University:
Massachusetts Institute of Technology
Course:
12.820 | Turbulence in the Ocean and Atmosphere
Academic year:

2022
Views:

314

Pages:

7
Author:

yucasmoderating

QG Turbulence and Waves The quasigeostrophic equation contains a number of essential features of large scale geophysical flows, while retaining some of the simplicity of 2D flow. We assume that the system is rapidly rotating and hydrostatic, so that the vertical vorticity equation becomes with C = (-v,,ll.,,() and the P-plane approxin~ationf = f,, +By. We assume that C is sinall compared to f ( R o = C/ f << 1) though it nYay be similar in size to 6 f / f = PL/ f . In that case the term C . Vw is order (1f compared to f g u i . Thus the vortex stretching is dominantly associated with fluid columns suffering extension along the rotation axis. We can in general represent a nondivergent flow as a a and we choose a gauge such that z$l + -g2 a?] = 0 so that Then = gd and g2 = --$axa . For near-geostrophic balance, 1* u=-ZXV?, f . order DL/ f times the vorticity. Thus the vorticity equation becomes the divergence am 1s 3 -C3 t + J($, C + by) = f 32a + disa -lri aAF aB aA a B and C = V2+ with J ( A , B) = z qz The buoyancy equation can also be simplified by neglecting the divergent part of the horizontal flow and noting that &b/N2 is order ((1f ) ( f2 L 2 / N 2 H 2f;or synoptic/ mesoscale flows the last factor is order one. Thus - a = f z$ a and combining gives the QG equation Using b = ~p 3 -q 3t with + .J($,q) = di.s.s/heat 3 f2 3 q=V2$+---$+BY Dz N2 Dz The QG equations determine the evolutioil of a scalar property, the approximate potential vorticity q , under advection by the horizontal flow u = i x V$. Although the movement of PV is treated two-dimensionally at a given depth, the flow is related to the PV structure at nearby depths. Conserved properties The QG equations preserve energy and potential enstrophy Indeed, they conserve the average of any function of the PV, not just the square, so that we have to worry about whether or not the energy and entrophy tell the whole story. The /3 term also can have importailt consequences, depending on the boundaries. If we represent rl=Lli,+Py In the doubly-periodic case with uniform buoyancy on the top and bottom bouildaries (&$ = 0) the only surviving term is the one which can be thought of as Jd3x K2E. We'll talk about other cases later. Charney (1971) argues that for small enough scales in the interior of the atmosphere, we call treat N 2 as constant: rescale z* = N z / f , and transform the L operator into V:$. All of the arguments for upscale energy transfer and downscale enstrophy transfer apply. so that the spectrum should be just as in the 2-D case. In addition, the theory predicts equipartition of energy among the Ir: 11; and bf / N fields. Demos, Page 2: Data FjijrtijR1sargurrlent; Fjiirtiift's (1953) argument can also be applied to the 3D QG flow problem. Suppose we have unit energy a t a net waveilumber K such that and we wish to transfer it elsewhere through illviscid iilteractions. Let a fraction al go to larger scales ( K / 2 )and a2 to smaller scales 2K. Then our energy and enstrophy pictures look like K/2 Wavenuinber Init. energy 0 1 0 Init. enstrophy 0 K2 0 Final energy a1 1 a l p a2 *z Final enstrophy K2a1/4 K 2 ( 1 a1 a 2 ) K24a2 - - - If we conserve both energy and enstropl~yby this interaction (i.e., we're in an inertial range), we find a1 = 4az so that Init. energy 0 1 0 Init. enstrophy 0 K 0 Final energy 4a2 1 5a2 az Final enstropl~y K 2 a z K 2 ( 1 5a2) K24a2 - - More energy is transferred to large scales and more enstrophy to sinall scales. Indeed the center of the energy is now a t wavenumber K ( 1 az) and the center of the enstropl~yis at K ( 1 f 3 . 