高层动力强迫对回流型华南暖区暴雨影响的个例研究
|
摘要
应用NCEP再分析资料,分析了2014年5月8—9日发生在华南的一次暖区暴雨过程,研究高层动力强迫对此次华南暖区暴雨的影响。此次暴雨过程发生在暖湿的西南气流中,无明显天气尺度锋面系统影响,属于华南暖区暴雨过程。根据中尺度对流系统(MCS)的生消发展特征,可以将其分为5月8日与9日两个阶段,第一阶段具有显著的回流型暖区暴雨的特征,主要研究该阶段。研究发现,高PV扰动沿对流层高层南亚高压东北侧的西北气流下滑东移,导致IPV正异常,其东侧的辐散气流显著发展,在高层辐散气流的抽吸作用下,上升运动首先从中上层发展起来。在过程发展前期,IPV正异常主要是由平流作用引起,且在其东侧诱发出南风异常,进而导致辐散气流发展。当降水发生后,潜热加热反馈作用使高层辐散气流进一步加强,此时,辐散增强是对流发展的结果。此外,低层浅薄偏东风是本次暖区暴雨发生的低层背景场,其与西南风气流汇合,提供有利的低层辐合条件。
Using NCEP reanalysis data, the impacts of upper dynamics forcing on warm vector rainstorm over the south of China are studied via a case on 8—9 May 2014. Results show that the rainstorm occurred in warm and wet southwesterlies without an obviously synoptic scale front in lower troposphere and was a warm vector rainstorm. According to the characteristics of mesoscale convective systems(MCS), the rainstorm can be divided into two different stages(May 8 and May 9). The first stage can be classified into a returning type of warm vector rainstorm and is focused on in this paper. Study shows that the high PV disturbance moves southeastward and then eastward along the northwest side of a South Asia High, and leads to the positive anomalies of IPV. At the eastside of the anomalies the divergence develops significantly. Due to upper-level tropospheric pumping, ascending develops first in the middle and upper layer. In the initial stage of the rainstorm, positive anomalies of IPV are caused mainly by advection, and on its east side southerlies are induced and divergence develops. After the occurrence of precipitation, the feedback of latent heat released from the precipitation intensifies the upper-level divergence, which is the result of the development of convection. In addition, the easterlies in the lower layer provide the background for this warm vector rainstorm. It can supply the low-level favorable convergence when meeting with southwesterlies.
Using NCEP reanalysis data, the impacts of upper dynamics forcing on warm vector rainstorm over the south of China are studied via a case on 8—9 May 2014. Results show that the rainstorm occurred in warm and wet southwesterlies without an obviously synoptic scale front in lower troposphere and was a warm vector rainstorm. According to the characteristics of mesoscale convective systems(MCS), the rainstorm can be divided into two different stages(May 8 and May 9). The first stage can be classified into a returning type of warm vector rainstorm and is focused on in this paper. Study shows that the high PV disturbance moves southeastward and then eastward along the northwest side of a South Asia High, and leads to the positive anomalies of IPV. At the eastside of the anomalies the divergence develops significantly. Due to upper-level tropospheric pumping, ascending develops first in the middle and upper layer. In the initial stage of the rainstorm, positive anomalies of IPV are caused mainly by advection, and on its east side southerlies are induced and divergence develops. After the occurrence of precipitation, the feedback of latent heat released from the precipitation intensifies the upper-level divergence, which is the result of the development of convection. In addition, the easterlies in the lower layer provide the background for this warm vector rainstorm. It can supply the low-level favorable convergence when meeting with southwesterlies.
引文
[1] TAO S Y, CHEN L X. A review of recent research on the East Asian summer monsoon in China[M]. Monsoon Meteorology, Chang C P,Krishnamurti T N, Eds. London:Oxford University Press, 1987:60-92.
[2]李真光,梁必骐,包澄澜.华南前汛期暴雨的成因与预报问题[M]//华南前汛期暴雨文集.北京:气象出版社,1981.
[3]黄士松.华南前汛期暴雨[M].广州:广东科技出版社,1986:227-228.
[4]朱乾根,林锦瑞,寿绍文,等.天气学原理和方法[M].北京:气象出版社,1992.
[5]孙健,赵平,周秀骥.一次华南暴雨的中尺度结构及复杂地形的影响[J].气象学报,2002,60(3):333-342.
