Simulation Study on the Radiation Impacts on the Formation and Development of a Tibetan Plateau Vortex
-
摘要: 已有研究表明辐射对热带气旋发生发展具有明显调制作用，高原涡与热带气旋有类似的暖心低压结构，辐射在高原涡发生发展过程中的作用也值得探讨。本文利用ERA-Interim再分析资料，通过中尺度数值模式WRF-ARW研究了辐射日变化对高原涡个例发展的影响机制。模拟结果表明，太阳短波辐射对高原涡的发生发展具有明显的调制作用。控制试验（CTL；即保留太阳辐射日变化）较好的再现了高原涡的发展过程。在去掉短波辐射过程的夜间试验（All_night）中，前期高原涡发展速度较快。而在白天（All_day）试验中，短波辐射过程抑制了高原涡的发展。诊断分析表明，夜间长波辐射冷却加强对流层温度递减率，减弱大气静力稳定度；同时，大气温度的降低使得夜间相对湿度增大，有利于对流层低层出现位势不稳定，进而促使高原涡的形成和发展。反之，太阳短波辐射有利于对流层高层增温，加强大气静力稳定度，从而抑制对流活动发展。夜间低层辐合更为强盛，有利于上升运动的加强并诱发高原涡形成；非平衡项结果显示，在高原涡环流中心区域存在正值区，而低涡四周为明显的负值区。从动力学和热力学特征来看，高原涡的发展与热带气旋具有一定的相似性。Abstract: Existing studies have shown that radiation has a significant effect on the occurrence and development of a tropical cyclone (TC). A Tibetan Plateau vortex (TPV) and a TC have a similar structure, the same as that of a warm-hearted and low-pressure structure, so the roles of radiation in the occurrence and development of the TPV is also worth discussing. In this study, the influence of the diurnal cycle of radiation on TPV development was examined using the Advanced Research Weather Research and Forecasting model. The results showed that solar shortwave radiation has a significant effect on the occurrence and development of the TPV. The control run (CTL; with the diurnal cycle of solar shortwave radiation) well reproduced the development process of the TPV. In the experiment with turning off the shortwave radiation (All_night), the TPV developed much faster at the early stage, whereas in the daytime experiment (All_day), the shortwave radiation suppressed the TPV development. The diagnostic analysis indicated that the longwave radiation cooling steepened the tropospheric lapse rate, thus weakening the atmospheric static stability. Additionally, the temperature reduction increased the relative humidity at night, which was conducive to potential instability in the lower troposphere and thus promoted TPV formation and development. Conversely, solar shortwave radiation warmed the upper troposphere and strengthened the static stability, which inhibited the convection development. The convergence at the lower layer is stronger at night than at day, which is beneficial to the ascending motion enhancement and the TPV formation. The unbalanced term indicated that the center of the TPV corresponded to the positive area of the unbalanced term and the outer edge of the TPV with the negative area of the unbalanced term. Numerical results showed that the TPV development bears many similarities to tropical cyclogenesis in terms of dynamics and thermodynamics.
