1998年7月河套气旋强烈发展时的暴雨过程分析

梁丰; 陶诗言

1998年7月河套气旋强烈发展时的暴雨过程分析

梁丰^1,2,
陶诗言¹

1.
中国科学院大气物理研究所, 北京 100029
2.
北京市气象局, 北京 100089

资助项目:

国家自然科学基金课题“干旱背景下黄河流域致洪暴雨的多尺度天气学模型研究” ZR2006-03

北京市科委项目“北京奥运会国际天气预报示范计划支持技术研究” Z0006279040191

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出版历程
- 收稿日期: 2006-06-02
- 修回日期: 2007-01-05
- 刊出日期: 2007-10-31

Diagnosis of a Heavy Rain Event Caused by the Intense Development of Yellow River Cyclone in July, 1998

Liang Feng^1,2,
Tao Shiyan¹

1.
Institute of Atmospheric Physics, Chinese Academy of Sciences, Beijing 100029
2.
Beijing Meteorological Bureau, Beijing 100089

摘要

摘要: 采用位涡理论对1998年7月4—7日的一次河套气旋强烈发展中的暴雨过程进行分析。结果表明：此次夏季河套气旋的强烈发展是在高层正位涡平流和低层暖平流的共同作用下产生的。高空双急流结构产生的强烈辐散加强了低层辐合，有利于气旋的加强。强降水出现在河套气旋强烈发展过程中，是由高层冷空气与季风涌带来的西南暖湿气流辐合而引起的大尺度降水过程。在这次气旋强烈发展过程中，对流层低层到中上层均出现强的上升气流，使得南方深厚的暖湿空气不断随西南风流入暴雨区上空。暴雨发生时，华北地区处于地面Ω型的θ_se高能舌之中，其上空500 hPa存在一个由大尺度动力强迫形成的东北—西南向的非地转湿 Q 矢量辐合带，对流云带与 Q 矢量辐合中心有非常好的对应关系。
- 河套气旋;
- 位涡;
- 非地转湿Q矢量;
- 暴雨
Abstract: A Yellow River cyclone intensifies rapidly during July 5 to 7, 1998. Its center pressure decreases by 12 hPa over a 24 h period and it produces heavy rain with the maximum rainfall exceeding 350 mm in Beijing. A diagnostic study is conducted from a potential vorticity or "PV thinking" perspective using NCAR/NCEP 6 hourly reanalysis data. The results show that the rapid development of the Yellow River Cyclone is related to the coupling between a surface low system and an upper level positive PV anomaly. When the positive PV anomaly near the tropopause advects over a pre existing surface cyclone, the cyclone deepens dramatically. Warm advection at 850 hPa intensifies the development of cyclone. Heavy rain occurs in the rapid intensification stage of the Yellow River Cyclone. This is a synoptic scale precipitation case, which is caused by the convergence between cold air descending from stratosphere and southwest warm and moisture air flow brought by the Monsoon Surge. On the vertical cross section through the region of heavy rain, abrupt jump of tropopause is shown clearly. The tropopause is near 250 hPa on the cold side and rises dramatically to above 100 hPa on the warm side. The extent of the descent of stratospheric air in the storm can be deduced by the tongue of 1 PVU extending from 200 to 600 hPa.While the cyclone intensifies rapidly, there are strong ascending motions, which lead to the deep moisture air from the south of China transporting to the heavy rain region continually by southwest wind. From the low to mid level of trop osphere, the humidity increases. The amount of precipitable water vapor increases 10.2 mm in 24 hours. The atmosphere is baroclinic over heavy rain region. High level jet with wind speed greater than 30 m·s^-1 and low level jet with wind speed greater than 12 m·s^-1 are found at 200 hPa and 850 hPa, respectively. At surface, a tongue of high θ_se value prevails in North China. At 500 hPa, there is a convergent zone of non geostrophic wet Q vector extending from southwest to northeast, which is caused by the large scale force. The convective cloud bands have a good relationship with the convergent center of Q vector. In the convergence zone, a number of MCSs continuously move to North China alone the southwest wind on the northwest side of the Subtropical High and cause amount of rainfall. It is called "train effect". Furthermore, topography influences the location of heavy rain. East wind prevails at surface over Beijing area when rainfall occurs. The west mountain blocks and lifts the east flow and increases the precipitation on upstream side of the mountain. The maximum precipitation centers occur at Changping, Yanqing.
- Yellow River cyclone;
- potential vorticity;
- non geostrophic wet Q vector;
- heavy rain

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图 1 1998年6月16日—7月16日华北地区主要降水过程与天气系统配置

(a)沿37.5°~42.5°N平均的500 hPa正相对涡度(单位:10^-6s^-1)的纬向-时间剖面,(b)(d)(f)华北地区35站平均的逐日降水量R,(c)110°~120°E平均的200 hPa西风分量的时间-经向剖面(长虚线为气候平均的20 m·s^-1风速线) (e)110°~120°E整层(地面~300 hPa)水汽通量平均(箭头, 单位:kg·m ^-1·s^-1)和T_BB≤0 ℃的区域(阴影区), (g)30°~32°N平均的向外长波辐射距平≤-15 W·m ^-2的区域(实线)与500 hPa位势高度

