Inertia–gravity waves and deformation radius
Linearizing a uniform-depth rotating shallow-water layer at rest on an f-plane yields propagating roots ω²=f²+gH(k_x²+k_y²) and a balanced zero-frequency mode.
Key knowledge
Linearizing a uniform-depth rotating shallow-water layer at rest on an f-plane yields propagating roots ω²=f²+gH(k_x²+k_y²) and a balanced zero-frequency mode. The nonrotating long-wave speed is c=√(gH), and the rotational deformation length is L_d=c/|f|. Rotation and gravity therefore control different time and length limits of the same model.
Values and equations
ω²=f²+gH(k_x²+k_y²); c=√(gH); L_d=c/|f|
- ω,f
- wave angular frequency and Coriolis parameter s⁻¹
- g
- stated gravity or separately specified reduced gravity m s⁻²
- H,L_d
- reference layer thickness and deformation length m
- k_x,k_y
- horizontal angular wavenumbers m⁻¹
- c
- nonrotating hydrostatic wave speed m s⁻¹
Conditions and scope
- Small perturbations about positive constant H,constant f,flat bottom,inviscid hydrostatic single layer; use a specified reduced gravity g′ instead of g for the corresponding active-layer model.
- f≠0 for a finite deformation-radius expression. Wave phase/group velocities differ from parcel transport; short waves outside hydrostatic depth averaging and variable stratification need fuller dispersion relations.
Sources · 1
References
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Evidence and review
Read actual§4.1 determinant and roots equations59–62 and§4.2 deformation scale66–68, plus source long-wave limit. Translated reduced gravity to the explicitly stated free-surface limit, kept the zero-frequency root and |f| for a positive length.
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Entry details
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- uni-earth-inertia-gravity-waves
- Revision
- core.1
- Structured reference record
- University core expansion