夏季青藏高原深厚及浅薄降水云气候特征分析

潘晓; 傅云飞

doi:10.7522/j.issn.1000-0534.2014.00112

高原气象 >

2015 , Vol. 34 >Issue 5: 1191 - 1203

DOI: https://doi.org/10.7522/j.issn.1000-0534.2014.00112

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夏季青藏高原深厚及浅薄降水云气候特征分析

潘晓 ,
傅云飞

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中国科学技术大学地球和空间科学学院, 合肥 230026

收稿日期: 2014-03-13

网络出版日期: 2015-10-28

基金资助

国家公益性行业支撑项目(GYHY201306077);国家自然科学基金项目(41230419,91337213);中国科学院战略先导科技专项(XDA05100303)

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Analysis on Climatological Characteristics of Deep and Shallow Precipitation Cloud in Summer over Qinghai-Xizang Plateau

PAN Xiao ,
FU Yunfei

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School of Earth and Space Sciences, University of Scienceand Technology of China, Hefei 230026, China

Received date: 2014-03-13

Online published: 2015-10-28

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摘要

利用1998-2007年热带测雨卫星TRMM搭载的测雨雷达PR和可见光/红外扫描仪VIRS的融合资料,研究了夏季青藏高原深厚降水(深厚强对流和深厚弱对流)及浅薄降水的水平分布、垂直结构及红外信号特征,并对其日变化特点和降水的经向移动特征进行了分析。结果表明,夏季高原降水主要以深厚弱对流降水为主(67.8%),浅薄降水次之(26.4%),深厚强对流降水出现最少(5.8%)。不同云顶红外辐射温度的平均降水廓线表明,深厚降水从雨顶高度至近地面高度均经历先增大后减小的过程,而浅薄降水只有增大过程。深厚强对流和深厚弱对流的降水频次峰值均出现在16:00(地方时,下同),降水强度峰值分别出现在18:00和13:00,其中深厚强对流降水强度在00:00还出现次峰值。浅薄降水的降水频次及强度峰值均出现在20:00,呈现夜雨特点。深厚降水和浅薄降水的云顶红外辐射温度日变化特征相似,最低值均出现在19:00。深厚强对流和深厚弱对流降水具有明显的东移特征,其中深厚弱对流降水的东移特征更为明显,而浅薄降水无明显的经向传播特征。

关键词： 青藏高原; 降水云; 红外辐射温度; 气候特征; 日变化

本文引用格式

潘晓 , 傅云飞 . 夏季青藏高原深厚及浅薄降水云气候特征分析[J]. 高原气象, 2015 , 34(5) : 1191 -1203 . DOI: 10.7522/j.issn.1000-0534.2014.00112

Abstract

Climatological characteristics of the deep (strong deep convection and weak deep convection), shallow precipitat ionincluding their horizontal distribution, vertical structures, infrared signal characteristics, the diurnal variation and meridional movement of the precipitation mentioned above in the Plateau (QX) are investigated based on combining measurements of the tropical rainfall measuring mission (TRMM) precipitation radar (PR) and visible and infrared scanner (VIRS) from 1998 to 2007.The results show that the precipitation over QX is mainly in the form of week deep convection, which occupies 67.8% followed by the form of shallow precipitation with 26.4% and the strong deep convection with 5.8%.The average rain rates of deep precipitation for different cloud infrared radiant temperature all experience an increasing-reducing process from the storm top altitude to the ground level, while the shallow precipitation only has anincreasing process.Both the precipitation frequency peaks forstrong deep convection and weak deep convection appear at 16:00(local time, hereafter the same).While the precipitation intensities of which reach their peak at 13:00 and 18:00, respectively.Moreover, the strong deep convection has a secondary peak at 00:00.For the shallow precipitation, the precipitation frequency and intensity peaks both appear at 20:00, having the characteristicof night rain.The diurnal variation curves of radiant temperatureof deep and shallow precipitation are similar to each other, as a result, their minimaappear around 19:00.It is obvious that the strong deep convection and weak deep convection have the characteristics of eastward movement, and the week deep convection is more obvious.The shallow precipitation don' t have significant meridional propagation characteristics.

