Adiabatic Temperature Change and Stability

Adiabatic Temperature Change and Stability 

In “The Atmosphere” we discovered that air temperature usually decreases with an increase in elevation through the troposphere. The decrease in temperature with elevation is called the environmental lapse rate of temperature or normal lapse rate of temperature. Recall that the normal lapse rate of temperature is the average lapse rate of temperature of .65o C / 100 meters. The environmental lapse rate of temperature is the actual vertical change in temperature on any given day and can be greater or less than .65o C / 100 meters. Also recall that the decrease in temperature with height is caused by increasing distance from the source of energy that heats the air, the Earth’s surface. Air is warmer near the surface because it’s closer to its source of heat. The further away from the surface, the cooler the air will be. It’s like standing next to a fire, the closer you are the warmer you’ll feel. Temperature change caused by an exchange of heat between two bodies is called diabatic temperature change. There is another very important way to change the temperature of air called adiabatic temperature change. 

 

 

Adiabatic temperature change of air occurs without the addition or removal of energy. That is, there is no exchange of heat with the surrounding environment to cause the cooling or heating of the air. The temperature change is due to work done on a parcel of air by the external environment, or work done by a parcel of air on the air that surrounds it. What kind of work can be done? The work that is done is the expansion or compression of air. 

Imagine an isolated parcel of air that is moving vertically through the troposphere. We know that air pressure decreases with increasing elevation. As the parcel of air moves upward the pressure exerted on the parcel decreases and the parcel expands in volume as a result. In order to expand (i.e.. do work), the parcel must use its internal energy to do so. As the air expands, the molecules spread out and ultimately collide less with one another. The work of expansion causes the air’s temperature to decrease. You might have had personal experience with this kind of cooling if you’ve let the air out of an automobile or bicycle tire. Air inside the tire is under a great deal of pressure, and as it rushes outside it moves into a lower pressure environment. In so doing, the parcel quickly expands against the outside environment air. By placing your hand in front of the valve stem, you can feel the air cool as it expands. This is called adiabatic cooling. 

As air descends through the troposphere it experiences increasing atmospheric pressure. This causes the parcel volume to decrease in size, squeezing the air molecules closer together. In this case, work is being done on the parcel. As the volume shrinks, air molecules bounce off one another more often ricocheting with greater speed. The increase in molecular movement causes an increase in the temperature of the parcel. This process is referred to as adiabatic warming. 

The rate at which air cools or warms depends on the moisture status of the air. If the air is dry, the rate of temperature change is 1oC/100 meters and is called the dry adiabatic rate (DAR). If the air is saturated, the rate of temperature change is .6oC/100 meters and is called the saturated adiabatic rate (SAR). The DAR is a constant value, that is, it’s always 1oC/100 meters. The SAR varies somewhat with how much moisture is in the air, but we’ll assume it to be a constant value here. The reason for the difference in the two rates is due to the liberation of latent heat as a result of condensation. As saturated air rises and cools, condensation takes place. Recall that as water vapor condenses, latent heat is released. This heat is transferred into the other molecules of air inside the parcel causing a reduction in the rate of cooling. 

Source: 
(http://www.uwsp.edu/geO/faculty/ritter/geog101/textbook/atmospheric_moisture/lapse_rates_1.html)

 

Stability of Air 

Adiabatic temperature change is an important factor in determining the stability of the air. We can think of air stability as the tendency for air to rise or fall through the atmosphere under its own “power”. Stable air has a tendency to resist movement. On the other hand, unstable air will easily rise. What gives air “power” to rise? The tendency for air to rise or fall depends on the adiabatic and environmental lapse rates. 

Stable atmospheric conditions prevail when the environmental lapse rate is less than the saturated adiabatic rate. 

Air is unstable when the environmental lapse rate is greater than the dry adiabatic rate. Under these conditions, a rising parcel of air is warmer and less dense than the air surrounding it at any given elevation. 

Source: 
(http://www.uwsp.edu/geO/faculty/ritter/geog101/textbook/atmospheric_moisture/lapse_rates_2.html)

 

 

Conditional Instability 

If you cause dry air to rise, its temperature will drop due to adiabatic expansion. This vertical temperature gradient is called the dry adiabatic lapse rate. When the temperature gradient becomes sharper than this (i.e. the temperature drops sharply as altitude increases), the atmosphere becomes unstable. 

On the other hand, if you cause air saturated with water vapor to rise as the temperature falls the water vapor condenses and lets off heat, so the temperature gradient becomes smaller. This is called the moist adiabatic lapse rate. 

In other words, saturated air becomes unstable under a smaller temperature gradient than dry air. Conditions with a vertical temperature distribution under which both dry and saturated air are stable are called absolutely stable, and conditions that cause instability for both dry and saturated air are called absolutely unstable, and conditions that cause instability in saturated air but not dry air are called conditionally unstable. 

The lower layer of the atmosphere is in a state of conditional instability, so when water vapor reaches saturation point, it becomes unstable, and cumulus and cumulonimbus occur. 

Source: 
(http://www.gfd-dennou.org/library/gfd_exp/exp_e/glossary/ci1.htm) 

 

Conditional Instability: 

Any layer in the atmosphere where the rate of actual temperature decrease with height is between the moist and dry adiabatic lapse rate. The air is unstable if saturated but stable if unsaturated. Saturated air cools less with height due to latent heat release thus allowing the parcel to be warmer than the environment if lifting occurs in a conditionally unstable environment. 

Source: 
(http://www.theweatherprediction.com/habyhints/45/)