暴雨过程中逆风区特征及应用判据研究
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摘要
为研究暴雨过程中逆风区特征及应用判据,统计分析2010—2017年山东临沂地区暴雨过程中的多普勒雷达观测资料,结果表明:暴雨过程中,风暴内的垂直环流是造成逆风区发生发展的直接原因;逆风区表现为β中尺度和γ中尺度,其形态在不同天气类型下有明显差异;逆风区持续阶段降水强度增大,持续时间与过程累积雨量呈正相关;当雷达最低仰角识别到逆风区,其厚度≥4. 0 km、强度≥15 m·s~(-1)、径向速度绝对值最大值≥5 m·s-1且持续30 min以上时,风暴常明显发展,相关特征可用于预报风暴和暴雨的发展。
The Doppler radar data of torrential rainfall processes in Linyi,Shandong from 2010 to 2017 are statistically analyzed to study the characteristics and its application criteria of adverse wind areas during these processes. Results reveal that: 1) the occurrence and development of adverse wind areas are direct results of the vertical circulations inside the storms during the torrential rainfall processes; 2) the adverse wind areas present meso-γ and meso-β scales with different shapes in different weather types;3) the precipitation intensity tends to increase while the adverse wind areas persistently exist,and the duration of the adverse wind is positively correlated to the accumulated precipitation; 4) when the radar identifies the adverse wind area at the lowest elevation angle with the thickness equal to or greater than 4. 0 km,the intensity equal to or greater than 15 m · s-1,the absolute value of the maximum radial velocity equal to or greater than 5 m·s~(-1),and the duration above 30 minutes,the storm generally significantly develops. Relevant characteristics can be reference in forecasting storms and torrential rainfall processes.
The Doppler radar data of torrential rainfall processes in Linyi,Shandong from 2010 to 2017 are statistically analyzed to study the characteristics and its application criteria of adverse wind areas during these processes. Results reveal that: 1) the occurrence and development of adverse wind areas are direct results of the vertical circulations inside the storms during the torrential rainfall processes; 2) the adverse wind areas present meso-γ and meso-β scales with different shapes in different weather types;3) the precipitation intensity tends to increase while the adverse wind areas persistently exist,and the duration of the adverse wind is positively correlated to the accumulated precipitation; 4) when the radar identifies the adverse wind area at the lowest elevation angle with the thickness equal to or greater than 4. 0 km,the intensity equal to or greater than 15 m · s-1,the absolute value of the maximum radial velocity equal to or greater than 5 m·s~(-1),and the duration above 30 minutes,the storm generally significantly develops. Relevant characteristics can be reference in forecasting storms and torrential rainfall processes.
引文
[1]朱乾根,林锦瑞,寿绍文,等.天气学原理与方法[M].4版.北京:气象出版社,2007:328-393.
[2]愈小鼎,姚秀萍,熊廷南,等.多普勒天气雷达原理与业务应用[M],北京:气象出版社,2006:82-129.
[3]张沛源,余志敏,王慕维,等.多普勒天气雷达资料在强天气短时预报中的应用[C]//第十一届亚运会气象保障研究论文集.北京:气象出版社,1992:68-74.
[4]张沛源,陈荣林.多普勒速度图上的暴雨判据研究[J].应用气象学报,1995,6(3):373-378.
[5]段丽,卞素芬,俞小鼎,等.用SA雷达产品对京西三次局地暴雨落区形成的精细分析[J].气象,2009,35(3):21-28.
[6]徐芬,王博妮,夏文梅,等.长江中下游地区一次春季暴雨过程的多普勒雷达速度特征分析与研究[J].高原气象,2014,33(2):548-556.
[7]冯晋勤,汤达章,曹长尧.福建西部山区短时暴雨雷达回波特征及中小尺度系统分析[J].气象,2014,40(3):297-304.
[8]胡明宝,高太长,汤达章.多普勒天气雷达资料分析与应用[M].北京:解放军出版社,2000:113-116.
[9]李军霞,汤达章,李培仁,等.中小尺度的多普勒径向速度场特征分析[J].气象科学,2007,27(5):557-563.
[10]李柏,古庆同,李瑞义,等.新一代天气雷达灾害性天气监测能力分析及未来发展[J].气象,2013,39(3):265-280.
[11]王丽荣,胡志群,汤达章,等.多普勒雷达径向速度资料在对流天气预报中的应用[J].气象科学,2007,27(6):695-701.
[12]STENSRUD D J,BAO J W,WARNER T T.Using initial condition and model physics perturbations in short-range ensemble simulations of mesoscale convective systems[J].Mon Wea Rev,2000,128(7):2077-2107.