Key words： The Qinghai-Xizang P; Precipitation cloud; Infrared radiation t; Climatological chara; Diurnal variation

参考文献

[1]Wetherald R T,Manabe S.Cloud feedback processes in a general circulation model[J].J Atmos Sci,1988,45(8):1397-1416.
[2]游景炎,段英,游来光.云降水物理和人工增雨技朮研究[M].北京:气象出版社,1994:89-100.
[3]Freud E,Rosenfeld D,Andreae M O,et al.Robust relationsbetween CCN and the vertical evolution of clouddrop size distribution in deep convect ive clouds[J].Atmos Chem Phys,2008,8(6):1661-1675.
[4]尚博,周毓荃,刘建朝,等.基于Cloudsat的降水云和非降水云垂直特征[J].应用气象学报,2012,23(1):1-9.
[5]刘健.利用卫星数据分析青藏高原云微物理特性[J].高原气象,2013,32(1):38-45,doi:doi:10.7522/j.issn.1000-0534.2013.00005.
[6]叶笃正,张捷迁.青藏高原加热作用对夏季东亚大气环流影响的初步模拟实验[J].中国科学,1974,8(1):301-320.
[7]罗会邦,陈蓉.夏半年青藏高原东部大气热源异常对环流和降水的影响[J].气象科学,1995,15(4):95-102.
[8]李跃清.青藏高原地面加热及上空环流场与东侧旱涝预测的关系[J].大气科学,2003,27(1):107-114.
[9]毛江玉,吴国雄.青藏高原热状况和海温异常对亚洲季风季节转换年际变化的影响[J].地球物理学报,2006,49(5):1279-1287.
[10]王同美,吴国雄,万日金.青藏高原的热力和动力作用对亚洲季风区环流的影响[J].高原气象,2008,27(1):1-9.
[11]Zhong L,Su Z,Ma Y,et al.Accelerated changes of environmental conditions on the Tibetan Plateau caused by climate change[J].J Climate,2011,24(24):6540-6550.
[12]Zhong L,Ma Y,Ma W,et al.Remote sensing of land surface parameters in the middle reaches of Yarlung Zangbo River and its two tributaries from AVHRR and MODIS data[J].J Meteor Soc Japan,2012,90:75-86,doi:10.2151/jmsj.2012-C05.
[13]郁淑华,高文良,彭骏.青藏高原低涡活动对降水影响的统计分析[J].高原气象,2012,31(3):592-604.
[14]赵勇,李如琦,杨霞,等.5月青藏高原地区感热异常对北疆夏季降水的影响[J].高原气象,2013,32(5):1215-1223,doi:10.7522/j.issn.1000-0534.2012.00117.
[15]Zhong L,Ma Y,Fu Y,et al.Assessment of soil water deficit for the middle reaches of Yarlung-Zangbo River from optical and passive microwave images[J].Remote Sens Environ, 2014,142:1-8.
[16]潘保田,李吉均.青藏高原:全球气候变化的驱动机与放大器[J].兰州大学学报:自然科学版,1996,32(1):108-115.
[17]叶笃正.青藏高原气象学[M].北京:科学出版社,1979:74-79.
[18]钱正安,张世敏,单扶民.1979年夏季高原地区对流云的分析.青藏高原气象科学实验文集[C].北京:科学出版社,1984:243-257.
[19]秦宏德,周和生,刘建西.青藏高原那曲地区对流性降水回波的统计特征[C].青藏高原气象科学实验文集(一),北京:科学出版社,1984:258-268.
[20]陈隆勋,宋玉宽,刘骥平,等.从气象卫星资料揭示的青藏高原夏季对流云系的日变化[J].气象学报,1999,57(5):549-560.
[21]刘黎平,楚荣忠.GAME — TIBET青藏高原云和降水综合观测概况及初步结果[J].高原气象,1999,18(3):441-450.
[22]江吉喜,范梅珠.夏季青藏高原上的对流云和中尺度对流系统[J].大气科学,2002,26(2):263-270.
[23]戴进,余兴,刘贵华,等.青藏高原雷暴弱降水云微物理特征的卫星反演分析[J].高原气象,2011,30(2):288-298.
[24]Bhatt B C,Nakamura K.Characteristics of monsoon rainfall around the Himalayas revealed by TRMM precipitation radar[J].Mon Wea Rev,2005,133(1):149-165.
