强热带风暴“莲花”(0903)非对称降水结构分析-海洋预报

强热带风暴“莲花”(0903)非对称降水结构分析

单位：1. 厦门市气象局, 福建, 厦门, 361012;
2. 四川省气候中心, 四川, 成都, 610072

分类号：论文

出版年·卷·期（页码）：2010·2010·第五期（64-71）

摘要：

利用雷达回波和NCEP分析资料,本文从水汽条件、环境风垂直切变和风暴移动状态等方面诊断分析了0903号强热带风暴"莲花"非对称降水结构形成的可能机制。结果表明:"莲花"南侧充足的水汽输送为强降水的发生提供了基本的水汽条件,同时水汽通量在水平空间上的非对称分布也在一定程度上导致了降水的非对称分布。环境风垂直切变是导致"莲花"降水结构改变并最终形成一波非对称降水结构的主要动力因子。随着垂直切变的增强,同时配合风暴南侧充足的水汽条件,一波非对称降水结构逐渐形成,在较强垂直切变长时间的作用下,强降水最终集中于顺切变方向左侧。在较强垂直切变的作用下,逆切变一侧的下沉运动抑制了陆地摩擦和地形抬升所形成的对流的发展。相对于较强的垂直切变而言,"莲花"相对稳定的移速和移向条件难以主导强热带风暴降水的空间分布。

Using radar reflectivity and NCEP analysis data,the possible mechanism to form asymmetric rainfall structure of Linfa was diagnosed and analyzed from water vapor condition,environmental vertical wind shear and storm moving aspects.The result demonstrated that the abundant water vapor transportation in south part of Linfa provided basic water vapor condition to the happening of heavy rainfall.The asymmetric water vapor flux distribution contributed to asymmetric rainfall in some degree.Environmental vertical wind shear was the major dynamic factor to lead to the change of rainfall structure and form wavenumber-1 asymmetric rainfall structure finally.As the shear enhanced,and with the abundant water vapor condition in south part of Linfa,wavenumber-1 asymmetric rainfall structure formed gradually.Then the heavy rainfall concentrated in downshear left ultimately as the longtime effect of strong shear.Under strong shear condition,the sink motion around upshear restrained the development of convection,which induced by the friction of land and uplift of terrain.Compared to strong shear,the relative stable moving speed and direction of storm was difficult to be the leading role to rainfall structure.

参考文献：

[1] 岳彩军,寿绍文,曾刚等."海棠"(Haitang)台风降水非对称分布成因初步研究[J].高原气象,2008,27(6):1333-1342.
[2] 岳彩军."海棠"台风降水非对称分布特征成因的定量分析[J].大气科学,2009,33(1):51-70.
[3] 吕梅,邹力,姚鸣明等.台风"艾利"降水的非对称结构分析[J].热带气象学报,2009,25(1):22-28.
[4] 石顺吉,余锦华,张大林.热带风暴Bilis(2006)登陆期间一波非对称降水分布成因的探讨[J].热带海洋学报,2009,28(1):34-42.
[5] Corbosiero K L,Molinari J.The effects of vertical wind shear on the distribution of convection in tropical cyciones[J].Mon Wea Rev,2002,130:2110-2123.
[6] Dunion J P,Velden C S.The impact of the Sahara air layer on Atlantic tropical cyclone activity[J].Bull Amer Meteor Soc,2004,85:353-365.
[7] Shapior L J.The asymmetric boundary layer flow under a translating hurricane[J].J Atmos Sci,1983,40:1984-1998.
[8] Chan J C L,Liu K S,Ching S E,et al.Asymmetric distribution of convection associated with tropical cyclones making landfall along the South China coast[J].Mo Wea Rev,2004,132:2410-2420.
[9] Rogers R,Chan S Y,Tenerelli J,et al.A numerical study of the impact of vertical shear on the distribution of rainfall in Hurricane Bonnie(1998)[J].Mon Wea Rev,2003,131:1577-1599.
[10] Chen S Y S,Knaff J A,Marks F D.Effect of vertical wind shear and storm motion on tropical cyclone rainfall asymmetries deduced from TRMM[J].Mon Wea Rev,2006,134:3190-3208.
[11] Braun S A,Wu L G.A numerical study of Hurricane Erin(2001).Part Ⅱ:Shear and the organization of eyewall vertical motion[J].Mon Wea Rev,2007,135:1179-1194.
[12] Kaplan J,Demaria M.Large-scale characteristics of rapidly intensifying tropical cyclones in the North Atlantic basin[J].Wea Forecasting,2003,18:1093-1108.
[13] Braun S A,Montgomery M T,Pu Z X.High-resolutin simulation of Hurricane Bonnie(1998).Part Ⅰ:The organization of eyewall vertical motion[J].J Atmos Sci,2006,63:19-42.
[14] Jones S C.The evolution of vortices in vertical shear.Ⅰ:Initially barotropic vortices[J].Quart J Roy Meteor Soc,1995,121:821-851.
[15] Frank W M,Ritchie E A.Effects of environmental flow upon tropical cyclone structure[J].Mon Wea Rev,1999,127:2044-2061.
[16] Zhang D L,Kieu C Q.Potential vorticity diagnosis of a simulated hurricane.Part Ⅱ:Quasi-balanced contributions to forced secondary circulations[J].J Atmos Sci,2006,63:2898-2914.
[17] Lonfat M,Rogers R,Marchok T,et al.A parametric model for predicting hurricane rainfall[J].Mon Wea Rev,2007,135:3086-3097.

服务与反馈：

【文章下载】【发表评论】【查看评论】【加入收藏】