TURBULENT MEASUREMENT OVER THE SOUTHEASTERN TIBETAN PLATEAU

Bian Lingen; Lu Longhua; Cheng Yanjie; Lu Changgui; Yao Zhanyu; Xu Qiangde; Chen Lianshou

Vol.12, NO.1, 2001

Article Contents

Article Navigation > Journal of Applied Meteorological Science > 2001 > 12(1): 1-13

Bian Lingen, Lu Longhua, Cheng Yanjie, et al. Turbulent measurement over the southeastern Tibetan Plateau. J Appl Meteor Sci, 2001, 12(1): 1-13.

Citation:

Bian Lingen, Lu Longhua, Cheng Yanjie, et al. Turbulent measurement over the southeastern Tibetan Plateau. J Appl Meteor Sci, 2001, 12(1): 1-13.

Bian Lingen, Lu Longhua, Cheng Yanjie, et al. Turbulent measurement over the southeastern Tibetan Plateau. J Appl Meteor Sci, 2001, 12(1): 1-13.

Citation:

Bian Lingen, Lu Longhua, Cheng Yanjie, et al. Turbulent measurement over the southeastern Tibetan Plateau. J Appl Meteor Sci, 2001, 12(1): 1-13.

PDF( 216 KB)

TURBULENT MEASUREMENT OVER THE SOUTHEASTERN TIBETAN PLATEAU

Chinese Academy of Meteorological Sciences, Beijing 100081

Received Date: 1999-11-08
Rev Recd Date: 2000-03-07
Publish Date: 2001-02-28

Abstract

Abstract

Based on the second Tibetan Plateau Meteorological Experiment (TIPEX) turbulent data from Changdu, the turbulent structure and transportation characteristics in the near-surface layer for summer time are analyzed by using the eddy correlation technique. The main results show that the relation between the normalized variance of 3D winds and z/L satisfies the similarity law under both unstable and stable stratification. The relations of normalized variances of temperature and specific humidity to z/L obey the law of 1/3 fractional power only under the unstable condition. In the case of stable stratification, their relations to z/L are disperse. The sensible heat dominates in the dry period, making up 80% of the total heating; while in the wet period the heating is intensified to great degree, in which latent (sensible) heat constitutes 60% (40%). The relations of drag coefficients (C_d and C_h) to z/L are quite close and the fitted C_dn (4.40×10^-3) C_hn (4.70×10^-3) are obtained in a neutral case, which are bigger than those for the middle and western parts of the plateau in the same period.
- TIPEX;
- Eddy correlation;
- Turbulent structure;
- Drag coefficient

FullText(HTML)

References(18)

Figures and Tables

图 1 (a) 超声风温仪DA 600的水平合成风速V_c与风洞风速V_t的比较, (b) E009B红外水汽测量仪输出电压 (V) 与比湿 (q) 的关系

(图中1和2为测试点)

DownLoad: Full-Size Img PowerPoint

图 2 1998年5月20日15:00三维风u (a), w (b), 温度 (c) 和湿度 (d) 的湍流谱

DownLoad: Full-Size Img PowerPoint

图 3 干期 (圆点) 和湿期 (三角) 0.5～8 m的温度差 (a) 和比湿差 (b) 的平均日变化

DownLoad: Full-Size Img PowerPoint

图 4 湍流强度 (a) 干期, (b) 湿期 (实线: I_u, 虚线: I_v, 点线: I_w) 和 (c) 稳定度 (实线: 干期, 虚线: 湿期)的平均日变化

DownLoad: Full-Size Img PowerPoint

图 5 三维风速归一化的标准方差与z/L的关系[a, b: y=3.45 (1-3z/L) ^1/3; c, d: y=3.15 (1-3z/L) ^1/3; e, f: y=1.30 (1-3z/L) ^1/3]

DownLoad: Full-Size Img PowerPoint

图 6 归一化的温度方差e_T/|T*|和e_q/q*与z/L的关系[a, b: y=1.0 (1-3z/L) ^-1/3; c, d: y=5.3 (1-3z/L) ^1/3]