[25]何文英,陈洪滨.TRMM卫星对一次冰雹降水过程的观测分析研究[J].气象学报,2006,64(3):364-376.
[26]傅云飞,宇如聪,崔春光,等.基于热带测雨卫星探测的东亚降水云结构特征的研究[J].暴雨灾害,2007,26(1):9-20.
[27]傅云飞,刘奇,自勇,等.基于TRMM卫星探测的夏季青藏高原降水和潜热分析[J].高原山地气象研究,2008,28(1):8-18.
[28]傅云飞,张爱民,刘勇,等.基于星载测雨雷达探测的亚洲对流和层云降水季尺度特征分析[J].气象学报,2008,66(5):730-746.
[29]傅云飞,冯沙,刘鹏,等.热带测雨卫星测雨雷达探测的亚洲夏季积雨云云砧[J].气象学报,2010,68(2):195-206.
[30]刘鹏,傅云飞.利用星载测雨雷达探测结果对夏季中国南方对流和层云降水气候特征的分析[J].大气科学,2010,34(4):802-814.
[31]傅云飞,刘鹏,刘奇,等.夏季热带及副热带降水云可见光/红外信号气候分布特征[J].大气与环境光学学报,2011,6(2):129-140.
[32]李典,白爱娟,黄盛军.利用TRMM卫星资料对青藏高原地区强对流天气特征分析[J].高原气象,2012,31(2):304-311.
[33]Fujinami H,Nomura S,Yasunari T.Characteristics of diurnal variations in convection and precipitation overthe southern Tibetan Plateau during summer[J].SOLA,2005,1:049-052.
[34]Fu Y,Liu G,Wu G,et al.Tower mast of precipitation over the central Tibetan Plateau summer[J].Geophy Res lett, 2006,33(5),doi:10.1029/2005GL024713.
[35]Fu Y,Liu G.Possible misidentification of rain type by TRMM PR over Tibetan Plateau[J].J Appl Meteorol Climatol,2007,46(5):667-672.
[36]傅云飞,李宏图,自勇.TRMM卫星探测青藏高原谷地的降水云结构个例分析[J].高原气象,2007,26(1):98-106.
[37]刘奇,傅云飞,刘国胜.夏季青藏高原与东亚及热带的降水的廓线差异分析[J].中国科学技术大学学报,2007,37(8):885-894.
[38]毛江玉,吴国雄.基于 TRMM 卫星资料揭示的亚洲季风区夏季降水日变化[J].中国科学地球科学,2012,42(4):564-576.
[39]Awaka J,Iguchi T,Okamoto K.Early results on rain type classification by the Tropical Rainfall Measuring Mission (TRMM)precipitation radar[C].Proc Eighth URSI Commission F Open Symp,1998:134-146.
[40]Liu Q,Fu Y,Yu R,et al.A new satellite-based census of precipitating and nonprecipitating clouds over the tropics and subtropics[J].Geophys Res Lett,2008,35(7),doi:10.1029/2008GL033208.
[41]Schumacher C,Houze R A.The TRMM precipitation radar's view of shallow,isolated rain[J].J Appl Meteor,2003,42(10):1519-1524.
[42]Yu R C,Zhou T,Xiong A,et al.Diurnal variations of summerprecipitation over contiguous China[J].Geophys Res Lett,2007,34(1),doi:10.1029/2006GL028129.
[43]过仲阳,林珲,江吉喜,等.卫星遥感揭示的青藏高原上MCS 活动特征及东移传播[J].遥感学报,2003,7(5):350-357.
[44]Rogers R R,Yau M K.A short course in cloud physics 3rd ed[M].Oxford:Pergamon Press,1989:293.
[45]Sorooshian S,Gao X,Hsu K,et al.Diurnal variability of tropical rainfall retrieved from combined GOES and TRMM satellite information[J].J Climate,2002,15(9):983-1001.

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