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This '''Barotropic vorticity equation''' assumes the atmosphere is nearly barotropic, which means that the direction and speed of the [[geostrophic wind]] are independent of height. In other words, there is no vertical [[wind shear]] of the geostrophic wind. It also implies that thickness contours (a proxy for temperature) are parallel to upper level height contours. In this type of atmosphere, high and low pressure areas are centers of warm and cold temperature anomalies. Warm-core highs (such as the [[subtropical ridge]] and Bermuda-Azores high) and [[cold-core low]]s have strengthening winds with height, with the reverse true for cold-core highs (shallow arctic highs) and warm-core lows (such as [[tropical cyclone]]s).<ref>{{cite book|title=Atmospheric Science: An Introductory Survey|author=Wallace, John M. and Peter V. Hobbs|year=1977|isbn=0-12-732950-1|publisher=Academic Press, Inc.|pages=384–385}}</ref> | |||
A simplified form of the [[vorticity equation]] for an inviscid, [[divergence]]-free flow ([[Solenoidal vector field|solenoidal]] velocity field), the '''barotropic vorticity equation''' can simply be stated as<ref>{{cite book | |||
| title = An Introduction to Global Spectral Modeling | |||
| author1 = T. N. Krishnamurti | |||
| author2 = H. S. Bedi | |||
| author3 = V. M. Hardiker | |||
| author4 = L. Ramaswamy | |||
| edition = 2 | |||
| publisher = Birkhäuser | |||
| year = 2006 | |||
| isbn = 978-0-387-30254-6 | |||
}}</ref> | |||
:<math>\frac{D \eta}{D t} = 0,</math> | |||
where <math>\frac{D}{D t}</math> is the [[material derivative]] and | |||
:<math>\eta = \zeta + f</math> | |||
is ''absolute [[vorticity]]'', with <math>\zeta</math> being ''relative vorticity'', defined as the vertical component of the curl of the fluid | |||
velocity and ''f'' is the ''[[Coriolis parameter]]'' | |||
:<math>f = 2 \Omega \sin \phi,</math> | |||
where <math>\Omega</math> is the [[angular frequency]] of the planet's | |||
rotation (<math>\Omega</math>=0.7272*10<sup>−4</sup> s<sup>−1</sup> for the earth) and <math>\phi</math> is [[latitude]]. | |||
In terms of ''relative vorticity'', the equation can be rewritten as | |||
:<math>\frac{D \zeta}{D t} = -v \beta,</math> | |||
where <math>\beta = \partial f / \partial y</math> is the variation of the ''Coriolis parameter'' with distance <math>y</math> in the north-south direction | |||
and <math>v</math> is the component of velocity in this direction. | |||
In 1950, Charney, Fjørtoft, and von Neumann integrated this equation (with an added [[diffusion]] term on the [[Left-hand side and right-hand side of an equation|RHS]]) on a [[computer]] for the first time, using an observed field of 500 [[pascal (unit)|hPa]] [[geopotential height]] for the first timestep.{{fact|date=December 2013}} This was one of the first successful instances of [[numerical weather prediction]]. | |||
==See also== | |||
*[[Barotropic]] | |||
==References== | |||
{{reflist}} | |||
== External links == | |||
* http://www.met.reading.ac.uk/~ross/Science/BarVor.html | |||
[[Category:Equations of fluid dynamics]] | |||
{{Geophysics-stub}} | |||
Revision as of 16:43, 14 January 2014
This Barotropic vorticity equation assumes the atmosphere is nearly barotropic, which means that the direction and speed of the geostrophic wind are independent of height. In other words, there is no vertical wind shear of the geostrophic wind. It also implies that thickness contours (a proxy for temperature) are parallel to upper level height contours. In this type of atmosphere, high and low pressure areas are centers of warm and cold temperature anomalies. Warm-core highs (such as the subtropical ridge and Bermuda-Azores high) and cold-core lows have strengthening winds with height, with the reverse true for cold-core highs (shallow arctic highs) and warm-core lows (such as tropical cyclones).[1]
A simplified form of the vorticity equation for an inviscid, divergence-free flow (solenoidal velocity field), the barotropic vorticity equation can simply be stated as[2]
where is the material derivative and
is absolute vorticity, with being relative vorticity, defined as the vertical component of the curl of the fluid velocity and f is the Coriolis parameter
where is the angular frequency of the planet's rotation (=0.7272*10−4 s−1 for the earth) and is latitude.
In terms of relative vorticity, the equation can be rewritten as
where is the variation of the Coriolis parameter with distance in the north-south direction and is the component of velocity in this direction.
In 1950, Charney, Fjørtoft, and von Neumann integrated this equation (with an added diffusion term on the RHS) on a computer for the first time, using an observed field of 500 hPa geopotential height for the first timestep.Template:Fact This was one of the first successful instances of numerical weather prediction.
See also
References
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