大涡模式分辨率对海洋信风区大气边界层结构和演变模拟的影响

任燕; 黄倩; 张君霞; 王婵

doi:10.16032/j.issn.1004-4965.2018.01.003

大涡模式分辨率对海洋信风区大气边界层结构和演变模拟的影响

doi: 10.16032/j.issn.1004-4965.2018.01.003

任燕¹,
黄倩^2, ,,
张君霞²,
王婵³

1.
北京大学物理学院大气与海洋科学系，北京 100871
2.
兰州大学半干旱气候变化教育部重点实验室/兰州大学大气科学学院，甘肃兰州 730000
3.
寒旱区陆面过程与气候变化重点实验室/中国科学院西北生态环境资源研究院，甘肃兰州 730000

基金项目:

国家自然科学基金项目 41775013

国家自然科学基金项目 41275006

国家自然科学基金项目 41205007

详细信息

通讯作者:
黄倩，女，甘肃省人，副教授，博士，硕士研究生导师，主要从事大气边界层湍流和沙尘传输的研究。E-mail: qianhuang@lzu.edu.cn

中图分类号: P435.1
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出版历程
- 收稿日期: 2016-10-28
- 修回日期: 2017-09-18
- 刊出日期: 2018-02-01

EFFECT OF LARGE EDDY RESOLUTION ON SIMULATION OF STRUCTURE AND EVOLUTION OF THE MARINE TRADE-WIND BOUNDARY LAYER

1.
Department of Atmospheric and Oceanic Sciences, School of Physics, Peking University, Beijing 100871, China
2.
Key Laboratory for Semi-Arid Climate Change of the Ministry of Education, College of Atmospheric Sciences, Lanzhou University, Lanzhou 730000, China
3.
Laboratory of Land Surface Process and Climate Change in Cold and Arid Regions, Northwest Institute of Eco-Environment and Resources, CAS, Lanzhou 730000, China

摘要

摘要: 利用BOMEX（巴巴多斯海洋与气象学试验）的探空资料和LEM（大涡模式），通过改变LEM水平分辨率的敏感性数值试验，对比分析不同尺度的湍涡对信风积云边界层中混合层和云层的结构、演变以及对流形式和强度的影响。结果表明，水平分辨率较高时模拟的湍涡尺度较小、混合层顶的夹卷作用较强，模拟的混合层较暖、较干，而且模拟的对流泡尺度较小、强度较大，能够模拟出较精细的边界层结构；而水平分辨率较低时则相反。模拟的湍涡尺度对海洋信风区边界层积云中液态水混合比的模拟结果影响较大：LEM模拟的湍涡尺度较小时模拟的信风积云形成的时间较早、云顶高度较高，单个云块的体积较小但数目较多，液态水含量较高；而模拟的湍涡尺度较大时则相反。虽然水平分辨率为50 m和125 m的试验都能模拟出较精细的信风边界层中混合层、云层的结构和演变特征，但是，考虑到提高分辨率在模拟过程中产生的噪音信号对结果的影响以及计算时间等问题，LEM采用125 m的水平网格距是对海洋信风边界层积云对流模拟较为理想的选择。
- 大气物理学 /
- 边界层结构 /
- 大涡模式 /
- 信风积云 /
- 模式分辨率
Abstract: The effects of turbulent eddies with various scales on the structure and evolution of mixed layer and cumulus layer are analyzed by using the sounding data from the Barbados Oceanographic and Meteorological Experiment (BOMEX) and a large eddy simulation (LEM) sensitivity test with different horizontal grid spacings. The results showed that a fine structure of the boundary layer convection with a warm and dry mixed layer is simulated with smaller model horizontal grid spacings. Strong convection and entrainment also were modeled using high-resolution tests due to small turbulent eddies being resolved. If larger model horizontal grid spacings were used, larger turbulent eddies led to a weaker boundary layer convection with cooler and wetter mixed layer and weaker entrainment. The simulated scale of turbulent eddies were also shown to affect the simulation of liquid water mixing ratio in the trade-wind cumulus layer. If small turbulent eddies were modeled, this led to an early formation of trade-wind cumulus and a high cloud top. Large liquid water content with small volume of single cloud was found in the trade-wind cumulus layer. It gave the opposite results if large turbulent eddies were simulated. Considering the effects of noise signals generated by the high resolution simulations and computing time, the use of 100 m grid spacing as LEM horizontal resolution in simulating marine trade-wind cumulus boundary layer is a ideal choice, although the characteristics of mixed layer and cumulus layer from a fine trade-wind boundary layer could be modeled by using the simulation with 50 m or 100 m grid spacings.
- atmospheric physics /
- boundary layer structure /
- large eddy simulation /
- trade-wind cumulus /
- model resolution

HTML全文

图 1 平均位温θ和水汽混合比q_v廓线（a，实线为初始廓线，点线和虚线分别为模拟3 h和7 h的结果）和风廓线（b）

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图 2 不同水平分辨率敏感性试验模拟的1 h、2 h、3 h、5 h（a~d）后的混合层虚位温（实线）、水汽混合比（虚线）的平均廓线