[13]陶岚.多普勒天气雷达中的中尺度气旋识别[D].南京:南京信息工程大学,2006.
[14]胡大海.基于多普勒雷达径向速度图的风暴信息提取[D].天津:天津大学,2010.
[15]陈鲍发,魏鸣,柳守煜.逆风区的回波演变与强对流天气的结构分析[J].暴雨灾害,2008,27(2):127-134.
[16]赵海军.晴空回波特征与风场信息应用[J].气象科技,2017,45(3):477-484.
[17]伍志方,叶爱芬,胡胜,等.中小尺度天气系统的多普勒统计特征[J].热带气象学报,2004,20(4):391-400.
[18]王啸华,郑媛媛,徐芬,等.2011年江苏南部两场大暴雨对比分析[J].气象科学,2015,35(4):497-505.
[19]DAVIS R S.Flash flood forecast and detection methods[J].Meteor Monogr,2001,28(50):481-526.
[20]王宝鉴,黄玉霞,魏栋,等.TRMM卫星对青藏高原东坡一次大暴雨强降水结构的研究[J].气象学报,2017,75(6):966-980.
[21]杨晓霞,高留喜,宋佳嘉,等.山东夏季强降水的影响系统和物理量特征[J].海洋气象学报,2018,38(3):57-66.
[2]愈小鼎,姚秀萍,熊廷南,等.多普勒天气雷达原理与业务应用[M],北京:气象出版社,2006:82-129.
[3]张沛源,余志敏,王慕维,等.多普勒天气雷达资料在强天气短时预报中的应用[C]//第十一届亚运会气象保障研究论文集.北京:气象出版社,1992:68-74.
[4]张沛源,陈荣林.多普勒速度图上的暴雨判据研究[J].应用气象学报,1995,6(3):373-378.
[5]段丽,卞素芬,俞小鼎,等.用SA雷达产品对京西三次局地暴雨落区形成的精细分析[J].气象,2009,35(3):21-28.
[6]徐芬,王博妮,夏文梅,等.长江中下游地区一次春季暴雨过程的多普勒雷达速度特征分析与研究[J].高原气象,2014,33(2):548-556.
[7]冯晋勤,汤达章,曹长尧.福建西部山区短时暴雨雷达回波特征及中小尺度系统分析[J].气象,2014,40(3):297-304.
[8]胡明宝,高太长,汤达章.多普勒天气雷达资料分析与应用[M].北京:解放军出版社,2000:113-116.
[9]李军霞,汤达章,李培仁,等.中小尺度的多普勒径向速度场特征分析[J].气象科学,2007,27(5):557-563.
[10]李柏,古庆同,李瑞义,等.新一代天气雷达灾害性天气监测能力分析及未来发展[J].气象,2013,39(3):265-280.
[11]王丽荣,胡志群,汤达章,等.多普勒雷达径向速度资料在对流天气预报中的应用[J].气象科学,2007,27(6):695-701.
[12]STENSRUD D J,BAO J W,WARNER T T.Using initial condition and model physics perturbations in short-range ensemble simulations of mesoscale convective systems[J].Mon Wea Rev,2000,128(7):2077-2107.
[13]陶岚.多普勒天气雷达中的中尺度气旋识别[D].南京:南京信息工程大学,2006.
[14]胡大海.基于多普勒雷达径向速度图的风暴信息提取[D].天津:天津大学,2010.
[15]陈鲍发,魏鸣,柳守煜.逆风区的回波演变与强对流天气的结构分析[J].暴雨灾害,2008,27(2):127-134.
[16]赵海军.晴空回波特征与风场信息应用[J].气象科技,2017,45(3):477-484.
[17]伍志方,叶爱芬,胡胜,等.中小尺度天气系统的多普勒统计特征[J].热带气象学报,2004,20(4):391-400.
[18]王啸华,郑媛媛,徐芬,等.2011年江苏南部两场大暴雨对比分析[J].气象科学,2015,35(4):497-505.
[19]DAVIS R S.Flash flood forecast and detection methods[J].Meteor Monogr,2001,28(50):481-526.
[20]王宝鉴,黄玉霞,魏栋,等.TRMM卫星对青藏高原东坡一次大暴雨强降水结构的研究[J].气象学报,2017,75(6):966-980.
[21]杨晓霞,高留喜,宋佳嘉,等.山东夏季强降水的影响系统和物理量特征[J].海洋气象学报,2018,38(3):57-66.