Thermal wind in atmospheric pressure coordinates
For a dry ideal-gas atmosphere in hydrostatic/geostrophic balance, pressure-coordinate shear satisfies ∂u_g/∂p=R_d T_y/(fp) and ∂v_g/∂p=−R_d T_x/(fp).
Key knowledge
For a dry ideal-gas atmosphere in hydrostatic/geostrophic balance, pressure-coordinate shear satisfies ∂u_g/∂p=R_d T_y/(fp) and ∂v_g/∂p=−R_d T_x/(fp). Horizontal temperature gradients here are on constant-pressure surfaces. Integrating between two pressure levels gives their geostrophic wind difference; it does not set the wind at either level by itself.
Values and equations
u_{g,p}=R_dT_y/(fp); v_{g,p}=−R_dT_x/(fp)
- u_g,v_g
- east/north geostrophic velocities m s⁻¹
- p
- pressure Pa
- T
- dry-air temperature K
- R_d
- specific gas constant of dry air J kg⁻¹ K⁻¹
- x,y
- east/north horizontal coordinates on a pressure surface m
- f
- signed Coriolis parameter s⁻¹
Conditions and scope
- p>0,f≠0,R_d is gas constant per unit dry-air mass, and horizontal coordinates are east/north. Use hydrostatic balance and nearly geostrophic flow.
- Moist-air density needs a consistent virtual-temperature/composition model. Height and pressure gradients cannot be interchanged silently; near-equatorial or strongly accelerating flow falls outside the approximation.
Sources · 1
References
Sources retain their recorded scope. A source link alone does not establish verification of every statement.
Evidence and review
Read actual pressure/height conversion and ideal-gas pressure-coordinate equations8–9. Preserved its specific-gas-constant convention and fixed-pressure gradient domain; did not universalize dry-air T to moist mixtures.
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Entry details
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- Revision
- core.1
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