高原气象

高原气象 >

2018 , Vol. 37 >Issue 3: 826 - 836

DOI: https://doi.org/10.7522/j.issn.1000-0534.2018.00030

论文

塔克拉玛干沙漠腹地夜间稳定边界层观测个例分析

  • 张建涛 ,
  • 何清 ,
  • 王敏仲 ,
  • 金莉莉
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  • 新疆师范大学 地理科学与旅游学院, 新疆 乌鲁木齐 830054;中国气象局乌鲁木齐沙漠气象研究所, 新疆 乌鲁木齐 830002;塔克拉玛干沙漠大气环境观测试验站, 新疆 塔中 841000

收稿日期: 2017-10-25

  网络出版日期: 2018-06-28

基金资助

公益性行业（气象）科研专项[GYHY（QX）201506001-14]；国家自然科学基金项目（41575008，41775030，41605008）

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A Case Analysis of Nighttime Stable Boundary Layer Observation in the Hinterland of Taklimakan Desert

  • ZHANG Jiantao ,
  • HE Qing ,
  • WANG Minzhong ,
  • JIN Lili
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  • Xinjiang Normal University, Institute of geography and tourism, Urumqi 830054, Xinjiang, China;Institute of Desert Meteorology, China Meteorological Administration, Urumqi 830002, Xinjiang, China;Taklimakan Desert Atmosphere and Environment Observation Experiment Station, Tazhong 841000, Xinjiang, China

Received date: 2017-10-25

  Online published: 2018-06-28

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摘要

利用塔克拉玛干沙漠腹地2016年7月13-14日和26-27日GPS探空和地面气象观测资料，分析了塔克拉玛干沙漠夏季晴天夜间各气象要素垂直廓线特征。结果表明：夜间（21：00至次日08：00，北京时，下同）稳定边界层的厚度达到240 m。残余混合层最大厚度与前一天对流混合层厚度相当，随时间推移其厚度到10：15损耗近三分之一，残余逆温层顶盖厚度达到400 m；在残余逆温层顶盖和稳定边界层顶附近有风速极大值出现，而07：15稳定边界层顶附近有低空急流发展，其最大风速达到10.8 m·s-1；夜间低空处比湿的变化趋势是先增后减小再增大的过程，其最小值为2.95 g·kg-1，出现在04：15的稳定边界层顶附近。残余混合层内比湿随高度略微增大；夜间逆温层对水汽通量有阻挡和聚合的作用，使其在稳定边界层顶和残余混合层顶附近出现极大值，并于07：15达到最大值。垂直水汽通量于04：15在残余混合层中下部做下沉运动、上部和残余逆温层顶盖中做上升运动；同时，夜间陆面过程中，存在较强的辐射冷却和较小的摩擦速度，这也是形成较为浅薄的夜间稳定边界层主要的热力因素和湍流动力因素。

关键词： 塔克拉玛干沙漠; 夜间稳定边界层; 残余混合层; 低空急流; 水汽通量

本文引用格式

张建涛 , 何清 , 王敏仲 , 金莉莉 . 塔克拉玛干沙漠腹地夜间稳定边界层观测个例分析[J]. 高原气象, 2018 , 37(3) : 826 -836 . DOI: 10.7522/j.issn.1000-0534.2018.00030

Abstract

Based on the data of GPS sounding and ground weather observation data of 13-14 and 26-27 July 2016 in the hinterland of Taklimakan desert, the vertical profile characteristics of meteorological elements was analyzed in summer clear-sky Nighttime in this paper. It is revealed that the thickness of stable boundary layer is found to be 240 m at night[from 21:00 (Beijing time, the same as after) to the next day 08:00]. The maximum thickness of the residual mixing layer is the same as that of the convective mixing layer the previous day. Over time, the maximum thickness is lost about one third at 10:15, and the thickness of the residual temperature inversion layer top cover is up to 400 m; There is a maximum of wind speed in the residual temperature inversion layer top cover, near stable boundary layer roof, there develop a low-altitude jet stream whose maximum wind speed has reached 10.8 m·s-1 at 07:15; The change trend of specific humidity at the low altitude night is a process of increasing first, then decreasing and last increasing, and the minimum value is 2.95 g·kg-1, which has appeared near stable boundary layer roof at 04:15. Specific humidity of the residual mixed layer enlarges slightly with height; the night temperature inversion layer has the effect of blocking and polymerization on water vapor flux, and makes it appear the relative maximum value in nighttime near the top of stable boundary layer and residual mixing layer, which reaches the peak value at 07:15. The vertical water vapor flux does the sinking movement in the middle to lower part of residual mixing layer, whereas does the ascending motion in the upper part of residual mixing layer and residual temperature inversion layer top cover at 04:15; At the same time, there are quite strong radiation cooling and relatively small frictional velocity in the nocturnal land surface process, which are also the main thermodynamic factors and turbulent dynamic factors that form the relatively shallow nighttime stable boundary layer.

