Baroclinic annulus flows with sloping boundaries
jump to navigationThe presence of boundaries at the top and bottom of the channel which are inclined in the radial direction may have some important modifying affects on baroclinic wave flows. This is partly because flow adjacent to a radially-sloping boundary will tend to be forced towards a trajectory in the meridional plane moving parallel with the slope – which may affect the ability of fluid parcels to release potential energy within the baroclinic ‘wedge of instability’ (see [link]). This may be seen more clearly in the figure below for cases where the upper and lower boundary slope in the opposite sense.
The diagram above illustrates the energetics of baroclinic instability with parallel sloping upper and lower boundaries. Thick solid lines show the upper and lower boundaries, thin solid lines the geopotentials, dashed lines indicate isotherms or isopycnals and arrows indicate the angle of parcel interchange (after Mason 1975).
The effect is shown most clearly in the leftmost column, which corresponds to the situation of marginal baroclinic instability. In this case, with horizontal endwalls the preferred trajectory for parcel interchange is parallel with the isotherms – which releases no potential energy and so is a state of neutral stability.
- With endwalls sloping in the same sense as the isotherms/isopycnals, parcel interchange is constrained to slope more steeply than before (with horizontal boundaries). This actually requires increased potential energy to interchange fluid parcels, implying a positively stable condition for baroclinic instability.
- With endwalls which slope in the opposite sense to the isotherms/isopycnals, the preferred trajectory for parcel interchange is less steep than for horizontal boundaries. This actually forces the slope of the interchange trajectory into the ‘wedge of instability’, allowing the spontaneous release of potential energy. The result is that the flow is destabilised and growth of baroclinic waves is enhanced.
The other main effect of sloping boundaries may be to introduce a form of ‘planetary vorticity gradient’. If the upper and lower boundaries slope at different angles, the depth of the annulus becomes a function of radius. Such a variation can be shown to be directly equivalent to a planetary ‘beta effect’ in the case of purely barotropic flow. In that case, azimuthally travelling waves will become dispersive and behave like Rossby waves in the atmosphere or oceans. For baroclinic flows, however, this analogy is more complicated, and effects may be a mixture of both beta-effects and changes to the baroclinic stability characteristics of the flow.
These effects can be illustrated in laboratory experiments. A schematic arrangement is shown below.
Schematic apparatus for studying the effects of sloping boundaries on baroclinically unstable flows. Upper and lower boundaries can be sloped at either positive or negative angles θu and θl.
Group 1 - Ω = 1.5 rad s-1
- θu = θl = 0 (no slope): m = 4
- θu = θl = 24° (upward slope, opposite to isotherms): m = 5
- θu = θl = 24° (upward slope, parallel to isotherms): m = 2AV
- -θu = θl = -24° (opposite slopes): m = 3