毛乌素沙地南缘凝结水观测实验分析

J4 ›› 2008, Vol. 26 ›› Issue (3): 8-13.

毛乌素沙地南缘凝结水观测实验分析

张晓影^{1, 2} ,李小雁^{1, 2} ,王　卫² ,马育军²

1. 北京师范大学,地表过程与资源生态国家重点实验室,北京　100875;2. 北京师范大学资源学院土地资源研究所,北京　100875

收稿日期:2008-05-21 出版日期:2008-09-30 发布日期:2008-09-30
作者简介:张晓影(1984 - ) ,女,河南开封人,在读硕士,主要从事水文与水资源研究. E-mail: zhangxiaoying@ires. cn
基金资助:
:全国优秀博士学位论文作者专项资金(200426) 、国家自然科学基金(40571023) 、国家十一五科技支撑项目( 2006BAD26B0701)资助

Exper imen ta lObserva tion Ana lysis on Dew Forma tion in Southern M u us Sandy Land

ZHANG Xiaoying^1,2 , L I Xiaoyan^1,2 , WANGWei² , MA Yujun²

1. S tate Key Laboratory of Earth Surface Processes and Resource Ecology, B eijing N orm al University, B eijing 100875, China;
2. Institute of Land Resources, College of Resources Sciences and Technology, B eijing N orm al University, B eijing 100875, China

Received:2008-05-21 Online:2008-09-30 Published:2008-09-30

摘要/Abstract

摘要：

采用称重法对2007年8月期间毛乌素沙地南缘不同地表类型(改良沙地、生物结皮、物理结皮和流沙) 、沙丘不同部位的凝结水形成动态过程进行了系统观测。结果表明:改良沙地凝结水量达0. 206 mm /d,显著大于生物结皮、物理结皮和流沙,生物结皮凝结水量为0. 100 mm /d,显著高于流沙,而其他两者之间凝结水量无显著性差异;沙丘不同部位凝结水量差异显著,丘间地凝结水量最大,沙丘坡面次之,沙丘顶部最少,日凝结水量分别为0. 0873 mm /d、0. 0768 mm /d和0. 0674 mm /d;从凝结水形成过程看出凝结水一般在每天17: 00产生,次日7: 00结束,在夜晚21: 00和凌晨3: 00左右出现2个凝结水较大值;凝结水的形成与气象因子密切相关,凝结水量与地表温度、大气和地表温度差以及净辐射具有显著相关性。

关键词: 凝结水观测, 改良沙地, 不同沙地表层, 毛乌素沙地中

Abstract:

Measurements of dew were carried out on four different soil surfaces ( biological soil crust, physical soil crust, bare sand and imp roved sandy soil) and different locationswithin a dune inMu us SandyLand in August 2007. Moreover, the p rocess of dew formation within a day was also observed. The results indicated that the characteristic of particle size was a determining factor for the dew amount for the different soil surfaces, the imp roved sandy soil had highest dew amount because it had a higher content of silt, and the dew amount of biological crust is significant higher than that of the bare dune sand. In general, dew begins at 17: 00 and ends at 7: 00,which correlated with the land surface temperature, the difference between air temperature and land surface temperture, net radiation on an hour time scale, and temperature daily range. The dew amount also changes with different locations of a dune, the dew amount in the top of the dune is least ( 0. 066 mm) , andmost (0. 100 mm) in foot slope of the dune, the resultmay relate to the sun radiation.

Key words: dew observation, imp roved soil, different soil surfaces, Mu us Sandy Land

中图分类号:

P412. 13

张晓影, 李小雁, 王　卫, 马育军. 毛乌素沙地南缘凝结水观测实验分析[J]. J4, 2008, 26(3): 8-13.

ZHANG Xiao-Ying, LI Xiao-Yan, WANG 　Wei, MA Yo-Jun. Exper imen ta lObserva tion Ana lysis on Dew Forma tion in Southern M u us Sandy Land[J]. J4, 2008, 26(3): 8-13.