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图 3 不同水平分辨率敏感性试验模拟的1 h、2 h、3 h、5 h（a~d）后的混合层中的浮力通量平均廓线

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图 4 模拟3 h后垂直速度（左）、虚位温（中）和水汽混合比（右）的概率密度函数分布

a1、b1、c1为180 m高度; a2、b2、c2为360 m高度; a3、b3、c3为540 m高度。蓝色、绿色、红色和黑色分别代表试验R50、R125、R200和R500的结果。

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图 5 试验R50、R125、R200、R500（a~d）的敏感性试验模拟的3 h后垂直速度Y-Z剖面

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图 6 不同水平分辨率敏感性数值试验模拟3 h后垂直速度（左）、虚位温（中）、水汽混合比（右）的概率密度函数分布

a1、b1、c1为900 m高度; a2、b2、c2为1 200 m高度; a3、b3、c3为1 500 m高度。蓝色、绿色、红色和黑色分别代表试验R50、R125、R200和R500的值。

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图 7 不同水平分辨率敏感性数值试验模拟的总云覆盖率（a）和云底高度（点线）、云顶高度（实线）随时间的变化（b）

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图 8 不同水平分辨率敏感性试验模拟1 h、2 h、3 h、5 h后（a~d）的液态水混合比平均廓线

单位：mg/kg。

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图 9 试验R50、R125、R200、R500(a~d)的敏感性试验模拟的3 h后液态水混合比的X-Y剖面

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参考文献(43)