[6]李江南,蒙伟光,闫敬华,等.热带风暴Fitow(01140)暴雨的中尺度特征及成因分析[J].热带气象学报,2005,21(1):24-32.
[7]陶诗言.中国之暴雨[M].北京:科学出版社,1980.
[8]周秀骥,薛纪善,陶祖钰,等. 1998年华南暴雨科学试验研究[M].北京:气象出版社,2003.
[9]牛本璐,林万涛,张云.初始扰动对一次华南暴雨预报的影响的研究[J].大气科学,2009, 3(6):1 333-1 347.
[10]陈茂钦,徐海明.江淮锋面和华南暖区两次暴雨过程可预报性对比[J].南京信息工程大学学报自然科学版,2011, 3(2):118-127.
[11]张晓美,蒙伟光,张艳霞,等.华南暖区暴雨中尺度对流系统的分析[J].热带气象学报,2009, 25(5):551-560.
[12]夏如娣,赵思雄,孙建华.一类华南锋前暖区暴雨β中尺度系统环境特征的分析研究[J].大气科学,2006, 30(5):988-1 008.
[13]夏如娣,赵思雄. 2005年6月广东锋前暖区暴雨β中尺度系统特征的诊断与模拟研究[J].大气科学,2009, 33(3):468-488.
[14]徐燚,闫敬华,王谦谦,等.华南暖区暴雨的一种低层重力波触发机制[J].高原气象,2013, 32(4):1 051-1 061.
[15]闫敬华,郑彬,苏百兴.“5·17”梅州局地致洪大暴雨过程分析[C]//中国气象学会2004年年会论文集(下册).北京:气象出版社,2004.
[16]叶朗明,徐碧裕.两次不同类型暖区暴雨的对比分析[J].气象研究与应用,2014, 35(4):5-10.
[17] XIE P P, XIONG A Y. A conceptual model for constructing high-resolution gauge-satellite merged precipitation analyses[J]. J Geophys Res, 2011, 116, D21106, doi:10.1029/2011JD016118
[18]宇婧婧,沈艳,潘旸,等.中国区域逐日融合降水数据集与国际降水产品的对比评估[J].气象学报,2015, 73(2):394-410.
[19]林良勋,冯业荣,黄忠,等.广东省天气预报技术手册[M].北京:气象出版社,2006.
[20]叶朗明,苗峻峰.华南一次典型回流暖区暴雨过程的中尺度分析[J].暴雨灾害,2014, 33(4):342-350.
[21]于鑫,郑腾飞,黄健,等.一次华南海岸带暖区暴雨过程的观测分析[J].热带气象学报,2017, 33(1):134-144.
[22]林修栋,于超,张芳华,等. 2014年春末华南一次暖区暴雨的成因初探及数值预报检验[J].贵州气象,2016, 40(4):44-51.
[23] ERTEL H. Ein neuer hydrodynamische wirbdsatz[J]. Meteor Z Braunsch, 1942, 59:33-39.
[24] HOSKINS B J, MCLNTYRE M E, ROBERTSON A W. On the use and significance of isentropic potential vorticity maps[J]. Quart J Roy Metero Soc, 1985, 111(470):877-946.
[25] YANAI M, ESBENSEN S, CHU J H. determination of bulk properties of tropical cloud clusters from large-scale heat and moisture budgets[J]. J Atmos Sci, 1973, 30(4):611-627.
[26]刘屹岷,吴国雄,刘辉,等.空间非均匀加热对副热带高压形成和变异的影响Ⅲ:凝结潜热加热与南亚高压及西太平洋副高[J].气象学报,1999, 57(5):525-537.
[27]吴国雄,刘屹岷,刘平.空间非均匀加热对副热带高压带形成和变异的影响I:尺度分析[J].气象学报,1999, 57(3):257-263.
[28]吴国雄,刘屹岷.热力适应、过流、频散和副高I:热力适应和过流[J].大气科学,2000, 24(4):433-446.
[2]李真光,梁必骐,包澄澜.华南前汛期暴雨的成因与预报问题[M]//华南前汛期暴雨文集.北京:气象出版社,1981.
[3]黄士松.华南前汛期暴雨[M].广州:广东科技出版社,1986:227-228.
[4]朱乾根,林锦瑞,寿绍文,等.天气学原理和方法[M].北京:气象出版社,1992.