-
图 1 2013年6月4日12:00至10日00:00高原涡观测路径。红色数字表示时间，括号内数值为500 hPa最低位势高度（单位: dagpm）
Figure 1. Observation track of the TPV (Tibetan Plateau vortex) from 1200 UTC 4 to 0000 UTC 10 June 2013. Red numbers indicate the time (UTC), the lowest geopotential height (units: dagpm) at 500 hPa is indicated in the brackets
图 2 2013年6月4日（a、c）06:00、（b、d）12:00（a、b）基于再分析资料以及（c、d）CTL试验模拟的500 hPa等压面上的流场（矢量，单位：m s−1）分布，等值线为地形高度在3000 m以上的区域，三角形为高原涡所处的位置
Figure 2. Distributions of wind field (vectors, units: m s−1) from (a, b) reanalysis data, (c, d) CTL (control run) experiment at 500 hPa at 0600 UTC (left column), 1200 UTC (right column) June 4, 2013. Contours outline the Tibetan Plateau with an altitude higher than 3000 m; the triangle shows the location of the TPV
图 3 2013年6月4日09:00（左列）、15:00（中间列）和21:00（右列）模拟的500 hPa等压面上的环境场大尺度相对涡度（阴影，单位：10−5 s−1）、小尺度系统相对涡度（等值线，单位：10−5 s−1）和风场（矢量，单位：m s−1）分布：（a–c）CTL试验；（d–f）All_night试验；（g–i）All_day试验。绿色方框为涡旋中心区域（300 km×300 km）
Figure 3. Distributions of large-scale relative vorticity (shaded, units: 10−5 s−1), small-scale system vorticity (contours, units: 10−5 s−1) and wind field (vectors, units: m s−1) from (a–c) CTL, (d–f) All_night experiment, and (g–i) All_day experiment at 500 hPa at 0900 UTC (left column), 1500 UTC (middle column), and 2100 UTC (right column) 4 June 2013. The green box indicates the central area of the TPV（300 km×300 km）
图 4 2013年6月4日高原涡中心附近（300 km×300 km）12:00～18:00时间平均的CFAD（Contoured Frequency by Altitude Diagram，阴影）分布：（a）CTL试验；（b）All_night试验；（c）All_day试验
Figure 4. Averaged CFAD ( Contoured Frequency by Altitude Diagram; shaded) during 1200 UTC–1800 UTC 4 June 2013, calculated over a box area with a radius of 300 km around the vortex center: (a) CTL; (b) All_night experiment; (c) All_day experiment
图 5 2013年6月4日00:00～23:00低涡中心附近区域平均（300 km×300 km）相对涡度（阴影，单位： 10−5 s−1）的垂直分布：（a）CTL试验；（b）All_night试验；（c）All_day试验
Figure 5. Time evolution of the vertical profile of vorticity (shaded, units: 10−5 s−1) during 0000 UTC–2300 UTC 4 June 2013, averaged over a box area with a radius of 300 km around the vortex center: (a) CTL experiment; (b) All_night experiment; (c) All_day experiment
图 8 2013年6月4日09:00（左列）、15:00（中间列）和21:00（右列）500 hPa等压面上的环境场大尺度相对涡度（阴影，单位：10−5 s−1）、OW指数（等值线，单位：10−9 s−2）分布：（a）CTL试验；（b）All_night试验；（c）All_day试验
Figure 8. Distributions of environmental vorticity (shaded, units: 10−5 s−1), OW index (contour, units: 10−9 s−2) at 500 hPa at 0900 UTC (left column), 1500 UTC (middle column) and 2100 UTC (right column) 4 June 2013: (a) CTL experiment; (b) All_night experiment; (c) All_day experiment
图 9 2013年6月4日09:00（左列）、15:00（中间列）和21:00（右列）500 hPa等压面上非平衡项（阴影，单位：10−9 s−2）、风场（矢量，单位：m s−1）分布：（a）CTL试验；（b）All_night试验；（c）All_day试验
Figure 9. Distributions of non-balance terms (shaded, units: 10−9 s−2 ), wind field (vectors, units: m s−1) at 500 hPa at 0900 UTC (left column), 1500 UTC (middle column) and 2100 UTC (right column) 4 June 2013: (a) CTL experiment; (b) All_night experiment; (c) All_day experiment
