Atoc 1050 Chapter 6

Front 1

Convection

Back 1

Vertical motions within the atmosphere caused by buoyancy. Convection results in mixing of air and transport of warm air aloft.

Front 2

Air Parcel

Back 2

A distinct blob of air that we will imagine we can identify as it
moves through the atmosphere

Front 3

Stable

Back 3

If the parcel is displaced vertically, it will return to its original
position

Front 4

Neutral

Back 4

if the parcel is displaced vertically, it will remain in its new position

Front 5

Unstable

Back 5

If the parcel is displaced vertically, it will accelerate away from its
original position in the direction of the initial displacement

Front 6

Adiabatic Process

Back 6

a process in which an air parcel does not mix with its
environment or exchange energy with its environment

Front 7

Dry Adiabatic Lapse Rate

Back 7

the rate at which an unsaturated air parcel will
cool if it rises or warm as it sinks (applies to an air parcel with a relative
humidity of less than 100%)

Dry adiabatic lapse rate = 10 deg C / km

Front 8

Lapse Rate

Back 8

The rate at which temperature decreases with increasing altitude.

Front 9

Moist Adiabatic Lapse Rate

Back 9

the rate at which a saturated air parcel will cool
if it rises or warm if it sinks (applies to an air parcel with a relative humidity
of 100%)

Moist adiabatic lapse rate = 6 deg C / km (on average in the troposphere)

Front 10

Environment

Back 10

the atmosphere outside of an air parcel

Front 11

Environmental Lapse Rate

Back 11

the rate at which the environment’s temperature
decreases with increasing altitude

Front 12

Lifting condensation level

Back 12

– the level where condensation first occurs as an
air parcel is lifted (where the relative humidity of the air parcel becomes
100%)

Front 13

Level of free convection

Back 13

the level where an air parcel first becomes
buoyant (warmer than its environment)