西北太平洋热带气旋快速增强阶段的风速分布特征

徐威; 周顺武; 葛旭阳; 马悦

doi:10.16032/j.issn.1004-4965.2017.02.012

西北太平洋热带气旋快速增强阶段的风速分布特征

doi: 10.16032/j.issn.1004-4965.2017.02.012

徐威¹,
周顺武^1, ,,
葛旭阳¹,
马悦^{1, 2}

1.
南京信息工程大学气象灾害教育部重点实验室/气象灾害预报预警与评估协同创新中心/气候与环境变化国际合作联合实验室，江苏南京 210044
2.
上海市气候中心，上海 200030

基金项目:

国家自然科学基金项目 41575056

国家重点基础研究发展规划项目 2015CB452803

中国气象局公益性行业科研专项 GYHY201506007

详细信息

通讯作者:
周顺武，男，四川省人，教授，博士，研究方向：季风动力学研究。E-mail: zhou@nuist.edu.cn

中图分类号: P444
计量
- 文章访问数: 1117
- HTML全文浏览量: 36
- PDF下载量: 683
- 被引次数: 0
出版历程
- 收稿日期: 2015-10-29
- 修回日期: 2016-11-16
- 刊出日期: 2017-04-01

Wind Speed Distribution Features of Rapidly Intensifying Tropical Cyclones in Northwest Pacific

Wei XU¹,
Shun-wu ZHPU^{1
, ,},
Xu-yang GE¹,
Yue MA^{1, 2}

1.
Key Laboratory of Meteorological Disaster, Ministry of Education (KLME), Joint International Research Laboratory of Climate and Environment Change (ILCEC), Collaborative Innovation Center on Forecast and Evaluation of Meteorological Disasters (CIC-FEMD), Nanjing University of Information Science & Technology, Nanjing 210044, China
2.
Shanghai Climate Center, Shanghai 200030, China

摘要

摘要: 利用联合台风预警中心的最优路径（best-track）资料，筛选出西北太平洋地区快速增强和非快速增强两类热带气旋样本。利用美国国家海洋与大气管理局（NOAA）的多平台热带气旋表面风分析资料，对比分析了两类样本的风速和涡度的分布特征。结果显示，快速增强的热带气旋样本通常结构更紧凑，最大风速较大，最大风速半径较小，台风内区的风速较大。在涡度上表现为快速增强热带气旋样本内区的涡度和涡度梯度较大。对两类样本进行t检验，结果显示两类样本内区的切向风差异明显，说明热带气旋的内区风速分布与其发展之间存在密切联系。其物理机制可能是：当存在较大的内区涡度梯度时，涡度隔离机制有利于对流单体向涡旋中心汇聚，此外较大的涡度意味着较大的惯性稳定度，有利于非绝热加热向热带气旋动能的转换，二者共同作用有利于热带气旋的快速发展。
- 热带气旋 /
- 风速分布 /
- 快速增强
Abstract: Two categories of tropical cyclone (TC) cases, rapidly intensifying (RI) and non-rapidly intensifying (non-RI) TC cases, are selected according to best-track data from Joint Typhoon Warning Center. Then by using Multiplatform Tropical Cyclone Surface Wind Analysis (MTCSWA) data, different wind speed distribution features and vorticity structure features between RI and non-RI TC cases in the northwest Pacific are analyzed. It is found that there exist significant differences in the TC inner-core structure, Thelarger the compact of TC is, the faster the intensification rate will be. Specifically, the TCs with stronger inner-core vorticity and larger vorticity gradient are more likely to develop rapidly. It is speculated that the larger vorticity gradient of RI cases accelerates convective bursts near the TC to merge through vorticity segregation processes. Meanwhile, greater vorticity implies greater inertial stability, which is helpful for diabatic heating to convert to kinetic energy of TCs. Both of these two factors are conducive to TC development.
- tropical cyclone /
- wind speed distribution /
- rapid intensification

HTML全文

图 1 台风“莫拉克”表面风场（2009年8月5日12时）

等值线为全风速，单位：knot。

下载: 全尺寸图片幻灯片

图 2 台风“莫拉克”方位角平均的表面切向风

（2009年8月5日12时）横坐标为离台风中心距离，即半径，单位：km；纵坐标为切向风速，单位：knot。

下载: 全尺寸图片幻灯片

图 3 快速增强样本（虚线）和非快速增强样本（实线）平均最大风速演变

单位：knot。

下载: 全尺寸图片幻灯片

图 4 快速增强样本（三角）和非快速增强样本（圆点）的S参数和24 h风速变化（dV）分布

横坐标为S参数值；纵坐标为24 h风速变化，单位：knot。

下载: 全尺寸图片幻灯片

图 5 快速增强样本（虚线）和非快速增强样本（实线）方位角平均的表面切向风分布

横坐标为离台风中心距离，即半径，单位：km；纵坐标为切向风速，单位：knot。

下载: 全尺寸图片幻灯片

图 6 快速增强样本和非快速增强样本的切向风速t检验分布横坐标为半径，单位：km；长虚线为显著性水平α=0.05的t检验临界值。

下载: 全尺寸图片幻灯片

图 7 快速增强样本（虚线）和非快速增强样本（实线）方位角平均的相对涡度分布特征

横坐标为半径，单位：km；纵坐标为相对涡度，单位：1×10^-4 s^-1。

下载: 全尺寸图片幻灯片

参考文献(29)

