doi:  10.3878/j.issn.1006-9895.1812.18209
污染天气下成都东部山地-平原风环流结构的数值模拟

A Numerical Simulation of Mountain-Plain Breeze Circulation in a Heavy Pollution Event in Eastern Chengdu
摘要点击 145  全文点击 55  投稿时间:2018-07-31  修订日期:2018-11-19
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基金:  国家重点研发计划重点专项项目2016YFC0203304
中文关键词:  大气污染  山谷风  山地-平原风环流  复杂地形
英文关键词:  Atmospheric pollution, Mountain-valley breeze, Mountain-plain breeze circulation, Complex terrain
        
作者中文名作者英文名单位
田 越TIAN Yue南京信息工程大学气象灾害教育部重点实验室
苗峻峰MIAO Junfeng南京信息工程大学气象灾害教育部重点实验室
赵天良ZHAO Tianliang南京信息工程大学中国气象局气溶胶与云降水重点开放实验室
引用:田 越,苗峻峰,赵天良.2019.污染天气下成都东部山地-平原风环流结构的数值模拟[J].大气科学
Citation:TIAN Yue,MIAO Junfeng,ZHAO Tianliang.2019.A Numerical Simulation of Mountain-Plain Breeze Circulation in a Heavy Pollution Event in Eastern Chengdu[J].Chinese Journal of Atmospheric Sciences (in Chinese)
中文摘要:
      本文利用中尺度模式WRF(V3.9)对2016年12月7日成都东部(龙泉山)一次污染过程下的山地-平原风环流进行了模拟,旨在探讨冬季污染天气下山地-平原风环流的结构和演变特征。此外,通过减少气溶胶光学厚度(AOD,aerosol optical depth)的敏感性试验探究气溶胶污染对山地-平原风环流的影响。结果表明:冬季污染大气条件下成都平原地区存在显著逆温。龙泉山南北长、东西窄且高度较低,由于东、西坡辐射能量的不均匀分布和背景风的强迫,上午、凌晨和夜间均出现越山下坡风环流,上午强度较强,凌晨和夜间强度较弱。该天龙泉山平原风环流在午后开始发展,最大影响范围为山体宽度的3-4倍,17:00左右结束。南北方向上各阶段环流差异较大,越山下坡风环流在南段最强,中段最弱;中、南段山体较低窄,平原风环流易被湍流掩盖,北段平原风环流最为明显。AOD减小后辐射及地表热通量均有所增加,中、南段湍流更加旺盛,边界层显著抬升且降低时间滞后,山体与平原间感热通量差异增加,北段平原风环流增强、持续时间增长。
Abstract:
      In this paper, WRF (V3.9) is used to simulate the Longquan mountain-plain breeze circulation in a heavy pollution event on December 7, 2016. The structure and evolution of the mountain-plain breeze circulation are discussed as purpose. Besides, the influence of AOD on the mountain-plain breeze circulation is examined by conducting a sensitivity experiment in which the AOD value is reduced. The Longquan mountain is fairly long from north to south, comparatively narrow from east to west and low in height. Result shows that intense ground inversion exists in winter during a heavy pollution event. Cross-mountain downslope wind circulation occurs at night and late morning due to the imbalance of radiation, heat flux between west and east slope and the dynamic forcing of background wind. Plain breeze circulation begins after noon and ends at around 1700 LST. Maximum horizontal stretch of the plain breeze circulation can reach 3 to 4 times of the mountain width. Cross-mountain downslope breeze circulation and mountain-plain breeze circulation vary greatly in north-south direction. The former is stronger in the southern part of the mountain whereas the plain breeze circulation in the middle and southern part are easily covered by vigorous turbulences. In the northern part, on the contrary, there exists a significant plain breeze circulation. After reducing the AOD in the sensitivity experiment, the solar radiation, heat flux and planetary boundary layer height increase to a certain extent. Plain breeze circulation in the middle and southern part are more ambiguous due to amplified turbulences; while in the northern part, it is enhanced by the elevated planetary boundary layer and the strengthened difference in sensible heat between the mountain and plain area.
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