[1]	TIEDTKE M, HECKLEY W A, SLINGO J. Tropical forecasting at ECMWF: The influence of physical parameterizations on the mean structure of forecasts and analyses[J]. Q J Roy Meteorol Soc, 1988, 114(481): 639-664.
[2]	NEGGERS R A J, NEELIN J D, STEVENS B. Impact mechanisms of shallow cumulus convection on tropical climate dynamics[J]. J Clim, 2007, 20(11): 2 623-2 642.
[3]	WOOD R, BRETHERTON C S. Boundary layer depth, entrainment, and decoupling in the cloud-capped subtropical and tropical marine boundary layer[J]. J Clim, 2004, 17(18): 3 576-3 588.
[4]	GHATE V P, MILLER M A, DIPRETORE L. Vertical velocity structure of marine boundary layer trade wind cumulus clouds[J]. J Geophys Res, 2011, 116(116): 971-978.
[5]	DUSSEN J J, ROODE S R, ACKERMAN A S, et al. The GASS/EUCLIPSE model intercomparison of the stratocumulus transition as observed during ASTEX: LES results[J]. J Adv Model Earth Syst, 2013, 5(3): 483-499.
[6]	DAVIDSON B. The Barbados oceanographic and meteorological experiment[J]. Bull Am Meteor Soc, 1968, 49(7): 928-934.
[7]	AUGSTEIN E, RIEHL H, OSTAPOFF F, et al. Mass and energy transports in an undisturbed Atlantic trade-wind flow[J]. Mon Wea Rev, 1973, 101(2): 101-111.
[8]	NITTA T, ESBENSEN S. Heat and moisture budget analyses using BOMEX data[J]. Mon Wea Rev, 1974, 102(1): 17-28.
[9]	LEMONE M A, PENNELL W T. The relationship of trade wind cumulus distribution to subcloud layer fluxes and structure[J]. Mon Wea Rev, 1976, 104(5): 524-539.
[10]	LEMONE M A. The marine boundary layer[M]//Workshop on the planetary boundary. Boston: Amer Meteor Soc, 1980: 192-231.
[11]	GHATE V P, MILLER M A, ZHU P. Differences between nonprecipitating tropical and trade wind marine shallow cumuli[J]. Mon Wea Rev, 2015, 144(2): 681-701.
[12]	温晓培, 隆霄, 张述文, 等.边界层参数化方案对台风SANBA初生阶段影响的数值模拟研究[J].热带气象学报, 2016, 32(3):358-367.
[13]	BRILL K, ALBRECHT B. Diurnal variation of the trade-wind boundary layer[J]. Mon Wea Rev, 1982, 110(6): 601-613.
[14]	赵春生, 石坂隆.层积云覆盖的海洋边界层云详细微物理过程的数值模拟[J].气象学报, 2004, 62(1):87-95.
[15]	SIEBEMA A P, CUIJPERS J W M. Evaluation of Parametric Assumptions for shallow cumulus convection[J]. J Atmos Sci, 1995, 52(6): 650-666.
[16]	JIANG H, COTTON W R. Large eddy simulation of shallow cumulus convection during BOMEX: Sensitivity to microphysics and radiation[J]. J Atmos Sci, 2000, 57(4): 582-594.
[17]	NUIJENS L, STEVENS B. The influence of wind speed on shallow marine cumulus convection[J]. Atmos Sci, 2012, 69(69): 168-184.
[18]	GRAY M E B, PETCH J, DERBYSHIRE S H, et al. Version 2.3 of the Met Office large eddy model[M]. Exeter in UK: The Met Office, 2001.
[19]	黄倩, 王蓉, 田文寿, 等.风切变对边界层对流影响的大涡模拟研究[J].气象学报, 2014, 72(1): 100-115.
[20]	STEVENS B. Atmospheric moist convection[J]. Ann Rev Earth Planet Sci, 2004, 33(33): 605-643.
[21]	刘艳, 唐南军, 杨学胜.利用COSMIC/GPS掩星折射率资料研究海洋边界层高度的特点[J].热带气象学报, 2015, 31(1): 43-50.
[22]	吕乃平, 李诗明, 苏立荣.赤道西太平洋的边界层特性和通量计算[J].海洋学报, 1990, 12(5): 571-580.
[23]	HIGNETT P. Observations of diunal variation in a cloud-capped marine boundary layer[J]. J Atmos Sci, 1940, 48(12): 1 474-1 482.
[24]	MOENG C H, ROTUNNO R. Vertical velocity skewness in the buoyancy drive boundary layer[J]. J Atmos Sci, 1990, 47(9): 1 147-1 162.
[25]	LEMONE M A. Some observations of vertical velocity skewness in the convective planetary boundary layer[J]. J Atmos Sci, 1990, 47(9): 1 163-1 169.
[26]	QIANHUANG, J H MARSHAM, D J PARKER, et al. A comparison of roll and convection and the subsequent deepening moist convection: An LEM case study based on SCMS data[J]. Mon Wea Rev, 2009, 137(1): 350-365.
[27]	徐华英, 李桂忱.有云泡结构的对流云中降水形成的研究[J].气象学报, 1980, 38(3): 260-268.
[28]	王昂生, 赵小宁, 康玉霞, 等.昔阳地区冰雹云形成过程的一些特征[J].大气科学, 1980, 4(2): 186-194.
[29]	陈添宇, 郑国光, 陈跃, 等.祁连山夏季西南气流背景下地形云形成和演化的观测研究[J].高原气象, 2010, 29(1): 152-163.
[30]	肖辉, 王孝波, 周非非, 等.强降水云物理过程的三维数值模拟研究[J].大气科学, 2004, 28(3): 385-404.
[31]	王建捷, 李泽椿. 1998年一次梅雨锋暴雨中尺度对流系统的模拟与诊断分析[J].气象学报, 2002, 60(2): 146-155.
[32]	高会旺, 黄美元, 余方群.大气污染物对流垂直输送作用的探讨[J].环境科学, 1998(4): 1-4.
[33]	金祺, 银燕, 谭稳.黄山地区复杂地形下污染气体输送过程的数值模拟[J].大气科学学报, 2012, 35(6): 680-688.
[34]	陈杨瑞雪, 罗亚丽.不同边界层参数化方案和陆面过程参数化方案对一次梅雨锋暴雨显式对流模拟的影响分析[J].热带气象学报, 2016, 32(5):656-667.
[35]	TIAN W S, PARKER D J, D KILBURN C A. Observations and numerical simulation of atmosphere cellular convection over mesoscale topography[J]. Mon Wea Rev, 2002, 131(1): 222-235.
[36]	DELNORE V E. Diurnal variation of temperature and energy budget for the oceanic mixed layer during Bomex[J]. J Phys Oceanogr, 1972, 2(3): 239-247.
[37]	王蓉, 黄倩, 田文寿, 等.边界层对流对示踪物抬升和传输影响的大涡模拟研究[J].大气科学, 2015, 39(4):731-746.
[38]	CHOW F K, MOIN P. A further study of numerical errors in large-eddy simulations[J]. J Computat Phys, 2003, 184(2): 366-380.
[39]	MEDEIROS B, STEVENS B, HELD I M, et al. Aquaplanets, climate sensitivity, and low clouds[J]. J Clim, 2008, 21(19): 4 974-4 991.
[40]	WANG H, FEINGOLD G. Modeling mesoscale cellular structures and drizzle in marine stratocumulus, Part Ⅰ: Impact of drizzle on the formation and evolution of open cells[J]. J Atmos Sci, 2009, 66(11): 3 237-3 256.
[41]	XUEWEN H, FEINGOLD G, STEVENS B. Aerosol effects on clouds, precipitation, and the organization of shallow cumulus convection[J]. J Atmos Sci, 2008, 65(2): 392-406.
[42]	YAMAGUCHI T, RANDALL D A, KHAIROUTDINOV M F. Cloud modeling tests of the ULTIMATE-MECHO scalar advection scheme[J]. Mon Wea Rev, 2011, 139(10): 3 248-3 264.
[43]	BROWN A R. The sensitivity of large eddy simulations of shallow cumulus convection toresolution and subgridmodel[J]. Q J R Meteorol Soc, 1999, 125(554): 469-482.