[1]	HARNOS D S, S W NESBITT. Convective structure in rapidly intensifying tropical 485 cyclones as depicted by passive microwave measurements[J]. Geophys Res Lett, 2011, 38(7): 1-5.
[2]	RAPPAPORT E N, FRANKLIN JL, AVILA LA, et al. Advances and challenges at the national hurricane center[J]. Wea Forec, 2009, 24(2): 305-419.
[3]	陈联寿.热带气旋研究和业务预报技术的发展[J].应用气象学报, 2006, 17(6): 672-681.
[4]	EMANUEL K. An air-sea interaction theory for tropical cyclones, Part Ⅰ: Steady-state maintenance[J]. J Atmos Sci, 1985, 43(6): 585-604.
[5]	郑静, 费建芳, 蒋国荣, 等.海气相互作用对热带气旋发生发展影响研究综述[J].海洋预报, 2008, 25(1): 56-64.
[6]	蒋小平, 刘春霞, 莫海涛, 等.海气相互作用对台风结构的影响[J].热带气象学报, 2010, 26(1): 55-59.
[7]	BLACK M L, J F GAMACHE, F D MARKS JR, et al. Eastern Pacific Hurricanes Jimena of 1991 and Olivia of 1994: The effect of vertical shear on structure and intensity[J]. Mon Wea Rev, 2002, 130(9): 2291-2312.
[8]	余晖, 费亮, 端义宏. 8807和0008登陆前的大尺度环境特征与强度变化[J].气象学报, 2002, 60(增刊): 78-87.
[9]	丁治英, 邢蕊, 徐海明, 等.南亚高压南部环境位涡对台风加强的影响分析[J].热带气象学报, 2012, 28(5): 675-686.
[10]	端义宏, 秦增灏, 顾建峰.海温变化对热带气旋强度影响的数值实验 (Ⅰ)——热带气旋强度的数值模拟和海温实验[M]//台风科学、业务实验和天气动力学理论的研究第三分册.北京:北京气象出版社, 1996: 129-134.
[11]	CIONE, JOSEPH J, EVAN A KALINA, et al. Observations of air-sea interaction and intensity change in hurricanes[J]. Mon Wea Rev, 2013, 141(7): 2368-2382.
[12]	HILL K A, KEVIN A, LACKMANN G M. Influence of environmental humidity on tropical cyclone size[J]. Mon Wea Rev, 2009, 137(10): 3294-3315.
[13]	于玉斌, 赵大军, 陈联寿.干冷空气活动对超强台风"桑美"(2006) 近海突然增强影响的数值模拟研究[J].热带气象学报, 2015, 31(1): 21-31.
[14]	KAPLAN J, M DEMARIA, J KNAFF. A revised tropical cyclone rapid intensification index for the Atlantic and eastern North Pacific basins[J]. Wea Forec, 2010, 25(1): 220-241.
[15]	WANG B, X ZHOU. Climate variation and prediction of rapid intensification in tropical cyclones in the western North Pacific[J]. Meteorol Atmos Phy, 2008, 99(1): 1-16.
[16]	HENDRICKS E A, M S PENG, FU B, et al. Quantifying environmental control on tropical cyclone intensity change[J]. Mon Wea Rev, 2010, 138(8): 3243-3271.
[17]	HENDRICKS E A, MONTGOMERY M T, DAVIS C A. The role of vortical hot towers in the formation of Tropical Cyclone Diana (1984)[J]. J AtmosSci, 2004, 61(11): 1209-1232.
[18]	MONTGOMERY M T, NICHOLLS M E, CRAM T A, et al. A vortical hot tower route to tropical cyclogenesis[J]. J Atmos Sci, 2006, 63(1): 355-386.
[19]	BRAUN S A, MONTGOMERY M T, PU Z. High-resolution simulation of Hurricane Bonnie (1998), Part Ⅰ: The organization of eyewall vertical motion[J]. J AtmosSci, 2006, 63(1): 19-42.
[20]	Ge X Y, XUW, ZHOUS W. Sensitivity of tropical cyclone intensification to inner-core structure[J]. Adv Atmos Sci, 2015, 32(10): 1407-1418.
[21]	FANG J, ZHANGF Q. Evolution of multi-scale vortices in the development of Hurricane Dolly (2008)[J]. J Atmos Sci, 2011, 68(1): 103-122.
[22]	GROSS J M. North Atlantic and East Pacific track and intensity verification for 2000[C]//Minutes of the 55th Interdepartmental Hurricane Conference, Miami, FL, Office of the Federal Coordinator for Meteorological Services and Supporting Research, NOAA, 2001: B12-B15.
[23]	DEMARIA M, ZEHR R M, KOSSIN J P, et al. The use of GOES imagery in statistical hurricane intensity prediction[C]//25th Conference on Hurricanes and Tropical Meteorology. San Diego: American Meteorological Society, 2002: 120-121.
[24]	ROGERS R, REASOR P, LORSOLO S. Airborne Doppler observations of the inner-core structural differences between intensifying and steady-state tropical cyclones[J]. Mon Wea Rev, 2013, 141(9): 2970-2991.
[25]	CHEN D Y, CHEUNG K K W, LEE C S. Some implication of core regime wind structures in western North Pacific tropical cyclones[J]. Wea Forec, 2011, 26(1): 61-75.
[26]	CARRASCO C, LANDSEAC, LIN Y. The influence of tropical cyclone size on its intensification[J]. Wea Forec, 2014, 29(3): 582-590.
[27]	XU J, WANG Y. Sensitivity of the simulated tropical cyclone inner-core size to the initial vortex size[J]. Mon Wea Rev, 2010, 138(11): 4135-4157.
[28]	KNAFF J A, DEMARIAM, MOLENAR D A. An automated, objective, multiple-satellite-platform tropical cyclone surface wind analysis[J]. J Appl Meteor Climatol, 2011, 50(10): 2149-2166.
[29]	SCHECTER D A, DUBIN D H E. Vortex motion driven by a background vorticity gradient[J]. Phy Rev Lett, 1999, 83(11): 2191-2194.