DownLoad: Full-Size Img PowerPoint

图 7 1998年5月18日00:00～6月30日24:00感热通量 (Q_H) 和潜热通量 (Q_E) 逐时变化

DownLoad: Full-Size Img PowerPoint

图 8 干期 (a) 和湿期 (b) 的感热通量 (Q_H) (实线) 和潜热通量 (Q_E) (虚线) 平均日变化

DownLoad: Full-Size Img PowerPoint

图 9 干期 (实线) 和湿期 (虚线) 的风速 (U) 和动量通量 (f) 的平均日变化

DownLoad: Full-Size Img PowerPoint

图 10 C_D和C_H与z/L的关系

DownLoad: Full-Size Img PowerPoint

表 1 湍流测量系统传感器的主要技术指标

表 2 近中性条件无因次风速方差值

表 3 昌都的平均热源强度

References

[1]	章基嘉, 朱抱真, 朱福康, 等.青藏高原气象学进展.北京:科学出版社, 1988.1~268.
[2]	Tsukamoto O, Sahashi K, Wang J.Heat budget and evapotranspiration at an Oasis surface surroundinged by desert.J.Met.Soc.Japan, 1995, 73(5):925~935.
[3]	周秀骥, 陶善昌, 姚克亚.高等大气物理学.北京:气象出版社, 1991.206~236.
[4]	Panafsky H A, Larko D, Lipschutz R, et al.Spectra of velocity components and complex terrain.Quart J.R.Meteor Soc., 1982, 108:215~230. doi: 10.1002/(ISSN)1477-870X
[5]	Kaimal J C, Wyngaard J C, Izumi Y, et al.Spectral characteristics of surface layer turblence.Quart J.R.Meteor.Soc., 1972, 98:563~589. doi: 10.1002/(ISSN)1477-870X
[6]	Panafsky H A, Dutton J A.Atomspheric Turbulence.New York:John Willy and Sons, 1984.10~50.
[7]	Hedde T, Darand P.Turbulence intensities and bulk coefficients in the surface layer above sea.Boundary Layer Meteorology, 1994, 71:415~432. doi: 10.1007/BF00712178
[8]	Wyngaard J C, Cote O R.Volution of a convective planetary bound rylayer-a high-order-closure model study.Boundary Layer Meteorology, 1974, 7:290~307.
[9]	祁永强, 王介民.青藏高原五道梁地区湍流输送特征的研究.高原气象, 1996, 15(2):172~177. http://www.cnki.com.cn/Article/CJFDTOTAL-GYQX602.005.htm
[10]	Panafsky H A, Tenekes H, Lenschow D H, et al.The characteristics of turbulent velocity components in the surface layer under convective conditions.Boundary Layer Meteorology, 1977, 21:356~360. doi: 10.1007/BF00121926?no-access=true
[11]	Hirohiko I, Taichi H, Kenji T, et al.Summary of planetary boundary Layer observation in GAME/TIBET.Proceedings of the 1st international workshop on GAME/Tibet, Xian, China, 11~13, Jan.1999, 69~76.
[12]	王介民, 刘晓虎, 马耀民.HEIFE戈壁地区近地层大气湍流结构和输送特征.气象学报, 1993, 51(3):343~349. http://www.cnki.com.cn/Article/CJFDTOTAL-QXXB199303009.htm
[13]	Hogstrom U, Semdman-Hogstrom A S.Turbulence mechanics at an agricultural site.Boundary layer Meteorology, 1974, 7:374~388.
[14]	朱福康, 赵卫.青藏高原地面净辐射对大气环流作用的一些观测事实.青藏高原气象科学实验文集 (三).北京:科学出版社, 1987.54~61.
[15]	李家伦, 洪钟祥, 罗卫东, 等.青藏高原改则地区近地层通量观测研究.大气科学, 1999, 23(2):142~151. http://www.cnki.com.cn/Article/CJFDTOTAL-DQXK199902001.htm
[16]	Mitsuta Y, Tsukamoto O.Drag coefficients in light wind, Bull.Disaster prevention Res.Inst., Kyoto Univ., 1978, 28(2):25~32.
[17]	李月洪, 李维亮, 丁晓蓉, 等.1993年7~9月拉萨近地层湍流输送特征的分析.亚洲季风研究的新进展.北京:气象出版社, 1996.26~27.
[18]	陈万隆, 翁笃鸣.关于青藏高原感热和潜热旬总量计算方法的初步研究.青藏高原气象科学实验文集 (二).北京:科学出版社, 1984.38~39.