图 10 2013年6月4日21:00（a）CTL、（b）All_night和（c）All_day试验中垂直运动（阴影，单位：10−2 m s−1）和切向风速（等值线，单位：m s−1）的轴对称分量的半径—高度的垂直剖面
Figure 10. Radius–height cross sections of the axisymmetric component of vertical velocity (shaded, units: 10−2 m s−1) and tangential wind speed (contour, units:
$ m{s}^{-1} $ ) in (a) CTL, (b) All_night, and (c) All_day experiments at 2100 UTC 4 June 2013
图 12 2013年6月4日（a–c）CTL、（d–f）All_night和（g–i）All_day试验的500 hPa等压面上公式（2）中扰动动能倾向
$\displaystyle\frac{\partial K'}{\partial t}$ （左列）、纬向风辐合$-\overline{u{'}^{2}}\displaystyle\frac{\partial }{\partial x}\overline{u}$ （中间列）和径向风辐合$-\overline{v{'}^{2}}\displaystyle\frac{\partial }{\partial y}\overline{v}$ （右列）00:00～12:00时间平均结果分布（阴影，单位：10−5 m2 s−3），三角形为高原涡所处的位置Figure 12. Horizontal pattern of kinetic energy tendency
$\displaystyle\frac{\partial K'}{\partial t}$ (left column), latitudinal wind convergence$-\overline{u{'}^{2}}\displaystyle\frac{\partial }{\partial x}\overline{u}$ (middle column ) and radial wind convergence$-\overline{v{'}^{2}}\displaystyle\frac{\partial }{\partial y}\overline{v}$ (right column ) in Eq. 2 on the 500 hPa (shaded, units: 10−5 m2 s−3), the triangle reflects the location of the TPV in (a-c) CTL, (d-f) All_night, and (g-i) All_day. Time averaged from 0000 UTC–1200 UTC 4 June 2013
图 13 2013年6月4日00:00～23:00（a）CTL、（b）All_night和（c）All_day试验中低涡中心附近区域平均（300 km×300 km）相对湿度（阴影）垂直分布随时间的变化
Figure 13. Time evolution of the vertical profile of relative humidity (shaded), averaged over a box area centered at the TPV during 0000 UTC–2300 UTC 4 June 2013: (a) CTL experiment; (b) All_night experiment; (c) All_day experiment
图 14 2013年6月4日00:00～23:00（a）CTL、（b）All_night和（c）All_day试验中低涡中心附近区域平均（300 km×300 km）的降水效率随时间的变化
Figure 14. Time evolution of PE (Precipitation Efficiency) in CTL, All_night, and All_day experiments during 0000 UTC–2300 UTC 4 June 2013. Averaged over a box area with a radius of 300 km around the vortex center
图 15 2013年6月4日00:00～23:00（a）三组试验中低涡中心附近区域（300 km×300 km），辐射导致的平均加热廓线（单位：K h−1），低涡中心附近区域（300 km×300 km）平均温度垂直分布随时间变化的差异，（b）All_night 减CTL试验（c）All_day减 CTL试验（等值线，单位：K, 实线为正值，虚线为负值）
Figure 15. (a) Vertical profiles of radiative heating (units: K h−1) in the three experiments, which are averaged over a box area centered at TPV during 0000–2300 UTC 4 June 2013. Time evolution of the vertical profile of temperature contrast (units: K, solid lines indicate positive value, dash lines indicate negative value) which are averaged over the box area centered at the TPV for (b) All_night minus CTL and (c) All_day minus CTL
图 16 2013年6月4日09:00、15:00和21:00（a）CTL、（b）All_night和（c）All_day试验中低涡中心附近（300 km×300 km）区域平均的
$ {\partial \theta }/{\partial p} $ 垂直廓线（单位：K hPa−1）分布Figure 16. Vertical profiles of
$ {\partial \theta }/{\partial p} $ (units: K hPa−1) at 0900 UTC, 1500 UTC, and 2100 UTC 4 June 2013, which are averaged over the box area centered at the TPV: (a) CTL experiment; (b) All_night experiment; (c) All_day experiment表 1 试验的描述
