利用风廓线雷达研究郑州机场低空急流特征及其对飞行的影响
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摘要
利用2016、2017年郑州机场高分辨率边界层风廓线雷达半小时平均观测资料,对机场上空低空急流时空分布特征进行统计研究,结果表明:夏末、秋季低空急流出现次数相对较少,春季、夏初是高发时期,冬季易出现较强的超低空急流,只有春季风速从低层到高层呈现先增大后减小、再增大的变化过程,8月末可能是急流的时空转换期;夜间和凌晨是高发时段,白天降低30%～40%,一般情况下,00—12时(世界时,下同)急流较弱,12时后明显增强向上发展,19时开始减弱,持续至21时;急流中心最大风速一半以上在12～18 m/s,高度集中在60～180 m和300～900 m,超低空急流占大部分,夜间出现最大风速的概率远高于白天;低空急流发生高度大部分在飞机起飞或着陆的范围内,使飞机复飞概率增加,对夜间航班影响更大。
The spatial and temporal distribution features of a low-level jet are statistically studied, based on the half-hour average observation data of a high-resolution boundary layer wind profile radar at Zhengzhou Airport in 2016 and 2017. Results show that the low-level jet occurs relatively less frequent in late summer and autumn. In spring and early summer, there is a high incidence period. Ultra-low jets are easy to appear in winter. Spring is the only season in which the wind speed increases first, then decreases, and increases again from lower to upper level. The temporal and spatial transition period of jet streams may be at the end of August. Low-level jets occur frequently at night and early morning, but reduce by about 30% ～40%during the day. The jet stream is usually weak between 00:00 and 12:00(UTC, the same below),significantly increases after 12:00 and begins to weaken at 19:00, before dissipating at about 21:00. More than half of the maximum wind speed at the center of the jet stream is in 12～18 m/s, and the jet height is concentrated at 60～180 m and 300～900 m. Ultra-low jets are the majority. The probability of maximum wind speed appearing at night is higher than that in the daytime. The altitude of a low-level jet is mostly within the range of take-off and landing of the aircraft. So it is easy to cause aircraft to overfly, and the impact on nighttime flights is greater.
The spatial and temporal distribution features of a low-level jet are statistically studied, based on the half-hour average observation data of a high-resolution boundary layer wind profile radar at Zhengzhou Airport in 2016 and 2017. Results show that the low-level jet occurs relatively less frequent in late summer and autumn. In spring and early summer, there is a high incidence period. Ultra-low jets are easy to appear in winter. Spring is the only season in which the wind speed increases first, then decreases, and increases again from lower to upper level. The temporal and spatial transition period of jet streams may be at the end of August. Low-level jets occur frequently at night and early morning, but reduce by about 30% ～40%during the day. The jet stream is usually weak between 00:00 and 12:00(UTC, the same below),significantly increases after 12:00 and begins to weaken at 19:00, before dissipating at about 21:00. More than half of the maximum wind speed at the center of the jet stream is in 12～18 m/s, and the jet height is concentrated at 60～180 m and 300～900 m. Ultra-low jets are the majority. The probability of maximum wind speed appearing at night is higher than that in the daytime. The altitude of a low-level jet is mostly within the range of take-off and landing of the aircraft. So it is easy to cause aircraft to overfly, and the impact on nighttime flights is greater.
引文
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[3]衣育红,钱永甫,罗四维.索马里低空急流的数值模拟[J].热带气象,1989,5(3):201-209.
[4]汪永铭,薛纪善.华南前汛期低空急流的诊断分析[J].热带气象,1985,1(2):121-128.
[5]罗德海.环境场对边界层低空急流形成的影响[J].热带气象,1987,3(3):227-232.
[6]王会军,薛峰.索马里急流的年际变化及其对半球间水汽输送和东亚夏季降水的影响[J].地球物理学报,2003,46(1):18-25.
[7]陈忠明,何光碧,崔春光,等.对流、湿度锋与低空急流的耦合——持续性暴雨维持的一种可能机制[J].热带气象学报,2007,23(3):246-254.
[8]周静,郑永骏,苗春生,等.梅雨锋强降水与低空急流日变化的观测分析和数值模拟[J].热带气象学报,2017,33(5):750-761.
