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 givesin the interior. Since , perturbation advection of the boundary buoyancy givesat . At the lower boundary this is replaced by
For a Fourier component with zero interior PV,Solving this boundary-value problem in terms ofgiveswhere, with ,The boundary equations consequently reduce toFor , defineThe 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 , whereand modes are neutral for .
For , and is exponentially small. HenceThese 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. PutThe neutral equation implies . The radicand is thereforeIf is chosen with , thenThus , and the plus branch hasFor 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
There are currently no matching articles.