The Earth's atmosphere is an extremely thin sheet of air extending from the surface of the Earth to the edge of space. If the Earth were the size of a basketball, a tightly held pillowcase would represent the thickness of the atmosphere. Gravity holds the atmosphere to the Earth's surface. And within the atmosphere, very complex chemical, thermodynamic, and fluid dynamics effects occur. The atmosphere is not uniform; fluid properties are constantly changing with time and place. (We call this change the weather.)

These variations extend upward from the surface of the Earth. The sun heats the surface of the Earth, and some of this heat goes into heating the air near the surface. The heated air is then diffused or convected up through the atmosphere. Thus the air temperature will be highest near the surface and decreases as altitude increases. The speed of sound depends on the temperature and also decreases with increasing altitude. The pressure of the air can be related to the weight of the air over a given location. As we increase altitude through the atmosphere, there will be some air below us and some air above us. But there will always be less air above us than was present at a lower altitude. Therefore, air pressure decreases as we increase altitude. The air density depends on both the temperature and the pressure through the equation of state and also decreases with increasing altitude.

Aerodynamic forces directly depend on
the air density. To help aircraft designers, it is useful to define a
**standard atmosphere **model. (There are actually many different
models available--a standard or average day, a hot day, a cold day, a
tropical day. And the models are updated every few years to include
the latest atmospheric data.) The model was developed from
atmospheric measurements that were averaged and curve fit to produce
the given equations. The model assumes that the pressure and
temperature change only with altitude. The particular model given
here was developed in the early sixties, and the curve fits are given
for Metric units. These curve fits are also available in English
units. The model has three parts.

The first part covers the lower atmosphere, called the troposphere, which extends from the surface to 11,000 meters. In this layer temperature decreases with altitude:

Temperature: T = 15.04 - .00649 * h

Pressure: p = 101.29 * [(T + 273.1) / 288.08] ^ 5.256

The second part covers the middle atmosphere, called the lower statosphere, which extends from 11,000 meters to 25,000 meters. In this layer the temperature is constant:

Temperature: T = -56.46

Pressure: p = 22.65 * exp (1.73 - .000157 * h)

The third part covers the upper atmosphere, called the upper statosphere, which extends upwards from 25,000 meters. In this layer the temperature increases with altitude:

Temperature: T = -131.21 + .00299 * h

Pressure: p = 2.488 * [(T + 273.1) / 216.6] ^ -11.388

In each part, the pressure and temperature are curve fit; and the density is derived from the equation of state. r = p / (.2869 * [T + 273.1]) This is the model used in the FoilSim and EngineSim programs.

An interactive Java applet for this slide is also available. With the applet, you can change altitude and see the effects on pressure and temperature.

Navigation...

- Beginner's Guide to Aerodynamics
- Beginner's Guide to Propulsion
- Beginner's Guide to Model Rockets
- Beginner's Guide to Kites
- Beginner's Guide to Aeronautics

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- Beginner's Guide Home Page

*byTom
Benson
Please send suggestions/corrections to: benson@grc.nasa.gov *