Table 1. Description of the experiments
试验名称 描述 CTL 太阳短波辐射具有完整的日循环 All_night 太阳短波辐射的强度固定在午夜（00:00） All_day 太阳短波辐射的强度固定在正午（12:00） 
下载: 导出CSV
-
[1] Bister M, Emanuel K A. 1997. The genesis of hurricane Guillermo: TEXMEX analyses and a modeling study [J]. Mon. Wea. Rev, 125(10): 2662−2682. doi:10.1175/1520-0493(1997)125<2662:TGOHGT>2.0.CO;2 [2] Cao X, Li T, Peng M, et al. 2014. Effects of monsoon trough intraseasonal oscillation on tropical cyclogenesis over the western North Pacific [J]. J. Atmos. Sci., 71(12): 4639−4660. doi: 10.1175/JAS-D-13-0407.1 [3] Dell’Osso L, Chen S J. 1986. Numerical experiments on the genesis of vortices over the Qinghai-Tibet Plateau [J]. Tellus A:Dyn. Meteor. Oceanogr., 38(3): 236−250. doi: 10.3402/tellusa.v38i3.11715 [4] 杜梅, 李国平, 李山山. 2020. 高原横切变线与高原低涡关系的初步研究 [J]. 大气科学, 44(2): 269–281. Du Mei, Li Guoping, Li Shanshan. 2020. A preliminary study of the relationship between the plateau transverse shear line and plateau vortex [J]. Chinese Journal of Atmospheric Sciences (in Chinese), 44(2): 269−281. doi: 10.3878/j.issn.1006-9895.1906.18191 [5] Dudhia J. 1989. Numerical study of convection observed during the winter monsoon experiment using a mesoscale two-dimensional model [J]. J. Atmos. Sci., 46(20): 3077−3107. doi:10.1175/1520-0469(1989)046<3077:NSOCOD>2.0.CO;2 [6] Dunion J P, Thorncroft C D, Velden C S. 2014. The tropical cyclone diurnal cycle of mature hurricanes [J]. Mon. Wea. Rev., 142(10): 3900−3919. doi: 10.1175/MWR-D-13-00191.1 [7] Ge X Y, Ma Y, Zhou S W, et al. 2015. Sensitivity of the warm core of tropical cyclones to solar radiation [J]. Adv. Atmos. Sci., 32(8): 1038−1048. doi: 10.1007/s00376-014-4206-0 [8] 葛旭阳, 许可, 马悦, 等, 2018. 云辐射强迫效应对热带气旋发展和结构的影响[J]. 大气科学学报, 41(1): 46–54Ge Xuyang, Xu Ke, Ma Yue, et al. 2018. Impacts of cloud-radiative forcing on tropical cyclone intensification and structure [J]. Trans. Atmos. Sci. (in Chinese), 41(1): 46–54. doi: 10.13878/j.cnki.dqkxxb.20150421001 [9] 管靓, 周顺武, 葛旭阳, 等. 2016. “育婴袋”假说在西北太平洋台风生成地点的应用研究 [J]. 热带气象学报, 32(4): 494−502. doi: 10.16032/j.issn.1004-4965.2016.04.007Guan Liang, Zhou Shunwu, Ge Xuyang, et al. 2016. The application of marsupial paradigm in typhoons cyclogenesis location over the western North Pacific [J]. J. Trop. Meteor. (in Chinese), 32(4): 494−502. doi: 10.16032/j.issn.1004-4965.2016.04.007 [10] 郭春蕊, 张庆红. 2012. 台风榴莲(2001)生成初期中尺度涡旋合并过程研究 [J]. 气象学报, 70(1): 1−14. doi: 10.11676/qxxb2012.001Guo Chunrui, Zhang Qinghong. 2012. A study of the role of mesoscale vortex merging in the genesis of Typhoon Durian (2001) [J]. Acta Meteor. Sinica (in Chinese), 70(1): 1−14. doi: 10.11676/qxxb2012.001 [11] 何光碧, 屠妮妮, 高文良. 2010. 一次高原低涡东移引发强降水过程的数值试验 [J]. 成都信息工程学院学报, 25(6): 626−633. doi: 10.3969/j.issn.1671-1742.2010.06.016He Guangbi, Tu Nini, Gao Wenliang. 