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[11] JOSHI R R, NARENDRA S, DESHPANDE S M, et al. UHF wind profiler observations of monsoon low level jet over Pune[J]. Indian Journal of Radio&Space Physics, 2006, 35(5):349-359.
[12]张小雯,郑永光,吴蕾,等.风廓线雷达资料在天气业务中的应用现状与展望[J].气象科技,2017,45(2):285-297.
[13]刘红艳,魏鸣,管理.多普勒雷达风场资料在临近预报中的应用[J].大气科学学报,2015,38(4):483-491.
[14]刘淑媛,郑永光,陶祖钰.利用风廓线雷达资料分析低空急流的脉动与暴雨关系[J].热带气象学报,2003,19(3):285-290.
[15]张京英,漆梁波,王庆华.用雷达风廓线产品分析一次暴雨与高低空急流的关系[J].气象,2005,31(12):41-44.
[16]张柽柽,胡明宝,邓少格,等.利用风廓线雷达资料对暴雨与低空急流关系的分析[J].气象水文海洋仪器,2011,28(1):32-35.
[17]金巍,曲岩,姚秀萍,等.一次大暴雨过程中低空急流演变与强降水的关系[J].气象,2007,33(12):31-38.
[18]李健,田军,栗敬仁.风廓线雷达在郑州机场一次持续雾霾过程的应用研究[C]//第34届中国气象学会年会S18气象雷达探测新技术与数据质控的业务应用论文集. 2017.
[19]牟惟丰.低空急流述评[J].气象科技,1998(4):7-12.
[20]赛瀚,苗峻峰.中国地区低空急流研究进展[J].气象科技,2012,40(5):766-771.
[21]李建辉.华南初夏的超低空急流及其对暴雨的影响[J].气象学报,1982,40(3):319-326.
[22]马福建.徐州冬季边界层低空急流的观测研究[J].气象科学,1983(2):41-46.
[23]李兴生,叶卓佳,刘林勤.夜间低空急流的分析研究[J].大气科学,1981,5(3):310-317.
[24]李兴生,朱翠娟,刘林勤,等.行星边界层中多极值风速廓线的研究[J].大气科学,1982,6(3):308-314.
[25]金维明,王学永,洪钟祥,等.夜间逆温条件下超低空急流的间歇性特征[J].大气科学,1983,7(3):296-302.
[26]丁一汇.高等天气学[M].北京:气象出版社,1991:573-586.
[27]陈楠,胡明宝,张柽柽,等.利用风廓线雷达资料对南京地区低空急流的统计分析[J].热带气象学报,2014,30(3):511-517.
[28]王东阡,张耀存.中国东部西南低空急流日变化特征及其机制[J].地球物理学报,2012,55(8):2 498-2 507.
[29] BLACKADAR A K. Boundary layer wind maxima and their significance for the growth of nocturnal inversions[J]. Bull Amer Meteor Soc,1957,38(5):283-290.
[30]何建中,伍荣生.边界层低空急流的数值研究[J].气象学报,1989,47(4):443-449.
[31]夏敏洁,周文君,裴海瑛,等.基于L波段雷达探空资料的南京低空逆温特征[J].大气科学学报,2017,40(4):562-569.
[32] UCCELLINI L W. On the role of upper tropospheric jet streaks and leeside cyclogenesis in the development of low-level jets in the Great Plains[J]. Mon Wea Rev,1980,108(10):1 689-1 696.
[2]孙淑清,马廷标,孙纪改.低空急流与暴雨相互关系的对比分析[J].气象学报,1979,37(4):36-44.
[3]衣育红,钱永甫,罗四维.索马里低空急流的数值模拟[J].热带气象,1989,5(3):201-209.
[4]汪永铭,薛纪善.华南前汛期低空急流的诊断分析[J].热带气象,1985,1(2):121-128.
[5]罗德海.环境场对边界层低空急流形成的影响[J].热带气象,1987,3(3):227-232.
[6]王会军,薛峰.索马里急流的年际变化及其对半球间水汽输送和东亚夏季降水的影响[J].地球物理学报,2003,46(1):18-25.