Key words： Taklimakan Desert; nighttime stable bou; residual mixing laye; a low-altitude jet s; water vapor flux

参考文献

[1]Axel V E, Teixeira J, 2013.A planetary boundary layer height climatology derived from ECMWF re-analysis data[J].J Climate, 26(17):6575-6590.
[2]Deardorff J W, 1970.Convective velocity and temperature scale for the unstable planetary boundary layer and for Rayleigh convection[J].J Atmos Sci, 27(8):1211-1213.
[3]Ebner L, Schr der D, Heinemann G, 2011.Impact of Laptev Sea flaw polynyas on the atmospheric boundary layer and ice production using idealized mesoscale simulations[J].Polar Res, 30(1):7210.
[4]Garcia-Carreras L, Parker D, Marsham J, et al, 2014.The turbulent structure and diurnal growth of the Saharan atmospheric boundary layer[J].J Atmos Sci, 72(2):693-713.
[5]Messager C, Parker D J, Reitebuch O, et al, 2010.Structure and dynamics of the Saharan atmospheric boundary layer during the West African monsoon onset:Observations and analyses from the research flights of 14 and 17 July 2006[J].Quart J Roy Meteor Soc, 136(S1):107-124.
[6]Stull R B, 1988. An introduction to boundary layer meteorology[M]. Dordrecht: Kluwer Academic Publisher, 2.
[7]Wang M Z, Wei W S, He Q, et al, 2016a.Summer atmospheric boundary layer structure in the hinterland of Taklimakan Desert[J].J Arid Land, 8(6):846-860.DOI:10.1007/s40333-016-0054-3.
[8]Wang M Z, Lu H, Ming H, et al, 2016b.Vertical structure of summer clear-sky atmospheric boundary layer over the hinterland and southern margin of Taklimakan Desert[J].Roy Meteor Soc, 23:438-447.DOI:10.1002/met.1568.
[9]He Q, Wei W S, Li X Y, et al, 2008.Profile characteristics of wind velocity, temperature and humidity in the surface layer during a sandstorm passing Taklimakan Desert hinterland[J].Desert Oasis Meteor, 2(6):6-11.<br/>何清, 魏文寿, 李祥余, 等, 2008.塔克拉玛干沙漠腹地沙尘暴过境时近地层风速、温度和湿度廓线特征[J].沙漠与绿洲气象, 2(6):6-11.
[10]He Q, Jin L L, Yang X H, et al, 2010.Analysis on O<sub>3</sub> concentration and affecting factors for boundary-layer in Hinterland of Taklimakan Desert in Autumn[J].Plateau Meteor, 29(1):214-221.<br/>何清, 金莉莉, 杨兴华, 等, 2010.秋季南疆沙漠塔中边界层O<sub>3</sub>浓度及影响因子分析[J].高原气象, 29(1):214-221.
[11]Li J G, Ao Y H, Li Z G, et al, 2014.Characteristics of atmospheric boundary layer over the Badain Jaran Desert in Summer[J].J Desert Res, 34(2):488-497.DOI:10.7522/j.issn.1000-694X.2013.00342.<br/>李建刚, 奥银焕, 李照国, 等, 2014.巴丹吉林沙漠夏季大气边界层结构[J].中国沙漠, 34(2):488-497.
[12]Li Z G, Lü S H, Wen L J, et al, 2016.Influence of incursion of dry cold air on atmospheric boundary layer process in Ngoring Lake Basin[J].Plateau Meteor, 35(5):1200-1211.DOI:10.7522/j.issn.1000-0534.2015.00076.<br/>李照国, 吕世华, 文莉娟, 等, 2016.一次干冷空气过境对鄂陵湖地区大气边界层过程的影响[J].高原气象, 35(5):1200-1211.
[13]Li Y Y, Zhang Q, Zhang A P, et al, 2016.Analysis on atmosphere boundary layer variation characteristics and their impact factors in arid region and semi-arid region over Northwest China[J].Plateau Meteor, 35(2):385-396.DOI:10.7522/j.issn.1000-0534.2014.00153.<br/>李岩瑛, 张强, 张爱萍, 等, 2016.干旱半干旱区边界层变化特征及其影响因子分析[J].高原气象, 35(2):385-396.