[5]孙健,赵平,周秀骥.一次华南暴雨的中尺度结构及复杂地形的影响[J].气象学报,2002,60(3):333-342.
[6]李江南,蒙伟光,闫敬华,等.热带风暴Fitow(01140)暴雨的中尺度特征及成因分析[J].热带气象学报,2005,21(1):24-32.
[7]陶诗言.中国之暴雨[M].北京:科学出版社,1980.
[8]周秀骥,薛纪善,陶祖钰,等. 1998年华南暴雨科学试验研究[M].北京:气象出版社,2003.
[9]牛本璐,林万涛,张云.初始扰动对一次华南暴雨预报的影响的研究[J].大气科学,2009, 3(6):1 333-1 347.
[10]陈茂钦,徐海明.江淮锋面和华南暖区两次暴雨过程可预报性对比[J].南京信息工程大学学报自然科学版,2011, 3(2):118-127.
[11]张晓美,蒙伟光,张艳霞,等.华南暖区暴雨中尺度对流系统的分析[J].热带气象学报,2009, 25(5):551-560.
[12]夏如娣,赵思雄,孙建华.一类华南锋前暖区暴雨β中尺度系统环境特征的分析研究[J].大气科学,2006, 30(5):988-1 008.
[13]夏如娣,赵思雄. 2005年6月广东锋前暖区暴雨β中尺度系统特征的诊断与模拟研究[J].大气科学,2009, 33(3):468-488.
[14]徐燚,闫敬华,王谦谦,等.华南暖区暴雨的一种低层重力波触发机制[J].高原气象,2013, 32(4):1 051-1 061.
[15]闫敬华,郑彬,苏百兴.“5·17”梅州局地致洪大暴雨过程分析[C]//中国气象学会2004年年会论文集(下册).北京:气象出版社,2004.
[16]叶朗明,徐碧裕.两次不同类型暖区暴雨的对比分析[J].气象研究与应用,2014, 35(4):5-10.
[17] XIE P P, XIONG A Y. A conceptual model for constructing high-resolution gauge-satellite merged precipitation analyses[J]. J Geophys Res, 2011, 116, D21106, doi:10.1029/2011JD016118
[18]宇婧婧,沈艳,潘旸,等.中国区域逐日融合降水数据集与国际降水产品的对比评估[J].气象学报,2015, 73(2):394-410.
[19]林良勋,冯业荣,黄忠,等.广东省天气预报技术手册[M].北京:气象出版社,2006.
[20]叶朗明,苗峻峰.华南一次典型回流暖区暴雨过程的中尺度分析[J].暴雨灾害,2014, 33(4):342-350.
[21]于鑫,郑腾飞,黄健,等.一次华南海岸带暖区暴雨过程的观测分析[J].热带气象学报,2017, 33(1):134-144.
[22]林修栋,于超,张芳华,等. 2014年春末华南一次暖区暴雨的成因初探及数值预报检验[J].贵州气象,2016, 40(4):44-51.
[23] ERTEL H. Ein neuer hydrodynamische wirbdsatz[J]. Meteor Z Braunsch, 1942, 59:33-39.
[24] HOSKINS B J, MCLNTYRE M E, ROBERTSON A W. On the use and significance of isentropic potential vorticity maps[J]. Quart J Roy Metero Soc, 1985, 111(470):877-946.
[25] YANAI M, ESBENSEN S, CHU J H. determination of bulk properties of tropical cloud clusters from large-scale heat and moisture budgets[J]. J Atmos Sci, 1973, 30(4):611-627.
[26]刘屹岷,吴国雄,刘辉,等.空间非均匀加热对副热带高压形成和变异的影响Ⅲ:凝结潜热加热与南亚高压及西太平洋副高[J].气象学报,1999, 57(5):525-537.
[27]吴国雄,刘屹岷,刘平.空间非均匀加热对副热带高压带形成和变异的影响I:尺度分析[J].气象学报,1999, 57(3):257-263.
[28]吴国雄,刘屹岷.热力适应、过流、频散和副高I:热力适应和过流[J].大气科学,2000, 24(4):433-446.
© 2004-2018 中国地质图书馆版权所有 京ICP备05064691号 京公网安备11010802017129号 地址：北京市海淀区学院路29号 邮编：100083 电话：办公室：(+86 10)66554848；文献借阅、咨询服务、科技查新：66554700 |