[7]陈忠明,何光碧,崔春光,等.对流、湿度锋与低空急流的耦合——持续性暴雨维持的一种可能机制[J].热带气象学报,2007,23(3):246-254.
[8]周静,郑永骏,苗春生,等.梅雨锋强降水与低空急流日变化的观测分析和数值模拟[J].热带气象学报,2017,33(5):750-761.
[9] The national weather service and the office of oceanic and atmospheric research. Wind profile assessment report and recommendations for future ese[R]. Publishing by U. S. Department of Commerce and National Oceanic and Atmospheric Administration,1994:1-141.
[10] MARK J M, KEN L. A climatology of the warm season great plains low-level jet using wind profile observations[J]. Wea Forecasting,1995, 10(3):576-591.
[11] JOSHI R R, NARENDRA S, DESHPANDE S M, et al. UHF wind profiler observations of monsoon low level jet over Pune[J]. Indian Journal of Radio&Space Physics, 2006, 35(5):349-359.
[12]张小雯,郑永光,吴蕾,等.风廓线雷达资料在天气业务中的应用现状与展望[J].气象科技,2017,45(2):285-297.
[13]刘红艳,魏鸣,管理.多普勒雷达风场资料在临近预报中的应用[J].大气科学学报,2015,38(4):483-491.
[14]刘淑媛,郑永光,陶祖钰.利用风廓线雷达资料分析低空急流的脉动与暴雨关系[J].热带气象学报,2003,19(3):285-290.
[15]张京英,漆梁波,王庆华.用雷达风廓线产品分析一次暴雨与高低空急流的关系[J].气象,2005,31(12):41-44.
[16]张柽柽,胡明宝,邓少格,等.利用风廓线雷达资料对暴雨与低空急流关系的分析[J].气象水文海洋仪器,2011,28(1):32-35.
[17]金巍,曲岩,姚秀萍,等.一次大暴雨过程中低空急流演变与强降水的关系[J].气象,2007,33(12):31-38.
[18]李健,田军,栗敬仁.风廓线雷达在郑州机场一次持续雾霾过程的应用研究[C]//第34届中国气象学会年会S18气象雷达探测新技术与数据质控的业务应用论文集. 2017.
[19]牟惟丰.低空急流述评[J].气象科技,1998(4):7-12.
[20]赛瀚,苗峻峰.中国地区低空急流研究进展[J].气象科技,2012,40(5):766-771.
[21]李建辉.华南初夏的超低空急流及其对暴雨的影响[J].气象学报,1982,40(3):319-326.
[22]马福建.徐州冬季边界层低空急流的观测研究[J].气象科学,1983(2):41-46.
[23]李兴生,叶卓佳,刘林勤.夜间低空急流的分析研究[J].大气科学,1981,5(3):310-317.
[24]李兴生,朱翠娟,刘林勤,等.行星边界层中多极值风速廓线的研究[J].大气科学,1982,6(3):308-314.
[25]金维明,王学永,洪钟祥,等.夜间逆温条件下超低空急流的间歇性特征[J].大气科学,1983,7(3):296-302.
[26]丁一汇.高等天气学[M].北京:气象出版社,1991:573-586.
[27]陈楠,胡明宝,张柽柽,等.利用风廓线雷达资料对南京地区低空急流的统计分析[J].热带气象学报,2014,30(3):511-517.
[28]王东阡,张耀存.中国东部西南低空急流日变化特征及其机制[J].地球物理学报,2012,55(8):2 498-2 507.
[29] BLACKADAR A K. Boundary layer wind maxima and their significance for the growth of nocturnal inversions[J]. Bull Amer Meteor Soc,1957,38(5):283-290.
[30]何建中,伍荣生.边界层低空急流的数值研究[J].气象学报,1989,47(4):443-449.
[31]夏敏洁,周文君,裴海瑛,等.基于L波段雷达探空资料的南京低空逆温特征[J].大气科学学报,2017,40(4):562-569.
[32] UCCELLINI L W. On the role of upper tropospheric jet streaks and leeside cyclogenesis in the development of low-level jets in the Great Plains[J]. Mon Wea Rev,1980,108(10):1 689-1 696.
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