Vol.24, NO.3, 2013
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Article Navigation >  Journal of Applied Meteorological Science  > 2013  >  24(3): 257-267
Cheng Zhengquan, Chen Lianshou, Li Ying. Influences of continental high on inland torrential rain associated with severe tropical storm Bilis (0604). J Appl Meteor Sci, 2013, 24(3): 257-267.
Citation: Cheng Zhengquan, Chen Lianshou, Li Ying. Influences of continental high on inland torrential rain associated with severe tropical storm Bilis (0604). J Appl Meteor Sci, 2013, 24(3): 257-267.
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Influences of Continental High on Inland Torrential Rain Associated with Severe Tropical Storm Bilis (0604)

  • 1.

    Key Laboratory of Regional Numerical Weather Prediction, Guangzhou 510080

  • 2.

    Guangzhou Central Meteorological Observatory, Guangzhou 510080

  • 3.

    Chinese Academy of Meteorological Sciences, Beijing 100081

  • Received Date: 2012-08-09
  • Rev Recd Date: 2013-02-28
  • Publish Date: 2013-06-30
    Abstract
  • The remnant vortex of severe tropical storm Bilis (0604) endures over land for a few days, results in a large range of torrential rain over South China and leads to a calamity after it lands in Fujian Province on 14 July 2006. Many studies are carried out and reveal the crucial effect of low level southwesterly monsoon jet to the extreme rain event. But the influence of the continental high on the torrential rain is also worth being discussed. The analysis of circulation shows that during the torrential rain process associated with Bilis, the continental high at upper level strengthens, moves eastwards, and stretches downwards to the low level after Bilis makes landfall, which strengthens the northeasterly stream at the southeastern side of the continental high. When Bilis moves westwards, the northeasterly stream at the low and middle levels in the northwestern quadrant of Bilis, overlapping with that southeast to the continental high, is strengthened and increases the transfer of water vapor and instability energy to the inland, which is favorable to the maintenance of the remnant low and the typhoon trough. The vorticity above the inland rainstorm area remains high during the process. The budget shows that it is the long existing remnant vortex and typhoon trough whose intense convergence at the low level produces a large amount of vorticity, triggers the successive development of MCS and results in the continuous heavy rain. The contribution of the continental high is to help the maintenance of the remnant low and the typhoon trough, and to enlarge the horizontal advection of vorticity at the upper level. And a set of numerical sensitivity experiments reveals that, based on the background of strong southwestern monsoon, the intensification and eastward stretch of the continental high not only forces Bilis to move southwestwards, but also provides strong divergence at upper level over Bilis. Besides, the continental high influences the intensity and the distribution of heavy rain. The endurance of the remnant vortex and the typhoon trough, due to the strong low level southwesterly monsoon jet and the continental high, enhances the intensification of vorticity above the inland rainstorm area and the occurrence of torrential rain. And in the sensitivity experiment of weakened continental high, the northeasterly winds in the northwestern quadrant of Bilis become weakened and the transfer of water vapor to the inland rainstorm area and the vorticity decrease accordingly, which leads to the northward movement of rain bands and the decline of rain intensity with the decrease of the 24 h rainfall maximum in the inland by 1/3, compared with the control experiment.
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    References(21)

  • Fig. 1  The track (a) and process rainfall (b) of Bilis

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    Fig. 2  Circulations at 0000 UTC 15 July 2006 (a) wind (vector) and height (contour, unit:gpm) fields at 200 hPa, (b) wind (vector) and height (contour, unit:gpm) fields at 500 hPa, (c) wind (vector) and water vapor flux (shaded, unit: g·cm-1·hPa-1·s-1)) fields at 850 hPa

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    Fig. 3  Regional average of geo-potential height of continental high at 200 hPa (a), 500 hPa (b) and 700 hPa (c) within 32°—40°N, 98°—108°E and regional average of wind velocity (unit:m·s-1) in the northwestern quadrant of Bilis (5°×5° domain) in July 2006

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    Fig. 4  Dynamic composite fields at 850 hPa before and after landfall

    (vector: wind; contour: specific humidity, unit: g·kg-1; shaded: water vapor flux, unit: g·cm-1·hPa-1·s-1; coordinates represent grid number with the grid space 1.0 degree from typhoon center, while negative denotes westwards and southwards, TC center locates at the origin) (a) 2 days before landfall, (b) 2 days after landfall

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    Fig. 5  Regional average of vorticity and its budget over the inland rainstorm area in July 2006

    (a) regional average of vorticity (unit: 10-5s-1), (b) horizontal divergence term (unit: 10-5s-2), (c) horizontal advection term (unit: 10-5s-1), (d) vertical transfer term (unit: 10-10s-2)

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    Fig. 6  Comparison of control and sensitivity experiment outputs to observations

    (a) track, (b) minimal sea level pressure from 14 July to 16 July in 2006

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    Fig. 7  Accumulated rainfall in 24h from observations, control and sensitivity experiments

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    Fig. 8  Comparison of the regional average of wind velocity in the northwestern quadrant (a 5°×5° domain) of Bilis (a) and divergence at 200 hPa (10°×10° domain)(b) between control and sensitivity experiments in July 2006

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    Fig. 9  Regional average of vorticity over the inland rainstorm area 24°—27°N, 112°—114°E in July 2006

    (a) control experiment, (b) sensitivity experiment

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    Table  1  Survey of rain events caused by Bilis from 0000 UTC 14 July to 0000 UTC 18 July in 2006

    降水量 累计站次
    过程降水量≥200 mm 81
    过程降水量≥300 mm 31
    过程降水量≥400 mm 11
    过程降水量≥500 mm 3
    过程降水量≥600 mm 1
    24 h降水量≥100 mm 129
    24 h降水量≥250 mm 7
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    Table  2  Synchronous and lag correlation coefficients between regional average of 200 hPa height and that of lower levels over the continental high of 32°—40°N, 98°—108°E

    相关 300 hPa 500 hPa 700 hPa 850 hPa
    同步 0.996 0.832 0.519 0.361
    滞后6 h 0.965 0.814 0.642 0.579
    滞后12 h 0.935 0.864 0.730 0.633
    滞后18 h 0.942 0.924 0.745 0.568
    滞后24 h 0.935 0.903 0.745 0.602
    滞后30 h 0.856 0.837 0.839 0.730
    滞后36 h 0.765 0.838 0.815 0.767
    DownLoad: Download CSV
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    • Received : 2012-08-09
    • Accepted : 2013-02-28
    • Published : 2013-06-30
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