third Edition, published by Butterworth-Heinemann, January 1, 1989, 304 pages. EAN 9780750632157 ISBN 0-7506-3215-1