沙尘天气下输沙率的野外观测与分析
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摘要
2014年7月—2014年8月借助风速仪、微梯度集沙仪,通过野外监测系统获取的试验数据,对塔中地区2014年7月—2014年8月沙尘天气过程中贴地层输沙率进行分析,得出:0～85 mm高度内,随着风速的增大,35～85 mm无论是绝对的输沙量还是相对的输沙量都减少。0～85 mm高度内,各层输沙率最大值均出现在风速为8 m·s-1左右,波动较为显著;最小值出现在6.5 m·s-1左右,波动不明显;沙尘天气中,输沙率最大值出现在5～15 mm高度,最小值出现在35～85 mm高度。扬沙天气中,风速>9.2 m·s-1时,输沙率最大值在0～5 mm处。沙尘暴天气,拐点风速为7.5 m·s-1,<7.5 m·s-1时,输沙率增加不显著,>7.5 m·s-1时,输沙率增加显著。通过微梯度集沙仪获得的上述试验数据是风沙工程设计的一个极重要工程参数,具有重要的实践意义。
We made continuous observation experiments of the sediment transport rate in Tazhong district,which is in the Taklamakan Desert hinterland. We analyzed the movement rules in the conditions of the different wind speed in the typical weather. The experiments were done by using H11-sensit wind sensor,anemometer,and micro-gradient sand sampler from July to August in 2014.The results showed that:In the height of 0～ 85 mm,with the increase of wind speed,the absolute sediment transport volume and relative sediment transport volume of 35 ～85 mm are reduced. In the height of 0 ～85 mm,the maximum sediment transport rate in each layer appears at a wind speed of 8 m·s-1,and the fluctuation is more significant;the minimum value appears at 6.5 m·s-1,and the fluctuation is not obvious. In the dusty weather, the maximum sand rate occurs at a height of 5 to 15 mm,and the minimum value appears at a height of 35 to 85 mm. In the sand blowing weather,when the wind speed is greater than 9.2 m·s-1,the maximum sediment transport rate is 0～5 mm. In the sandstorm weather,the wind speed at the inflection point is 7.5 m·s-1,and when the wind speed is less than 7.5 m·s-1,the sediment transport rate increases not significantly,and the sediment transport rate increases significantly when the wind speed is more than 7.5 m·s-1. The above test data obtained by the micro-gradient sand collector is a very important engineering parameter for the design of wind-blown sand engineering,and has important practical significance.
We made continuous observation experiments of the sediment transport rate in Tazhong district,which is in the Taklamakan Desert hinterland. We analyzed the movement rules in the conditions of the different wind speed in the typical weather. The experiments were done by using H11-sensit wind sensor,anemometer,and micro-gradient sand sampler from July to August in 2014.The results showed that:In the height of 0～ 85 mm,with the increase of wind speed,the absolute sediment transport volume and relative sediment transport volume of 35 ～85 mm are reduced. In the height of 0 ～85 mm,the maximum sediment transport rate in each layer appears at a wind speed of 8 m·s-1,and the fluctuation is more significant;the minimum value appears at 6.5 m·s-1,and the fluctuation is not obvious. In the dusty weather, the maximum sand rate occurs at a height of 5 to 15 mm,and the minimum value appears at a height of 35 to 85 mm. In the sand blowing weather,when the wind speed is greater than 9.2 m·s-1,the maximum sediment transport rate is 0～5 mm. In the sandstorm weather,the wind speed at the inflection point is 7.5 m·s-1,and when the wind speed is less than 7.5 m·s-1,the sediment transport rate increases not significantly,and the sediment transport rate increases significantly when the wind speed is more than 7.5 m·s-1. The above test data obtained by the micro-gradient sand collector is a very important engineering parameter for the design of wind-blown sand engineering,and has important practical significance.
引文
[1]刘新春.关于荒漠化研究几个问题的探讨[J].沙漠与绿洲气象,2007,1(1):27-31.
[2]张伟民,汪万福,张克存,等.不同沙源供给条件下砾石床面的风沙流结构与蚀积量变化风洞试验研究[J].中国沙漠,2009,29(6):1005-1010.