2010. The numerical experiment of plateau vortex moving eastwards accompanied by a heavy precipitation process [J]. J. Chengdu Univ. Inf. Technol. (in Chinese), 25(6): 626−633. doi: 10.3969/j.issn.1671-1742.2010.06.016 [12] Hendricks E A, Montgomery M T, Davis C A. 2004. The role of "vortical" hot towers in the formation of tropical cyclone Diana (1984) [J]. J. Atmos. Sci., 61(11): 1209−1232. doi:10.1175/1520-0469(2004)061<1209:TROVHT>2.0.CO;2 [13] Hobgood J S. 1986. A possible mechanism for the diurnal oscillations of tropical cyclones [J]. J. Atmos. Sci., 43(23): 2901−2922. doi:10.1175/1520-0469(1986)043<2901:APMFTD>2.0.CO;2 [14] Isern-Fontanet J, Font J, García-Ladona E, et al. 2004. Spatial structure of anticyclonic eddies in the Algerian basin (Mediterranean Sea) analyzed using the Okubo–Weiss parameter [J]. Deep Sea Research Ⅱ:Topical Studies in Oceanography, 51(25-26): 3009−3028. doi: 10.1016/j.dsr2.2004.09.013 [15] Kossin J P. 2002. Daily hurricane variability inferred from GOES infrared imagery [J]. Mon. Wea. Rev., 130(9): 2260−2270. doi:10.1175/1520-0493(2002)130<2260:DHVIFG>2.0.CO;2 [16] 李国平. 2002. 青藏高原动力气象学[M]. 北京: 气象出版社, 19–23Li Guoping. 2002. Dynamic Meteorology of the Tibetan Plateau (in Chinese) [M]. Beijing: China Meteorological Press, 19–23. [17] 李山山. 2017. 高原切变线影响强降水的特征分析 [D]. 成都信息工程大学硕士学位论文. Li Shanshan. 2017. Characteristic analysis of plateau shear lines related to heavy rainfall [D]. M. S. thesis (in Chinese), Chengdu University of Information Technology. [18] 李国平, 刘红武. 2006. 地面热源强迫对青藏高原低涡作用的动力学分析 [J]. 热带气象学报, 22(6): 632−637. doi: 10.3969/j.issn.1004-4965.2006.06.017Li Guoping, Liu Hongwu. 2006. A dynamical study of the role of surface heating on the Tibetan Plateau vortices [J]. J. Trop. Meteor. (in Chinese), 22(6): 632−637. doi: 10.3969/j.issn.1004-4965.2006.06.017 [19] Li X F, Gao S T. 2012. Precipitation Modeling and Quantitative Analysis [M]. Dordrecht: Springer, 209–217. doi: 10.1007/978-94-007-2381-8 [20] Li L, Zhang R H, Wen M. 2011. Diagnostic analysis of the evolution mechanism for a vortex over the Tibetan Plateau in June 2008 [J]. Adv. Atmos. Sci., 28(4): 797−808. doi: 10.1007/s00376-010-0027-y [21] Li L, Zhang R H, Wen M. 2014. Diurnal variation in the occurrence frequency of the Tibetan Plateau vortices [J]. Meteor. Atmos. Phys., 125(3): 135−144. doi: 10.1007/s00703-014-0325-5 [22] Li L, Zhang R H, Wen M. 2018. Diurnal variation in the intensity of nascent Tibetan Plateau vortices [J]. Quart. J. Roy. Meteor. Soc., 144(717): 2524−2536. doi: 10.1002/qj.3343 [23] 李黎, 吕世华, 范广洲. 2019. 夏季青藏高原地表能量变化对高原低涡生成的影响分析 [J]. 高原气象, 38(6): 1172−1180. doi: 10.7522/j.issn.1000-0534.2018.00154Li Li, Lü Shihua, Fan Guangzhou. 2019. Analysis of the influence of the Qinghai-Tibetan Plateau surface energy change on the formation of the plateau vortex in summer [J]. Plateau Meteor. (in Chinese), 38(6): 1172−1180. doi: 10.7522/j.issn.1000-0534.2018.00154 [24] 罗四维, 杨洋. 1992. 一次青藏高原夏季低涡的数值模拟研究 [J]. 高原气象, 11(1): 39−48.Luo Siwei, Yang Yang. 1992. A case study on numerical simulation of summer vortex over Qinghai-Xizang (Tibetan) Plateau [J]. Plateau Meteor. (in Chinese), 11(1): 39−48. [25] 罗四维, 何梅兰, 刘晓东. 1993. 