2.2 The Atmosphere’s Pressure Structure: Hydrostatic Equilibrium

2.2 The Atmosphere’s Pressure Structure: Hydrostatic Equilibrium

The atmosphere’s vertical pressure structure plays a critical role in weather and climate. We all know that pressure decreases with height, but do you know why?

The atmosphere’s basic pressure structure is determined by the hydrostatic balance of forces(link is external). To a good approximation, every air parcel is acted on by three forces that are in balance, leading to no net force. Since they are in balance for any air parcel, the air can be assumed to be static or moving at a constant velocity.

There are 3 forces that determine hydrostatic balance:

1. One force is downwards (negative) onto the top of the cuboid from the pressure, p, of the fluid above it. It is, from the definition of pressure(link is external),

   $$F_{top}=-p_{top}A$$

   [2.11]
2. Similarly, the force on the volume element from the pressure of the fluid below pushing upwards (positive) is:

   $$F_{bottom}=p_{bottom}A$$

   [2.12]
3. Finally, the weight(link is external) of the volume element causes a force downwards. If the density(link is external) is ρ, the volume is V, which is simply the horizontal area A times the vertical height, Δz, and g the standard gravity(link is external), then: 

   $$F_{weight}=-\rho Vg=-\rho gA\Delta z$$

   [2.13]

By balancing these forces, the total force on the fluid is:

This sum equals zero if the air's velocity is constant or zero. Dividing by A,

or:

P_top − P_bottom is a change in pressure, and Δz is the height of the volume element – a change in the distance above the ground. By saying these changes are infinitesimally(link is external) small, the equation can be written in differential(link is external) form, where dp is top pressure minus bottom pressure just as dz is top altitude minus bottom altitude.

The result is the equation:

This equation is called the Hydrostatic Equation. See the video below (1:18) for further explanation:

Using the Ideal Gas Law, we can replace ρ and get the equation for dry air:

We could integrate both sides to get the altitude dependence of p, but we can only do that if T is constant with height. It is not, but it does not vary by more than about ±20%. So, doing the integral,

$$p= p_o{e}^{-\raisebox{1ex}{$z$}\!\left/ \!\raisebox{-1ex}{$H$}\right.} where p_o=surface pressure and H= \frac{R^{*}\overline{T}}{M_{air}g}$$

H is called a scale height because when z = H, we have p = p_oe^–1. If we use an average T of 250 K, with M_air = 0.029 kg mol^–1, then H = 7.3 km. The pressure at this height is about 360 hPa, close to the 300 mb surface that you have seen on the weather maps. Of course the forces are not always in hydrostatic balance and the pressure depends on temperature, thus the pressure changes from one location to another on a constant height surface.

From equation 2.20, the atmospheric pressure falls off exponentially with height at a rate given by the scale height. Thus, for every 7 km increase in altitude, the pressure drops by about 2/3. At 40 km, the pressure is only a few tenths of a percent of the surface pressure. Similarly, the concentration of molecules is only a few tenths of a percent, and since molecules scatter sunlight, you can see in the picture below that the scattering is much greater near Earth's surface than it is high in the atmosphere.