Lecture #5: Concepts of
Atmospheric Stability;
Vertical Structure of the Atmosphere
Monday, 29 January 2001
Text Reading for Lecture #5
Basic concepts of stability (first 5 paragraphs on page 160)
A stable atmosphere
(from Texas A&M)
An unstable atmosphere
(from Texas A&M)
Vertical structure of the atmosphere (pages 8-14)
The tropopause is clearly evident in this photograph
of a thunderstorm. Note
how the anvil spreads out horizontally as it encounters the tropopause, and
also note the overshooting top as the strong storm updraft penetrates into
the stable layer of the stratosphere.
Hand-Written Lecture Notes from Class
Page 1, Page 2, Page 3, Page 4, Page 5, Page 6, Page 7, Page 8
An Interesting Factoid (from Kelvin's newspaper column)
Oklahomans know from experience that high air temperatures make one feel
hot. You may be surprised to learn that in some parts of the atmosphere, just the
opposite is true.
At altitudes above 100 miles, air temperatures can exceed 1000 degrees Fahrenheit.
However, a thermometer shielded from direct sunlight would indicate an extremely low
temperature, around minus 400 degrees Fahrenheit, and thus a person in a shaded area would
quickly freeze to death. This paradox lies in the fact that air temperature is
related not only to the speed of air molecules, but also the number of molecules present.
At high altitudes, air molecules absorb energetic solar rays and thus move at very high
speeds. When they strike an object, say a person, they transfer some of their energy
to increase the skin temperature and provide a sensation of warmth. However, the
thin air at high altitudes contains so few air molecules that virtually no energy is
transferred. Thus, the relationship between air temperature and feeling warm is no
longer meaningful.