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2.2 the Use of Potential Vorticity in Tropical Dynamics Wayne H

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2.2 the Use of Potential Vorticity in Tropical Dynamics Wayne H 2.2 The Use of Potential Vorticity in Tropical Dynamics Wayne H. Schubert∗ 1. Introduction information about the slowly evolving balanced part of the moist, precipitating, atmospheric flow. For a nonhydrostatic, moist, precipitating atmo- In this talk we consider four tropical phenomena sphere, the appropriate generalization of the well- that can be better understood using PV dynamics: known (dry) Ertel potential vorticity principle is (1) The emergence of twin tropical cyclones from super cloud clusters which straddle the equator; (2) DP 1 1 the formation and breakdown of shear zones associ- _ = ( F) θρ + ζζζ θρ; (1) Dt ρ r × · r ρ · r ated with ITCZ convection; (3) the flatness of the trade wind inversion; (4) mixing processes, polygo- where nal eyewalls, and rapid pressure falls in hurricanes. 1 P = ζζζ θρ (2) ρ · r 2. Twin tropical cyclones is the potential vorticity, ζζζ = 2Ω+ u the absolute For simplicity, we now neglect the frictional vorticity, ρ the total density, consistingr× of the sum term in (1) and concentrate on the diabatic of the densities of dry air, airborne moisture (vapor source/sink term, which plays a crucial role in many and cloud condensate) and precipitation, u is the tropical phenomena. This diabatic source/sink term velocity of the dry air and airborne moisture, and in the PV principle (1) can be rewritten as Ra=cP a θρ = Tρ(p0=p) is the virtual potential temper- ature, with T = p=(ρR ) the virtual temperature, p 1 1 ζζζ θ_ k θ_ ρ a _ ρ ρ ζζζ θρ = ζζζ θρ · r ! = P · r ! the total pressure (the sum of the partial pressures ρ · r ρ · r ζζζ θρ k θρ · r · r of dry air and water vapor), p0 the constant refer- ence pressure, Ra the gas constant for dry air, and @θ_ =@Z @θ_ = P ρ ! = P ρ cP a the specific heat at constant pressure for dry @θρ=@Z @Θρ air. Since θρ is a function of total density and total pressure only, its use as the thermodynamic vari- where k = ζζζ= ζζζ is the unit vector along the vorticity able in P leads to the annihilation of the solenoidal vector and @=@j jΘ denotes the derivative along the term, i.e., θ ( ρ p) = 0. Equation (1) is a ρ ρ vorticity vector. Equation (1) can now be written generalizationr of· ther × well-known r (dry) Ertel poten- as tial vorticity principle in three respects: (i) ρ is the DP @θ_ total density, consisting of the sum of the densities = P ρ : (3) of dry air, water vapor, airborne condensate, and Dt @Θρ precipitation; (ii) θ is the virtual potential temper- ρ This form emphasizes the exponential nature of the ature; (iii) Precipitation effects are included in F. In time behavior of P for material parcels. We note two the special case of an absolutely dry atmosphere, P important facts: (i) P 0 near the equator, so that reduces to the usual (dry) Ertel potential vorticity. diabatic heating near the≈ equator has little effect on For balanced flows, there exists an invertibility PV; (ii) θ_ peaks in midtroposphere, so convective principle which determines the balanced mass and ρ clusters are a \material" source of PV in the lower wind fields from the spatial distribution of P . It troposphere and a sink in the upper troposphere. is the existence of this invertibility principle that The effect of the P term on the right hand side of makes P such a fundamentally important dynami- (3) can be understood in the simpler context of the cal variable. In other words, P (in conjunction with shallow water equations. For the inviscid shallow the boundary conditions associated with the invert- water equations with a mass source/sink term Q on ibility principle) carries all the essential dynamical the right hand side of the continuity equation, the ∗Author address: Department of Atmospheric Sci- PV principle is ence, Colorado State University, Fort Collins, CO 80523- 1375; e-mail: [email protected] DP Q = P ; (4) Dt − h where P = h=h¯ ζ is the potential vorticity, with h the fluid depth, h¯ the constant initial mean fluid depth, ζ the absolute vorticity, and D=Dt the mate- rial derivative in the shallow water system. Because of the similarity of (3) and (4), we now examine some shallow water simulations with mass source/sinks near the equator. Figs. 1{3 show the temporal evolution of the shallow water fluid depth, the PV, and the winds produced by an elliptically shaped mass sink within the dotted curve. After 2 days of simulation, a Kelvin wave signature dominates the flow to the east of the mass sink. This Kelvin wave part of the so- lution is essentially invisible on the PV map. In the region of the mass sink, two cyclonic PV anomalies on opposite sides of the equator are being produced