参考文献

[ 1 ] 蒋瑾,王康富,张维静. 沙地凝结水及在水分平衡中的作用[ J ].干旱区研究, 1993, 10 (2) : 1 - 9.
[ 2 ] 阎百兴, 邓伟. 三江平原露水资源研究[ J ]. 自然资源学报,2004, 19 (6) : 732 - 737.
[ 3 ] BarradasV L, Glez - MedellínM G. Dew and its effect on two heliophile under storey species of a trop ical dry deciduous forest in
Mexico [ J ]. Int J Biometeorol, 1999, 43: 1 - 7.
[ 4 ] JacobsA F G. Dew deposition and drying in a desert system: a simp le simulation model[ J ]. Journal of Arid Environments, 1999, 42:211 - 222.
[ 5 ] 陈荷生,康跃虎. 沙坡头地区凝结水及其在生态环境中的意义[ J ]. 干旱区研究, 1992, 6 (2) : 64 - 72.
[ 6 ] Kidron G J, Ilana Herrnstadt, Eldad Barzilay. The role of dew as amoisture source for sand icrobiotic crusts in the Negev Desert Israel
[ J ]. Journal of Arid Environments, 2002, 52: 517 - 533.
[ 7 ] 郭占荣,刘建辉. 中国干旱半干旱地区土壤凝结水研究综述[ J ]. 干旱区研究, 2005, 22 (4) : 576 - 580.
[ 8 ] Ninari N, Berliner P R. The role of dew in the water and heat balance of bare loess soil in the Negev Desert: quantifying the actual
dew deposition on the soil surface [ J ]. Atmospheric Research,2002, 64: 323 - 334.
[ 9 ] Kalthoffa N, Fiebig - wittmaack M, Meiβner C, et al. The energy balance, evapo - transp iration and nocturnal dew deposition of an
arid valley in the Andes[ J ]. Journal of Arid Environments, 2006,65: 420 - 443.
[ 10 ] Agam N, Berliner P R. Dew formation and water vapor adsorp tion in semi - arid environments - A review [ J ]. Jounral ofArid Environments, 2006, 65: 572 - 590.
[ 11 ] AlnaserW E, Barakat A. Use of condensed water vapor from the atmosphere for irrigation in Bahrain [ J ]. App lied Energy, 2000,65: 3 - 18.
[ 12 ] BeysensD, Clusc O, MiletacM, et al. Collecting dew as a water source on small islands: the dew equipment forwater p roject in Bis
evo (Croatia) [ J ]. Energy, 2007, 32: 1032 - 1037.
[ 13 ] JacobsAdrie F G, Heusinkveld B G, Berkowicz SM. Dew deposition and drying in a desert system: a simp le simulation model [ J ].
Journal ofArid Environments, 1999, 42: 211 - 222. .
[ 14 ] MoroM J. Were A, Villagarc L, et al. Dew measurement by Eddym covariance and wetness sensor in a semiarid ecosystem of SE Spain
[ J ]. Journal of Hydrology, 2007, 335: 295 - 302.
[ 15 ] 张兴鲁. 干旱地区沙丘水汽凝结及其重要意义[ J ]. 地下水,1986 (6) : 39 - 42.
[ 16 ] 周金龙,艾克日木. 阿不都拉,董新光. 天山北麓平原区凝结水的观测实验分析[ J ]. 新疆农业大学学报, 2002, 25 ( 1) : 49 -53.
[ 17 ] 王胜,张强,张鸿. 稀疏植被地表反照率及土壤热传导率特征研究[ J ]. 中国沙漠, 2008, 1 (28) : 119 - 124.
[ 18 ] 邓辉. 人类活动的影响导致了毛乌素沙地向南扩大吗[ J ]. 陕西师范大学学报(哲学社会科学版) , 2007, 36 (5) : 11 - 12.
[ 19 ] 张建山. 沙漠滩区凝结水补给机理研究[ J ]. 地下水, 1995, 17(2) : 76 - 77.
[ 20 ] 张建山,仵彦卿,李哲. 陕北沙漠滩区降水入渗与凝结水补给机实验研究[ J ]. 水土保持学报, 2005, 19 (5) : 124 - 126.
[ 21 ] Li X Y. Effect of gravel and sand mulches on dew deposition in the semiarid region of China [ J ]. Hydrol, 2002 (260) : 151 - 160.
[ 22 ] 于庆和. 塔里木盆地北东缘群克地区土壤凝结水的初步研究[ J ]. 干旱区地理, 1992, 15 (3) : 77 - 84.
[ 23 ] 刘利霞,张宇清,吴斌. 生物结皮对荒漠地区土壤及植物的影响研究述评[ J ]. 中国水土保持科学, 2007, 5 (6) : 106 - 112.
[ 24 ] Kidron G J. Analysis of dew p recip itation in three habitatswithin a small arid drainage basin, Negev Highlands. Israel [ J ]. Atmospheric Research, 2000, 55: 257 - 270.
[ 25 ] 王志,王蕾,刘连友. 毛乌素沙地南缘沙丘水分的时空分布特征[ J ]. 干旱区研究, 2007, 24 ( l) : 61 - 65.
[ 26 ] 方静,丁永建. 荒漠绿洲边缘凝结水量及其影响因子[ J ]. 冰川冻土, 2005, 27 (5) : 755 - 760.
[ 27 ] Ye Y H, Zhou K, Song L Y, et al. Dew amounts and its correlationswith meteorological factors in urban landscapes of Guangzhou,
China[ J ]. Atmosphere research (Article in p ress)