1. Examining Vortex Rossby Wave (VRW) dispersion relations with numerical experiments Ting-Chi Wu MPO673 Vortex Dynamics Project final report 2011/04/28

2. Motivation and Background Montgomery and Kallenbach (1997) developed a theory for vortex rossby wave (VRW) with dispersion relationship and showed the outward propagating banded features. McWilliams et al (2003) generalized MK97’s work by extending in finite Rossby-number regimes. Cobosiero et al (2009) compared theoretical VRW dispersion relation with observation data (Radar) and have good agreement. However, previous studies only “qualitatively” address the propagation feature of VRW in theory, however, “quantitative” verification against the theory is needed. Comparing with observation requires a few assumptions while in numerical experiment parameter can be assigned to your like. Therefore, numerical model based on linearized shallow water equation in Nolan et al (2001) is used to generate VRW and compare the model results with theory provided by MK97.

3. Linearized Asymmetric Shallow-Water Model Basic state satisfies Gradient wind balance: Perturbations are functions of (r,λ,t): Basic state angular velocity Linearized From Nolan et al (2001)

4. Basic-State profile Modified Rankine vortex (α=0.5) Linear vorticity profile (all the way; to 100km) Changing aspect ratio (increase h) Perturbation profile Balanced Gaussian profile (20% of basic-state) Case studies

5. a. From VRW dispersion relations 2D non-divergent inviscid flow on an f-plane: Linearized Shallow-Water equations on an f-plane : All parameters are determined by basic-state except for n and k, and n is known once you specify the perturbation. Only k is left for estimation.

6. Abs(q n )Real(q n ) b. From Hovmoller diagram Real(q n *Exp(inθ)) C gr C pr C pλ

7. 1. Modified Rankine Vortex Choose α=0.5 (Same as HW#2)

8. Find k ---> Time-Radius Real(q n ) Linear? Approximate rate: 4x10 -8

9. Find k ---> Time-Radius Real(q n ) Linear? Approximate rate: 4x10 -8

10. n=2 n=3 Abs(q n )Real(q n ) Real(q n *Exp(inθ)) t, k,

11. C pr C gr n=2n=3

12. n=2 n=3 C pλ: Counter-clockwise About 20 m/s Radial wavenumber increases with time: n=3 is faster than n=2. Azimuthal propagation slows down faster.

13. 2. Linear Vorticity profile RMW=75km Vorticity extend=100km 2x10 -3 4x10 -3 By simplifying (linearizing) the vorticity profile, we hoped to have better approach of the theory.

15. VRW can be generated by perturbations far from core where almost no gradient exist. RMW 2*RMW 3*RMW

16. 3. Change Aspect Ratio To investigate if increasing H (decrease aspect ratio) can make the dispersion relation approach 2D Hmax = 10 km ratio= 300km/10km = 30 Hmax = 300 km Ratio = 300km/300km = 1

17. Identical? Only different in magnitude.

20. Conclusion and discussion By perturbing the vortex at some distance (~ 2xRMW or 3xRMW), VRW can be radiating outward from core. Perturbations of different azimuthal wavenumber shows consistent results from theory. While radial wavenumber is the key to the dispersion relation, it is also a relatively difficult parameter to determine. In our case studies, k is usually one to two order larger than observation value ( ~ 10 -5 ). C pr matches with the theory pretty well with different vorticity profile. This might be the dominant “apparent” terms in the propagation speed, and so does C pλ. C gr from theory is two order less than calculated from Hovmoller diagram. Changing aspect ratio does not change the vortex evolution because the dominant term of h in potential vorticity gradient cancel with the h in mean potential vorticity.

21. Conclusion and discussion Some thoughts why Cgr is not matching: dqdr v.s. wavelength Planetary Rossby Wave: – beta ~ 10 -11 m -1 s -1 ; wavelength ~ 10 6 m Vortex Rossby Wave: – dqdr ~ 10 -12 -10 -11 m -1 s -1 ; wavelength 10 3 - 10 4 m

22. Linearized Shallow Water2D ω CpCp CgCg