5 ~ ~R.emember ). that in the cascade t o larger scale) the vertical scale can increase the flow can become inore barotropic. - Beta effects Demos, Page 3 : b e t a runs Note that these arguments make no mention of the variation of the Coriolis parameter with latitude, P. While it is true that the P-effect does not make the QG equations inhomogeneous (the full equations or the shallow water equations are a different matter)) it does make the dynamics anisotropic. R.otation by 90 degrees alters the form of q . R.hines showed that turbulence on the P-plane has a profoundly different charater, developing = 0 case of the zonal bands of flow. He used the barotropic vorticity equation (the QG equation, though the BTVE is actually an exact representation of 2-D motion on a P-plane) & The dyilainics now iilcludes both turbulence and waves riding on the large-scale potential vorticity gradient p. The evolution of the flow beconles at some point a problem of interacting waves rather than nlultiple-scale energy transfers. We can see that this will happen at some scale by considering the parameter measuring iloillinear versus wave effects the wave steepness S = U/c. Since the phase speed for R.ossby waves is -,!3/k2: S = Uk2/p. For a k:-3 energy spectrum, we have the velocities proportional to k p l and the steepness behaves like k. Therefore: we expect the P-effect will have little influence on the short waves, but that the long waves will have restoring forxes which are as significant as the turbulent transfers. The scale a t which this transition = E~/~,!Y~/~. occurs should be when the steepness is order one, or L Alternatively, we could view the effects of the turbulence as mixing the PV and attempting t o homogenize it. But this can only be done over narrow latitude bands. Suppose we start with an initial eddy energy density E. If we hoinogenize the PV over width W , the zonal mean flow looks like - N 3 -U 3~ + Py = const. = 0 for - W/2 < y < W/2 so that U = ,!3y2/2 PW2/24. The energy density for this flow is - If we used all the initial energy and put it into zonal flow, we'd have Two things prevent this froin happening; not all of the energy goes into the waves and the interactions become very slow as wave processes dominate. Demos, Page 4 : Means Baroclinicity The transfer to large scale occurs in both horizoiltal and vertical directions. Therefore, we expect the energy in the gravest vertical mode (F = 1; A,) = 0) to dominate after a while. We can expand q' = L?i, and ?i, in the vertical eigenfunctions with r = v , , - A2?i, ,,, The F , functions are the eigenfunctions of the vertical operator Then the energy is E= Demos, Page 5: - [/%,!,$,,, + + Ez... = EO El Two vertical mode case Spectral space transfers Let us transform the streanlfunction to wavenumber space li, = $(k, t, na, t) exp(zk.r + dy)F ,, (z) q' = i(k,t , 7n,,t) exp(zk.r + zty)F ,,,(2) We introduce a shorthand ?i,? = $(k:, t, A,!,, t) so that each different subscript j corresponds to a different set of {k:, !; na) values. The streainfunction is related to the poteiltial vorticity by q? = ( k ; t; K;g1 + + - Now we can project out the equation for the amplitude of one mode by multiplying the equation by F,,,, (2) exp(-zk2 . x) and volunle averaging with the definition k3 = k l - kz. Let us look at one set of wavenumbers k l , k2, k3 and choose the labelling such that K: < K: < K;. The dynamics of this triad is given by This triad conserves energy and enstrophy iilterilally From the triad equations, we also have Energy leaving component 2 will transfer into both 1 and 3; when it does so, the average Kg > Kg K; scale (CK j E j / C E,)-' increases; however, oilly the triads with K: will actually put inore energy into the larger scale mode than the smaller scale one. Demos, Page 6 : Example < (0,0,0)t r i a d s > - - STABILITY:If we start with energy in the second component, we can calculate the rate at which it goes to other components by looking at the growth rate. We assume and so that the perturbation problem becomes The growth rates are determined by when the amplitude is small, the growth rate will be nonzero only in the regions where Demos, Page 6: Resonance Demos, Page 7: Demos, Page 7: <(1,1,0)> Resonance-angle Resonance-modes <(0,1,1)> < (0,0,0)> < (1,1,0)> < (0,1,I)>

QG Turbulence and Waves

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