Fig. 1 The main rainfalls in Huabei and the corresponding circulation pattern from June 16 to July 16, 1998

(a)zone-time section of 500 hP a positive relative vo rticity averaged within 37.5°—42.5°N,(b)(d)(f)averaging daily precipitation of 35 stations in Huabei,(c)time-meridian section of 200 hPa west wind, averaged within 110°—120°E(dashed lines denote isobaths of west wind with value of 20 m·s ^-1 in climate),(e)integrated water vapor flux from surface to 300 hPa averaged within 110°—120°E(arrow, unit:kg·m^-1·s^-1, regions with T_BB≤0℃ are shaded),(g)zone-time section of averaged OLRA within 30°—32°N(solid lines)and 500 hPa geopotential height(shaded from light to dark denote 586, 588, 592 dagpm, dashed line denotes 586 dagpm contour in climate)

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图 2 1998年θ=350 K等熵面的位涡分布(单位:10^-6 km²·kg^-1·s^-1)

(a)7月5日00:00,(b)7月5日12:00,(c)7月6日00:00,(d)7月7日00:00

Fig. 2 Potential vorticity(unit :10^-6 km²·kg^-1·s^-1)on the 350 Kisentropic surface at(a)00 :00 on July 5, 1998,(b)12 :00 on July 5, 1998,(c)00 :00 on July 6, 1998,(d)00 :00 on July 7, 1998

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图 3 1998年7月5日12 :00沿图 2b中A—B线的剖面图

(a)位涡(单位:PVU),(b)等风速线(实线, 单位:m·s^-1)及风矢量(垂直速度×100)和位温(虚线, 单位:K)

Fig. 3 Vertical section along A—B line in Fig.2b at 12:00 on July 5

(a)potential vorticity(unit :PVU), (b)wind speed(solid line, unit:m·s^-1)with wind vector and potential temperature(dashed line, unit:K)

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图 4 1998年7月5日12 :00(a)350 K等熵面位涡(实线, 仅绘出1~4 PVU)和850 hPa暖平流区(阴影区, 单位:10^-5K·s^-1)(b)GMS红外云顶亮温(阴影区, 单位:℃, 虚线为T_BB=-12℃)

Fig. 4 350 K PV(solid line, with contour from 1—4 PVU)and 850 hPa warm advection region(shaded areas, unit :10 ^-5K·s^-1)(a)and T_BB retrieved from GMS data(shaded areas, unit :℃; dashed line denotes-12℃)(b)at 12:00 on July 5, 1998

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图 5 1998年7月4—7日θ=310 K等熵面天气形势分布

(实线为等压线, 单位:hPa; 虚线为等比湿线, 单位:g·kg^-1, 阴影区为比湿大于10 g·kg^-1的区域) (a)7月4日00 :00,(b)7月5日12 :00,(c)7月6日00 :00,(d)7月7日00 :00

Fig. 5 Isobars(solid line, unit :hPa)and mix ratio contours(dashed line, unit:g·kg^-1)at 310 K isentropic surfaces for July 4—7, 1998(region with mix ratio value greater than 10 g/kg are shaded) (a)00 :00 on July 4,(b)12:00 on July 5,(c)00 :00 on July 6,(d)00:00 on July 7

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图 6 同图 5, 但为θ=330 K等熵面

(阴影区为比湿大于4 g·kg^-1的区域)

Fig. 6 Same as in Fig.5, but for 330 Kisentropic surface

(regions with mix ratio values greater than 4 g·kg^-1 are shaded)

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图 7 1998年7月5日12 :00暴雨区天气系统配置

(a)500 hPa位势高度(>586 dagpm, 实线)、200 hPa风速(>30 m·s^-1, 风向杆)、850 hPa水汽通量矢量(>0.15 m·s^-1, 箭头)和850 hPa比湿(>12 g·kg^-1, 阴影区), (b)地面θ_se(>335 K, 实线)、500 hPa Q矢量(箭头)及∇·Q(低于-0.5×10^-15 m·kg^-1·s^-1, 阴影区)

Fig. 7 Synoptic pattern of heavy rain region for 12:00 on July 5, 1998

(a)500 hPa height(with values greater than 586 dagpm, solid line), 200 hPa wind(with speed greater than 30 m·s ^-1, wind bar), 850 hPa water vapor flux(with values greater than 0.15 m·s^-1, arrow)and 850 hPa mix ratio(with greater than 12 g·kg^-1, shaded), (b)surface θ_se(with values greater than 335 K, solid line), 500 hPa Q vector(arrows)and Q vector divergence(values less than-0.5×10^-15 m·kg^-1·s^-1, shaded)

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