Geopotential height

Geopotential is the gravitational potential energy per unit mass at elevation ${\displaystyle Z}$ :

${\displaystyle \Phi (Z)=\int _{0}^{Z}\ g(\phi ,Z)\,dZ}$ 

where ${\displaystyle g(\phi ,Z)}$  is the acceleration due to gravity, ${\displaystyle \phi }$  is latitude, and ${\displaystyle Z}$  is the geometric elevation.^[1]

Geopotential height may be obtained from normalizing geopotential by the acceleration of gravity:

${\displaystyle {H}={\frac {\Phi }{g_{0}}}\ ={\frac {1}{g_{0}}}\int _{0}^{Z}\ g(\phi ,Z)\,dZ}$ 

where ${\displaystyle g_{0}}$  = 9.80665 m/s², the standard gravity at mean sea level.^[4] Expressed in differential form,

${\displaystyle {g_{0}}\ {dH}={g}\ {dZ}}$ 

Geopotential height plays an important role in atmospheric and oceanographic studies. The differential form above may be substituted into the hydrostatic equation and ideal gas law in order to relate pressure to ambient temperature and geopotential height for measurement by barometric altimeters regardless of latitude or geometric elevation:

${\displaystyle {dP}={-g}\ {\rho }\ {dZ}={-g_{0}}\ {\rho }\ {dH}={\frac {-g_{0}\ P}{R\ T}}\ {dH}}$ 

${\displaystyle {\frac {dP}{P}}=-{\frac {g_{0}}{R\ T}}\ {dH}}$ 

where ${\displaystyle P}$  and ${\displaystyle T}$  are ambient pressure and temperature, respectively, as functions of geopotential height, and ${\displaystyle R}$  is the specific gas constant. For the subsequent definite integral, the simplification obtained by assuming a constant value of gravitational acceleration is the sole reason for defining the geopotential altitude.^[5]

 

Geophysical sciences such as meteorology often prefer to express the horizontal pressure gradient force as the gradient of geopotential along a constant-pressure surface, because then it has the properties of a conservative force. For example, the primitive equations that weather forecast models solve use hydrostatic pressure as a vertical coordinate, and express the slopes of those pressure surfaces in terms of geopotential height.

A plot of geopotential height for a single pressure level in the atmosphere shows the troughs and ridges (highs and lows) which are typically seen on upper air charts. The geopotential thickness between pressure levels – difference of the 850 hPa and 1000 hPa geopotential heights for example – is proportional to mean virtual temperature in that layer. Geopotential height contours can be used to calculate the geostrophic wind, which is faster where the contours are more closely spaced and tangential to the geopotential height contours.^{[citation needed]}

The United States National Weather Service defines geopotential height as:

"...roughly the height above sea level of a pressure level. For example, if a station reports that the 500 mb [i.e. millibar] height at its location is 5600 m, it means that the level of the atmosphere over that station at which the atmospheric pressure is 500 mb is 5600 meters above sea level. This is an estimated height based on temperature and pressure data."^[6]

• Atmospheric model
• Above mean sea level
• Dynamic height, a similar quantity used in geodesy, based on a slightly different gravity value

• Hofmann-Wellenhof, B. and Moritz, H. "Physical Geodesy", 2005. ISBN 3-211-23584-1.
• Eskinazi, S. "Fluid Mechanics and Thermodynamics of our Environment", 1975. ISBN 0-12-242540-5.

•   Media related to Geopotential height at Wikimedia Commons