关于夏季青藏高原低涡的研究 [J]. 中国科学(B辑), 23(7): 778−784.Luo Siwei, He Meilan, Liu Xiaodong. 1993. A study of the Tibetan Plateau vortex in summer [J]. Science in China (Series B) (in Chinese), 23(7): 778−784. [26] 马林, 张青梅, 赵春宁, 等. 2003. 青藏高原东部牧区春季雪灾天气的形成及其预报 [J]. 自然灾害学报, 12(3): 61−68. doi: 10.3969/j.issn.1004-4574.2003.03.010Ma Lin, Zhang Qingmei, Zhao Chunning, et al. 2003. Formation and forecast of spring snow-disaster weather in the eastern pasture-area of Qinghai-Xizang Plateau [J]. Journal of Natural Disasters (in Chinese), 12(3): 61−68. doi: 10.3969/j.issn.1004-4574.2003.03.010 [27] Melhauser C, Zhang F Q. 2014. Diurnal radiation cycle impact on the Pregenesis environment of Hurricane Karl (2010) [J]. J. Atmos. Sci., 71(4): 1241−1259. doi: 10.1175/JAS-D-13-0116.1 [28] Montgomery M T, Nicholls M E, Cram T A, et al. 2006. A vortical hot tower route to tropical cyclogenesis [J]. J. Atmos. Sci., 63(1): 355−386. doi: 10.1175/JAS3604.1 [29] Ruppert Jr J H, Wing A A, Tang X D, et al. 2020. The critical role of cloud–infrared radiation feedback in tropical cyclone development [J]. Proc. Natl. Acad. Sci. USA, 117(45): 27884−27892. doi: 10.1073/pnas.2013584117 [30] Shen R, Reiter E R, Bresch J F. 1986a. Numerical simulation of the development of vortices over the Qinghai-Xizang (Tibet) Plateau [J]. Meteor. Atmos. Phys., 35(1): 70−95. doi: 10.1007/BF01029526 [31] 宋雯雯, 李国平, 唐钱奎. 2012. 加热和水汽对两例高原低涡影响的数值试验 [J]. 大气科学, 36(1): 117−129. doi: 10.3878/j.issn.1006-9895.2012.01.10Song Wenwen, Li Guoping, Tang Qiankui. 2012. Numerical simulation of the effect of heating and water vapor on two cases of Plateau Vortex [J]. Chinese Journal of Atmospheric Sciences (in Chinese), 36(1): 117−129. doi: 10.3878/j.issn.1006-9895.2012.01.10 [32] Steranka J, Rodgers E B, Gentry R C. 1986. The relationship between satellite measured convective bursts and tropical cyclone intensification [J]. Mon. Wea. Rev., 114(8): 1539−1546. doi:10.1175/1520-0493(1986)114<1539:TRBSMC>2.0.CO;2 [33] Tang X D, Zhang F Q. 2016. Impacts of the diurnal radiation cycle on the Formation, intensity, and structure of Hurricane Edouard (2014) [J]. J. Atmos. Sci., 73(7): 2871−2892. doi: 10.1175/JAS-D-15-0283.1 [34] 田珊儒, 段安民, 王子谦, 等. 2015. 地面加热与高原低涡和对流系统相互作用的一次个例研究 [J]. 大气科学, 39(1): 125–136. Tian Shanru, Duan Anmin, Wang Ziqian, et al. 2015. Interaction of surface heating, the Tibetan Plateau vortex, and a convective system: A case study [J]. Chinese Journal of Atmospheric Sciences (in Chinese), 39(1): 125−136. doi: 10.3878/j.issn.1006-9895.1404.13311 [35] Wang B. 1987. The development mechanism for Tibetan Plateau warm vortices [J]. J. Atmos. Sci., 44(20): 2978−2994. doi:10.1175/1520-0469(1987)044<2978:TDMFTP>2.0.CO;2 [36] Webster P J, Stephens G L. 1980. Tropical upper-tropospheric extended clouds: Inferences from winter MONEX [J]. J. Atmos. Sci., 37(7): 1521−1541. doi: 10.1175/1520-0469-37.7.1521 [37] Webster P J, Chang H R. 1988. Equatorial energy