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Influences of Continental High on Inland Torrential Rain Associated with Severe Tropical Storm Bilis (0604)
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摘要: 强热带风暴碧利斯 (0604)(简称碧利斯) 登陆后造成极其严重的灾害。对该次强降水过程诊断分析发现，除强盛的西南季风外，深厚的大陆高压也起着重要作用。自高层向低层逐渐加强的大陆高压，其东南侧深厚的偏东北气流，与碧利斯登陆后西北象限的东北风相叠加，配合强盛的西南季风，使得碧利斯残涡以及槽区得以长时间维持。涡度收支表明:长时间维持的台风槽，其低层强烈的辐合效应，对暴雨区低涡发展作用显著，致使中尺度对流系统不断发展而造成内陆连续强降水。数值试验表明：在强盛西南季风背景下，大陆高压的增强东伸，不仅能够提供高空强辐散，而且能增强碧利斯西北象限东北风，使得登陆后减弱的碧利斯残涡和台风槽得以长时间维持，致使内陆暴雨区各层涡度增加而导致暴雨维持与增幅。
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关键词:
- 强热带风暴碧利斯 (0604);
- 强降水;
- 大陆高压;
- 涡度收支
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. -
图 2 2006年7月15日00:00形势场 (a) 200 hPa风场 (矢量) 及高度场 (等值线，单位：gpm), (b) 500 hPa风场 (矢量) 及高度场 (等值线，单位：gpm), (c) 850 hPa风场 (矢量) 及水汽通量 (阴影，单位：g·cm-1·hPa-1·s-1)
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
图 3 2006年7月各层大陆高压区域32°~40°N，98°~108°E 200 hPa (a), 500 hPa (b) 和700 hPa (c) 平均位势高度以及碧利斯西北象限 (5°×5°经纬度范围) 平均全风速随时间-高度的变化 (单位：m·s-1)(d)
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
图 4 碧利斯环流的850 hPa风场的动态合成图
(矢量表示风场；等值线表示比湿，单位：g·kg-1；阴影表示水汽通量，单位：g·cm-1·hPa-1·s-1; 横、纵坐标代表距离台风中心的格点数，向西、向南为负，格距为1个经纬度，碧利斯位于网格中心) (a) 登陆前2 d，(b) 登陆后2 d
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
图 5 2006年7月粤湘交界暴雨区平均涡度及其收支
(a) 平均涡度 (单位：10-5s-1), (b) 水平散度项 (单位：10-10s-2), (c) 水平平流项 (单位：10-10s-2), (d) 垂直平流项 (单位：10-10s-2)
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)
图 6 控制试验、敏感性试验模拟结果与观测对比
(a) 路径，(b) 2006年7月14—16日中心附近最低海平面气压
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
图 7 2006年7月观测、控制试验与敏感性试验24 h累积降水量对比
Fig. 7 Accumulated rainfall in 24h from observations, control and sensitivity experiments
图 8 控制试验与敏感性试验中碧利斯西北象限 (5°×5°经纬度范围) 区域平均风速 (a) 与碧利斯高空200 hPa区域 (10°×10°经纬度范围) 平均散度 (b)
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
图 9 2006年7月内陆暴雨区 (24°~27°N，112°~114°E) 平均涡度随时间-高度的变化
(a) 控制试验，(b) 敏感性试验
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
表 1 2006年7月14日00：00—18日00：00碧利斯降水过程概况
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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表 2 大陆高压 (32°~40°N，98°~108°E) 区域平均200 hPa高度与各层高度场滞后相关系数
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
