Vol.26, NO.2, 2015
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Article Navigation >  Journal of Applied Meteorological Science  > 2015  >  26(2): 160-172
Wu Qingmei, Liu Zhuo, Wang Guorong, et al. The influence of boundary layer east wind on a North China rainstorm. J Appl Meteor Sci, 2015, 26(2): 160-172. DOI:  10.11898/1001-7313.20150204.
Citation: Wu Qingmei, Liu Zhuo, Wang Guorong, et al. The influence of boundary layer east wind on a North China rainstorm. J Appl Meteor Sci, 2015, 26(2): 160-172. DOI:  10.11898/1001-7313.20150204.
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The Influence of Boundary Layer East Wind on a North China Rainstorm

DOI: 10.11898/1001-7313.20150204

  • Beijing Meteorological Observatory, Beijing 100089

  • Received Date: 2014-07-24
  • Rev Recd Date: 2014-12-05
  • Publish Date: 2015-03-31
    Abstract
  • Using conventional observations, 1°×1° NCEP analysis data, ground-based radiometer data, FY-2E meteorolgical satellite and radar data, the boundary layer east wind and its influence on a North China rainstorm on 4 Jun 2013 is analyzed.The boundary layer east wind is from Northeast China Plain, and it becomes moist when passing the Bohai Sea, resulting in cooling in boundary layer, and the sharpest drop is about 9℃ at 925 hPa. The east wind influencing area is within about 300 km. The east wind and according temperature change are monitored accurately by the ground-based radiometer and profile radar, and the storm is triggered after the temperature decreases for about 5 hours.Main influencing weather systems of the rainstorm are the boundary layer east wind, wind shear at mid-low level, southwest low-level jet at 700 hPa and small-scale low trough at 500 hPa. The cold air caused by the boundary layer east wind meets the warm southwest air on the windward area of the Taihang and Yan Mountains, and the cold front is formed near Beijing area. The front lift and topographic lift effects are obvious and the according upward motion is about-0.8 Pa·s-1, which strengthens upward motion of the warm and moist air near 700 hPa at the north of Beijing. The east wind leads to cooling cushion and temperature inversion at boundary level, and cooling cushion effect triggers the thunderstorm again to some extent, which is generated above the boundary layer, and the most unstable convective available energy reaches 1517.5 J·kg-1. The elevated thunderstorm is found first to the east of the Taihang Mountains because of topographic lift effect. The analysis of infrared TBB of FY-2E shows that middle convective systems develop obviously when they move near the cold front of east wind. The thunderstorm occurs again just over the east wind cooling cushion area according to radar reflectivity.The moist is sent to the storm area by east winds from boundary layer and southwest winds at mid-low level. The mid-low level warm moist air leads to the increase of stratification convective instability, and at 850 hPa is 8.2 K and 11.7 K more than that of 500 hPa at 0800 BT and 2000 BT, respectively. There is strong dynamic instability over the storm area because the distinct vertical wind shear is formed by boundary layer east winds and strong southwest winds at middle level.
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  • Fig. 1  Observed 24 h rainfall (number, unit:mm) from 0800 BT 4 Jun to 0800 BT 5 Jun in 2013 with terrain (the shaded)(a) and 500 hPa geopotential height (contour, unit:dagpm) and winds at 0800 BT 4 Jun 2013(barb)(the thick solid is trough line)(b)

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    Fig. 2  Sea level pressure (solid line, unit:hPa) and 2 m wind at 2000 BT 3 Jun 2013(a), 0800 BT 4 Jun 2013(b) and wind observed by auto weather stations at 0000 BT 4 Jun 2013(c), 0400 BT 4 Jun 2013(d)(the double line denotes wind shear, the thick solid line denotes cold front, the arrow denotes the path of east wind, the dot denotes the wind speed is zero)

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    Fig. 3  Temperature (solid line, unit:℃) and wind at 0800 BT 4 Jun 2013 (the double line denotes warm wind shear line) (a)925 hPa, (b)700 hPa

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    Fig. 4  Wind of different heights observed by wind profile radar at Haidian Station in Beijing on 4 June 2013

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    Fig. 5  Temperature (unit:℃) of different altitudes observed by radiometer at Beijing Weather Observatory from 3 Jun to 4 Jun in 2013

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    Fig. 6  The zonal cross-section of q (dashed line, unit:g·kg-1) and wind (barb) along 40°N

    (a)2000 BT 3 Jun 2013, (b)0200 BT 4 Jun 2013, (c)0800 BT 4 Jun 2013

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    Fig. 7  The vertical velocity from 4 June to 5 Jun in 2013(unit:Pa·s-1)

    (a)850 hPa at 0800 BT 4 Jun, (b)700 hPa at 0800 BT 4 Jun, (c)700 hPa at 2000 BT 4 Jun, (d)850 hPa at 0200 BT 5 Jun

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    Fig. 8  The zonal cross-section of vertical velocity (contour, unit:Pa·s-1) and wind (barb) at 0800 BT (a) and 2000 BT (b) on 4 Jun 2013 along 40°N

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    Fig. 9  Sea level pressure (solid line, unit:hPa) and 2 m wind (barb)(a), temperature (contour, unit:℃) and wind (barb) of 700 hPa (b) at 2000 BT 4 Jun 2013

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    Fig. 10  Distribution of temperature of black body from infared images of FY-2E at 0700 BT (a) and 1000 BT (b) on 4 Jun 2013

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    Fig. 11  Combined radar reflectivity above 15 dBZ of Beijing Weather Observatory on 4 Jun 2013

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    Fig. 12  The zonal cross-section of temperature (dashed, unit:℃) and θse(solid line, unit:K) along 40°N at 0800 BT (a) and 2000 BT (b) on 4 Jun 2013

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    • Received : 2014-07-24
    • Accepted : 2014-12-05
    • Published : 2015-03-31
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