accumulation and emanation regions: Impacts of a zonally varying basic state [J]. J. Atmos. Sci., 45(5): 803−829. doi:10.1175/1520-0469(1988)045<0803:EEAAER>2.0.CO;2 [38] Xu K M, Randall D A. 1995. Impact of interactive radiative transfer on the macroscopic behavior of cumulus ensembles. Part II: Mechanisms for cloud–radiation interactions [J]. J. Atmos. Sci., 52(7): 800−817. doi:10.1175/1520-0469(1995)052<0800:IOIRTO>2.0.CO;2 [39] 徐梦婷, 周顺武, 葛旭阳. 2016. 季风涡旋对热带气旋生成影响的理想试验研究 [J]. 气象学报, 74(5): 733−743. doi: 10.11676/qxxb2016.060Xu Mengting, Zhou Shunwu, Ge Xuyang. 2016. An idealized simulation study of the impact of monsoon gyre on tropical cyclogenesis [J]. Acta Meteor. Sinica (in Chinese), 74(5): 733−743. doi: 10.11676/qxxb2016.060 [40] 杨克明, 毕宝贵, 李月安, 等. 2001. 1998年长江上游致洪暴雨的分析研究 [J]. 气象, 27(8): 9−14. doi: 10.3969/j.issn.1000-0526.2001.08.002Yang Keming, Bi Baogui, Li Yuean, et al. 2001. On flood-causing torrential rainfall in the upstream district of Changjiang River in 1998 [J]. Meteor. Mon. (in Chinese), 27(8): 9−14. doi: 10.3969/j.issn.1000-0526.2001.08.002 [41] 叶笃正, 高由禧. 1979. 青藏高原气象学[M]. 北京: 科学出版社, 278ppTe T C, Gao Youxi. 1979. Qinghai–Xizang Plateau Meteorology (in Chinese) [M]. Beijing: Science Press, 278pp. [42] 叶笃正, 罗四维, 朱抱真. 1957. 西藏高原及其附近的流场结构和对流层大气的热量平衡 [J]. 气象学报, 28(2): 108−121. doi: 10.11676/qxxb1957.010Yeh T C, Lo S W, Chu P C. 1957. The wind structure and heat balance in the lower troposphere over Tibetan Plateau and its surrounding [J]. Acta Meteor. Sinica (in Chinese), 28(2): 108−121. doi: 10.11676/qxxb1957.010 [43] Yeh T C. 1950. The circulation of the high troposphere over China in the winter of 1945–1946 [J]. Tellus, 2(3): 173−183. doi: 10.3402/tellusa.v2i3.8548 [44] 郁淑华, 高文良. 2010. 1998年夏季两例青藏高原低涡结构特征的比较 [J]. 高原气象, 29(6): 1357−1368.Yu Shuhua, Gao Wenliang. 2010. Comparison on structure characteristics of two Tibetan Plateau vortexes in Summer, 1998 [J]. Plateau Meteor. (in Chinese), 29(6): 1357−1368. [45] Yuter S E, Houze Jr R A. 1995. Three-dimensional kinematic and microphysical evolution of Florida cumulonimbus. Part I: Spatial distribution of updrafts, downdrafts, and precipitation [J]. Mon. Wea. Rev., 123(7): 1921−1940. doi:10.1175/1520-0493(1995)123<1921:TDKAME>2.0.CO;2 [46] Zhang D L, Fritsch J M. 1987. Numerical simulation of the Meso-β Scale structure and evolution of the 1977 Johnstown flood. Part Ⅱ: Inertially stable warm-core vortex and the Mesoscale convective complex [J]. J. Atmos. Sci, 44(18): 2593−2612. doi:10.1175/1520-0469(1987)044<2593:NSOTMS>2.0.CO;2 [47] Zheng Y J, Wu G X, Liu Y M. 2013. Dynamical and thermal problems in vortex development and movement. Part I: A PV-Q view [J]. Acta Meteor. Sinica, 27(1): 1−14. doi: 10.1007/s13351-013-0101-3 [48] Zhou Y S, Li X F, Gao S T. 2014. Precipitation efficiency and its relationship to physical factors [J]. Chinese Phys. B, 23(6): 064210. doi: 10.1088/1674-1056/23/6/064210 -
点击查看大图
计量
- 文章访问数: 106
- HTML全文浏览量: 9
- PDF下载量: 45
- 被引次数: 0