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[1] 陈久康, 丁治英.高低空急流与台风环流耦合下的中尺度暴雨系统.应用气象学报, 2000, 11(3):271-281. http://qikan.camscma.cn/jams/ch/reader/view_abstract.aspx?file_no=20000342&flag=1 [2] 李英, 陈联寿, 徐祥德.水汽输送影响登陆热带气旋维持和降水的数值试验.大气科学, 2005, 29(1):91-98. http://www.cnki.com.cn/Article/CJFDTOTAL-DQXK200501010.htm [3] 陈联寿.热带气旋研究和业务预报技术的发展.应用气象学报, 2006, 17(6):672-681. doi: 10.11898/1001-7313.20060605 [4] 李英, 陈联寿, 雷小途.高空槽对9711号台风变性加强影响的数值研究.气象学报, 2006, 64(5):553-563. http://www.cnki.com.cn/Article/CJFDTOTAL-QXXB200605001.htm [5] 于玉斌, 姚秀萍.对华北一次特大台风暴雨过程的位涡诊断分析.高原气象, 2000, 19(1):111-120. http://www.cnki.com.cn/Article/CJFDTOTAL-GYQX200001013.htm [6] 郑庆林, 宋青丽. 一个台风暴雨模式和山地地面拖曳效应对登陆台风暴雨增幅影响的数值研究//台风科学、业务试验和天气动力学理论的研究 (第四分册). 北京: 气象出版社, 1996: 215-221. [7] 郑庆林, 吴军, 蒋平.我国东南海岸线分布对9216号台风暴雨增幅影响的数值研究.热带气象学报, 1996, 12(4):304-313. http://www.cnki.com.cn/Article/CJFDTOTAL-RDQX604.002.htm [8] Shen W, Ginis I.A numerical investigation of surface water over land on landfalling hurricanes.J Atmos Sci, 2002, 59(4):789-802. doi: 10.1175/1520-0469(2002)059<0789:ANIOLS>2.0.CO;2 [9] 陈联寿, 丁一汇.西太平洋台风概论.北京:科学出版社, 1979:442-447. http://www.cnki.com.cn/Article/CJFDTOTAL-SYQY201603027.htm [10] 张艳霞, 钱永甫, 王谦谦.西北太平洋热带气旋的年际和年代际变化及其与南亚高压的关系.应用气象学报, 2004, 15(1):74-80. http://qikan.camscma.cn/jams/ch/reader/view_abstract.aspx?file_no=20040110&flag=1 [11] 魏维, 张人禾, 温敏.南亚高压的南北偏移与我国夏季降水的关系.应用气象学报, 2012, 23(6):650-659. doi: 10.11898/1001-7313.20120602 [12] 朱乾根, 林锦瑞, 寿绍文, 等.天气学原理和方法.北京:气象出版社, 1992. http://www.cnki.com.cn/Article/CJFDTOTAL-SYQY201603027.htm [13] 康志明, 陈涛, 钱传海, 等.0604号强热带风暴"碧利斯"特大暴雨的诊断研究.高原气象, 2008, 27(3):596-607. http://www.cnki.com.cn/Article/CJFDTOTAL-GYQX200803016.htm [14] 程正泉.登陆热带气旋特大暴雨机制研究.北京:中国气象科学研究院, 2008. [15] 程正泉, 陈联寿, 李英.登陆热带气旋与夏季风相互作用对暴雨的影响.应用气象学报, 2012, 23(6):660-671. doi: 10.11898/1001-7313.20120603 [16] 程正泉, 陈联寿. 0604号强热带风暴"碧利斯"与0605号台风"格美"强降水对比分析//第14届全国热带气旋科学讨论会, 2007: 59-65. [17] 蒋小平, 刘春霞, 费志宾, 等.南海夏季风对强热带风暴Bilis (0604) 引发暴雨的影响.热带气象学报, 2008, 24(4):379-384. http://www.cnki.com.cn/Article/CJFDTOTAL-RDQX200804012.htm [18] 李英, 陈联寿, 王继志.登陆热带气旋长久维持与迅速消亡的大尺度环流特征.气象学报, 2004, 62(2):167-179. doi: 10.11676/qxxb2004.018 [19] 丁一汇.天气动力学中的诊断分析方法.北京:科学出版社, 1989:176-177. http://www.cnki.com.cn/Article/CJFDTOTAL-SYQY201603027.htm [20] 卢咸池, 何斌.初值格谱变换的比较分析.计算物理, 1992, 9(4):768-770. http://www.cnki.com.cn/Article/CJFDTOTAL-JSWL1992S2038.htm [21] 孟智勇, 徐祥德, 陈联寿.9406号台风与中纬度系统相互作用的中尺度特征.气象学报, 2002, 60(1):31-39. doi: 10.11676/qxxb2002.003 -
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