The interior equation materially conserves three-dimensional quasi-geostrophic potential vorticity. At each rigid horizontal boundary, is proportional to the boundary buoyancy anomaly, so the other two equations express material conservation of that buoyancy.
A background streamfunction gives . Its interior PV is uniform. Writing and retaining first-order terms gives
in the interior. Since , perturbation advection of the boundary buoyancy gives
at . At the lower boundary this is replaced by
For a Fourier component with zero interior PV,
Solving this boundary-value problem in terms of
gives
where, with ,
The boundary equations consequently reduce to
For , define
The determinant gives the Damped Eady-wave dispersion relation
For , the quantity under the square root is real:
It is negative for small and positive for large . Therefore the Eady instability occurs for , where
and modes are neutral for .
For , and is exponentially small. Hence
These are two decoupled Boundary Rossby waves, one localized near each boundary. Their laboratory phase speeds lie just inside the basic velocities and because each propagates intrinsically against the local flow.
At , the real undamped part vanishes. Put
The neutral equation implies . The radicand is therefore
If is chosen with , then
Thus , and the plus branch has
For this is exponential growth. Lower-boundary damping therefore destabilizes the formerly neutral cutoff mode, an example of dissipation-induced instability.
When , the boundary coupling is exponentially small. The two eigenvalues are therefore the diagonal boundary-wave speeds through order :
The lower wave is damped at the imposed rate, while the upper wave is exponentially isolated from the lower boundary and remains neutral to algebraic order. Damping destroys the phase-locked counterpropagating-wave interaction at short horizontal wavelength rather than damping both waves equally.

Articles by others on the same topic (0)

There are currently no matching articles.