1. Momentum Budget of a Squall Line with Trailing Stratiform Precipitation: Calculation with a High-Resolution Numerical Model. Yang, M.-J., and R. A. Houze Jr., 1996, J. Atmos. Sci., 53, 3629-3652.

2. Introduction  The separate roles of the convective and stratiform precipitation regions have not been investigated in terms of how they may influence the largescale horizontal momentum field.  The objective of this study is thus to investigate the momentum budget of a two-dimensional squall line with leading-line/trailing-stratiform structure and thereby gain insight into the contributions of the convective and stratiform precipitation regions to the momentum transports over a largescale region containing the storm.

3. Introduction  To achieve this objective, they make use of the numerical simulation results for the 10-11 June 1985 squall line in PRE-STORM (Yang and Houze, 1995a,b).

4. Model description  2D nonhydrostatic cloud model (Klemp and Wilhelmson, 1978; modified by Wilhelmson and Chen, 1982)  The model has a 314-km-wide fine mesh with 1-km resolution in the center of the domain.  The model domain translates with the storm such that the simulated storm is always within the fine mesh.

5. Model description  The initial environmental conditions are based on the 2331 UTC 10 june 1985 sounding obtained at Enid, Oklahoma, 4h before the squall line passed this station.  The model was integrated for 15h.

6. Initial stage (7.5-8.5h) Mature stage (10-11h) Slowly decaying stage (12.5-13.5h)

7. CV: convective precipitation SF: stratiform precipitation RA: rear anvil FA: forward anvil

8. Storm-relative horizontal wind inflow ascending FTR descending RTF FTR flow

9. vertical velocity updraft downdraft weak vertical motion forced by the strong convergence caused by the release of latent heat of condensation mesoscale updraft mesoscale downdraft mesoscale ascent and descent were weaker

10. by the release of latent heat adiabatic temperature increase in the unsaturaed descent air by latent cooling of evaporation and melting reached -10K reached -9K potential temperature perturbation wider, deeper, and stronger produced by mesoscale downdraft

11. pressure perturbation meso- γ -scale low broadens and intensifies continues to broadens subsidence warming

12. subregional contributions to the large-scale mean horizontal and vertical velocity fields  large-scale area A=A CV +A SF +A RA +A FA  a physical quantity I: –σ:

13. vertical velocity [ I = w in (2) ] mesoscale updraft mesoscale downdraft

14. storm-relative horizontal velocity [ I = u - c in (2) ]

15. Time-averaged momentum equation  TEN PGF HAD VAD TRB  time-averaged form:

16. u-momentum equation initial stage ADV =HAD+VAD

17. u-momentum equation mature stage

18. Area-averaged momentum budgets  area-averaged form:

19. u-momentum equation mature stage FTRRTF

20. FTRRTF u-momentum equation over the large-scale area A

21. once the system matures, the stratiform precipitation region determines the net momentum tendency of the large-scale area A.

22. formulation of momentum flux  The total vertical flux of storm-relative horizontal momentum into three physically distinct parts: T tot S m S e T e  S m : transport by steady mean flow  S e : transport by standing eddies  T e : transport by transient eddies

23. vertical flux of storm-relative momentum The 1-h averaged velocity field in the simulated storm thus behaves as if the storm were in a steady state. All of the fluxes are transporting FTR momentum upward or RTF momentum downward. negative

24. The wind vectors of: (a) domain- averaged mean flow (b) standing eddy (c) total wind mesoscale circulation FTR + weak upward motion

25. vertical momentum flux by standing eddies S e 6.5 convective precipitation region momentum flux by standing eddies S e

26. Large-scale momentum budget TEN PGF HMF VMF VEF  The primary terms determining the large-scale momentum tendency TEN are PGF and (VMF+VEF).  And this two terms tend to oppose each other.

27. FTRRTF FTR PGF VEF

28. Conclusions  Decomposition of total momentum flux into three physically distinct modes – transports by steady mean flow, standing eddies, and transient eddies – shows that in the middle to upper levels, the transport by steady mean flow contributes most of the total momentum flux.  The transport by standing eddies explains most of the total momentum flux in low to middle levels.

29. Conclusions  summarizes the momentum balance The net momentum tendencies are a delicate imbalance of strong terms of opposite sign. RTF FTR RTF

30. Thanks

31. vertical convergence of momentum flux  Moncrieff (1992)  follow  =>

33. Convective and Stratiform precipitation  The partition between the convective and stratiform precipitation regions is based on simulated surface rainfall rate.  The convective precipitation region either has a surface rainfall rate greater than or equal to 15 mm h -1, or the gradient of rainfall rate is greater than 5 mm h -1 km -1.  The surface precipitation region not satisfying these criteria is defined as the stratiform precipitation region.