[14]Liu Y Q, He Q, Zhang H S, et al, 2011.Studies of land-atmosphere interaction parameters in Taklimakan Desert Hinterland[J].Plateau Meteor, 30(5):1294-1299.<br/>刘永强, 何清, 张宏升, 等, 2011.塔克拉玛干沙漠腹地地气相互作用参数研究[J].高原气象, 30(5):1294-1299.
[15]Liu Q, He Q, Yang X H, et al, 2009.Vertical distribution characteristic of winter atmospheric stability over the Hinterland of Taklimakan Desert[J].J Arid Meteor, 27(4):308-313.<br/>刘强, 何清, 杨兴华, 等, 2009.塔克拉玛干沙漠腹地冬季大气稳定度垂直分布特征分析[J].干旱气象, 27(4):308-313.
[16]Qiao J, Zhang Q, Zhang J, et al, 2010.Comparison of atmospheric boundary layer in winter and summer over arid region of Northwest China[J].J Desert Res, 30(2):422-431.<br/>乔娟, 张强, 张杰, 等, 2010.西北干旱区冬、夏季大气边界层结构对比研究[J].中国沙漠, 30(2):422-431.
[17]Wan Y X, Zhang Y, Zhang J W, et al, 2017.Influence of sensible heat on planetary boundary layer height in East Asia[J].Plateau Meteor, 36(1):173-182.DOI:10.7522/j.issn.1000-0534.2016.00001.<br/>万云霞, 张宇, 张瑾文, 等, 2017.感热变化对东亚地区大气边界层高度的影响[J].高原气象, 36(1):173-182.
[18]Wang M Z, Wei W S, Wei G, et al, 2014.Detection study of dust weather and clear-air turbulence in the hinterland of the Taklimakan Desert using a wind-profiling Radar[J].Remote Sens Technol Appli, 29(4):581-586.DOI:10.11873/j.issn.1004-0323.2014.4.0581.<br/>王敏仲, 魏文寿, 魏刚, 等, 2014.风廓线雷达对塔克拉玛干沙漠沙尘及晴空湍流的探测研究[J].遥感技术与应用, 29(4):581-586.
[19]Yang X H, He Q, Ajiguli S, et al, 2011.Character analysis of boundary layer during a sandstorm in hinterland of the Taklimakan Desert[J].Desert Oasis Meteor, 5(6):11-15.<br/>杨兴华, 何清, 阿吉古丽·沙依提, 等, 2011.塔克拉玛干沙漠腹地沙尘暴过程的大气边界层特征分析[J].沙漠与绿洲气象, 5(6):11-15.
[20]Zhang Q, Wang S, 2008.A study on atmospheric boundary layer structure on a clear day in the arid region in northwest China[J].Acta Meteor Sinica, 66(4):599-608.<br/>张强, 王胜, 2008.西北干旱区夏季大气边界层结构及其陆面过程特征[J].气象学报, 66(4):599-608.
[21]Zhang Q, 2007.Study on depth of atmospheric thermal boundary layer in extreme arid desert regions[J].J Desert Res, 27(4):614-620.<br/>张强, 2007.极端干旱荒漠地区大气热力边界层厚度研究[J].中国沙漠, 27(4):614-620.
[22]Zhao J H, Zhang Q, Wang S, et al, 2013.Studies on frequency density of inversion intensity and height of atmospheric boundary layer in arid region of Northwest China[J].Plateau Meteor, 32(2):2377-2386.DOI:10.7522/j.issn.1000-0534.2012.00037.<br/>赵建华, 张强, 王胜, 等, 2013.西北干旱区夏季大气边界层逆温强度和高度的频率密度研究[J].高原气象, 32(2):2377-2386.
[23]Zhao C L, Lü S H, Han B, et al, 2016.Relationship between the convective boundary layer and residual layer over Badain Jaran Desert in summer[J].Plateau Meteor, 35(4):1004-1014.DOI:10.7522/j.issn.1000-0534.2015.00080.<br/>赵采玲, 吕世华, 韩博, 等, 2016.夏季巴丹吉林沙漠残余层与深厚对流边界层的关系研究[J].高原气象, 35(4):1004-1014.
[24]Zhou M Y, Xu X D, Bian L G, et al, 2000.Observation analysis and kinetics study of planetary boundary layer on the Tibet Plateau[M].Beijing:China Meteorological Press.<br/>周明煜, 徐祥德, 卞林根, 等, 2000.青藏高原大气边界层观测分析与动力学研究[M].北京:气象出版社.
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