Meng, Z., F. Zhang, P. Markoswki, D. Wu, and K. Zhao, 2012: A modeling study on the development of a bowing structure and associated rear inflow within.

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Presentation transcript:

Meng, Z., F. Zhang, P. Markoswki, D. Wu, and K. Zhao, 2012: A modeling study on the development of a bowing structure and associated rear inflow within a squall line over south China. J. Atmos. Sci., 69, 1182–1207.

Line end vortices develop on either side of the system, and the vortices help enhance the mid-level rear inflow. Cyclonic on the northern end of the system and anticyclonic on the southern end, for an environment of westerly vertical wind shear The Coriolis force acts to intensify the cyclonic vortex and weaken the anticyclonic vortex.

This study examines the formation and evolution of the bowing process for a squall line that occurred in spring 2007 in South China.

shaded : dBZ

contour : geopotential height (m) shaded : precipitation (kgm -2 ) thick contours : θ (K) thin contours : θe (K) (wind at 850 hPa) (kgm -2 )

Qingyuan Wuzhou CAPE : 1067 Jkg -1 CAPE : 747 Jkg -1 solid : normal dash : parallel Wind shear : 15 ms -1 Wind shear : 30 ms -1

WRF V3.2 Starting at 1200 UTC 23 April Initial and boundary conditions provided by 6-hourly FNL NCEP analysis of 1 。 x1 。 Do.1Do.2Do.3Do.4 Grid points 150*120205*172316*205481*451 Horizontal intervals 40.5 km13.5 km4.5 km1.5 km Vertical layers 35 layers Microphysics WSM6 Planetary boundary processes Yonsei State University Cumulus parameterization Grell-DevenyiNo

c ≈ 17 ms -1 c ≈ 16 ms -1

shaded : dBZ blue : 1.5 km RI (> 4 ms -1 ) red : 2.5 km RI (> 4 ms -1 ) line-relative wind vector at 1.5 km height

B Buoyancy Θ’vΘ’v Virtual potential temperature perturbations ΘvΘv Environmental Virtual potential temperature qcqc Mixing ratio of condensate

southnorth

shaded : vertical wind shear (0.25~3 km) red : 50 & 60 dBZ black : 4 & 8 ms -1 RI (2.5 km)

environmental flow pressure gradient bookend vortices

shaded : dBZ line-relative wind vector at 1.5 km height blue : 1.5 km RI red : 2.5 km RI

23/2130 Z contours : θ ， shaded : dBZ shaded : RI contours : p ， (dBZ) (ms -1 )

23/2230 Z 23/2330 Z (ms -1 ) shaded : wind speed contours : p ，

vector : line-relative streamline contour : rear inflow (dBZ)

shaded : dBZ red contour: RI at 2.5 km blue contour: RI at 1.5 km shaded : 1.5 km vertical vorticity contours : 2.5 km vertical vorticity (dBZ) line-relative wind vector at 2.5 km height (s -1 )

shaded : dBZ black contours : RI shaded : 2.5 km vertical vorticity black contours : RI shaded : wind speed(ms -1 ) line-relative wind vector at 2.5 km height (dBZ) (ms -1 ) (s -1 )

shaded : dBZ black contours : RI shaded : 2.5 km vertical vorticity black contours : RI shaded : wind speed(ms -1 ) (dBZ) (ms -1 ) (s -1 )

shaded : 1.5 km vertical vorticity contours : verticial velocity shaded : vertical velocity contours : horizontal vorticity

shaded : 1.5 km vertical vorticity (s -1 )

shaded : dBZ red contour: RI at 2.5 km blue contour: RI at 1.5 km shaded : 1.5 km vertical vorticity contours : 2.5 km vertical vorticity line-relative wind vector at 2.5 km height (s -1 ) (dBZ)

shaded : dBZ black contours : RI shaded : 2.5 km vertical vorticity black contours : RI shaded : wind speed (ms -1 ) (s -1 ) (dBZ) (ms -1 )

shaded : dBZ black contours : RI shaded : 2.5 km vertical vorticity black contours : RI shaded : wind speed(ms -1 ) (s -1 ) (dBZ) (ms -1 )

(s -1 )

shaded : 1.5km vertical vorticity contours : verticial velocity shaded : vertical velocity contours : horizontal vorticity

shaded : 1.5 km vertical vorticity (s -1 )

shaded : dBZ stream line : 2.5 km black contour : RI (dBZ)

shaded : wind shear thick contours : θ (K) thin contours : θe (K) contour : geopotential height (m) (wind at 850 hPa)

The formation of the bowing structure is found to be closely associated with the rear inflow. Midtropospheric rear inflow is forced by bookend vortices, environmental flow and horizontal pressure gradient are not primarily responsible for the formation of the rear inflow. Bookend vortices form mainly through tilting of horizontal vorticity ： southern part ： Vortices are formed through the upward tilting of lower- level baroclinic horizontal vorticity. northern part ： vortices are formed through the downward tilting of upper-level baroclinic horizontal vorticity.

2330 UTC