through the P Q=h term in (4). Since this term vanishes at the− equator, there is no PV anomaly pro- duced there. Equatorial westerly winds occur in the region of the mass sink and to its west. The geopo- tential and wind fields at this time are very similar to the linear, steady state results of Gill. The two cyclones and the equatorial westerly winds continue to intensity through day 5. The westerly wind burst Figure 1: Formation of twin tropical cyclones, day 1. depicted in Fig. 3 is exactly on the equator. This should excite an oceanic Kelvin wave which is con- fined to within just a few degrees latitude about the dynamically active (i.e., have faster growth rates equator. If the simulated atmospheric convection, of barotropic instability) than wider ones. Narrow outlined by the dotted curve in Fig. 1, is shifted only strips also produce \easterly waves" of shorter zonal slightly north or south, the westerly wind burst does wavelength. Another interesting feature of Fig. 4 is not occur on the equator, and an oceanic Kelvin that, during this barotropic instability process, two wave would probably not be excited. plumes of negative PV are drawn across the equa- tor into the northern hemisphere. Associated with 3. Formation and breakdown of shear zones these PV anomalies are two regions of trade wind associated with ITCZ convection surges in the the southern hemisphere. During the northern summer, the ITCZ over 4. The flatness of the trade wind inversion the Pacific is zonally elongated and often wider and more active on its western and eastern ends. Fig. 4 In schematic north-south cross sections the shows the evolution of the fluid depth, wind, and trade inversion layer is often depicted as sloping up- PV fields produced by an irregularly shaped mass ward as air flows toward the ITCZ. This concep- sink, the outline of which is shown by the dots. A tual view is consistent with purely thermodynamic reversal of the poleward gradient of PV first ap- boundary layer models, which predict a deeper pears during day 2 of the integration, providing the boundary layer with increasing sea-surface temper- necessary condition for the occurrence of barotropic ature and decreasing large-scale subsidence. The instability. At 5 days a cyclonic PV strip that is slopes implied by such thermodynamic models and wider on its eastern and western ends has been pro- incorporated into schematic diagrams are approxi- duced. It is important to also note that the cy- mately 2000 m/1000 km. In contrast, observational clonic PV anomaly is most intense in the poleward studies of the inversion structure over the Atlantic half of the mass sink. This is a robust consequence and Pacific reveal a less dramatic slope, on the or- of the P factor on the right hand side of the po- der of 300 m/1000 km. This inconsistency can be tential vorticity equation. ITCZ cloud bands pro- resolved by adopting a somewhat different view of duce strips of enhanced PV that are about half the the trade inversion layer. In particular, rather than cloud band width. These narrow PV strips are more regarding it as a purely thermodynamic structure, Figure 2: Formation of twin tropical cyclones, day 2. Figure 3: Formation of twin tropical cyclones, day 5. regard it as a dynamical structure, a thin layer of spheric values of PV are carried upward into the high potential vorticity. By formulating a general- upper troposphere. The resulting spatial structure ization of the Rossby adjustment problem, we can of the PV field might be expected to be a tower of investigate the dynamical adjustments of a trade- high PV. Although this conceptual model seems rea- wind inversion layer of variable strength and depth. sonably accurate, it needs some refinement related From the solution of the adjustment problem there to the eye region. Once an eye has formed, there is emerges the notion that the subtropics control the no latent heat release in the central region, and large inversion structure in the tropics, i.e., that the sub- values of PV would not tend to occur there unless tropical inversion height is dynamically extended they were transported in from the eyewall. The re- into the tropics in such a way that there is little sulting spatial structure of the PV field might then variation in the depth of the boundary layer. be expected to be a tower of high PV with a hole in the center or, equivalently, an annular tower of high PV with low PV in the central region. The 5. Mixing processes, polygonal eyewalls, and reversal of the radial PV gradient near the eyewall rapid pressure falls in hurricanes might also be expected to set the stage for dynamic In the intense convective region of a hurricane instability and rearrangement of the PV distribu- the absolute vorticity vector tends to point upward tion.
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