[3]夏建新,石雪峰,吉祖稳.植被覆盖条件下地表输沙率模型[J].应用基础与工程科学学报,2006,14(2):218-227.
[4]拜格诺,风沙和荒漠沙丘物理学[M].钱宁译.北京:科学出版社,1959:57-65.
[5]拓万全,杨根生.流动沙丘表面输沙率的理论计算方程[J].干旱区资源与环境,1996,10(4):50-54.
[6] Wolfe S A,Nickeling W G. The protective role of spares vegetation in wind erosion[J]. Progress in Physical Geography,1993,17(1):50-68.
[7] Wasson R J,Nanina P M. Estimating wind transport of sand on vegetated surfaces[J]. Earth Surface Process and Landforms,1986,N(11):505-514.
[8] Buckley R. The effect of sparse vegetation on the dune sand by wind[J]. Nature,1987,325:426-428.
[9] Land caster N,Baas A. Influence of vegetation on cover on sand transport by wind:field studies at Owens Lake,California[J]. Earth Surface Processes and Landforms,1982,23:69-82.
[10]黄福祥,牛海山,王明星,等.毛乌素沙地植被覆盖率与风蚀输沙率定量关系[J].地理学报,2001,56(6),700-710.
[11]程皓,李霞,侯平,等.塔里木河下游不同植被覆盖度灌木防风固沙功能野外观测研究[J].中国沙漠,2007,27(6),1022-1026.
[12] Living Stone I,Wiggs G F S,Weaver C M. Geomorphology of desert sand dunes,A review of recent progress[J].Earth Science Reviews,2007,80(3-4):239-257.
[13]吴正,凌裕泉.风沙运动的若干规律及风沙危害问题的初步研究[M].北京:科学出版社,1965:7-14.
[14]王训明,陈广庭,韩致文,等.塔里木沙漠公路沿线的起沙风与输沙强度[J].中国沙漠,1997,17(2):168-172.
[15]王训明,董志宝,陈广庭,等.塔克拉玛干沙漠中部部分地区风沙环境特征[J].中国沙漠,2001,21(1):55-61.
[16]赵景峰,李崇舜,何清,等.塔克拉玛干沙漠腹地塔中一井地区起沙风分析和输沙量的估算[J].干旱区地理,1995,18(3):40-47.
[17]何清,魏文寿,李祥余,等.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分析[J].沙漠与绿洲气象,2008(6):6-11.
[18]薛红,胡列群,王旭.塔中地区沙尘暴天气气候学分析[J].新疆气象,1999,22(3):13-15.
[19]杨兴华,何清,丁国峰,等.塔克拉玛干沙漠腹地风蚀观测试验[J].沙漠与绿洲气象,2012,6(5):67-72.
[20]杨兴华,何清,霍文,等.沙漠地区不同下垫面近地表沙尘水平通量研究[J].干旱区研究,2014,31(3):564-569.
[21]钱正安,宋敏红,李万元.近50年来中国北方沙尘暴的分布及变化趋势[J].中国沙漠,2002,22(2):106-111.
[22]李新周,刘晓东.21世纪中蒙干旱-半干旱地区干旱化趋势的模拟研究[J].干旱区研究,2012,29(2):262-272.
[23]金莉莉,塔克拉玛干沙漠腹地紫外辐射特征研究[D].新疆师范大学,2010.
[24]雷加强,王雪芹.塔里木沙漠公路风沙危害形成研究[J].干旱区研究,2003,20(1):1-6.
[25]何清,买买提艾力·买买提依明.一种地表微梯度集沙仪:中国,200923010758.[P].2009-9.
[26]徐宏明,张庆河.粉沙质海岸泥沙特性实验研究[J].泥沙研究,2000.(3):42-49.
[27]何艺峰,刘春雨,王志强,等.跃移层风沙输运数值模拟[J].环境科学与技术,2012(增刊):74-77.
[28]李志勇,李荫堂.近地层输沙率数值模拟研究[J].干旱区研究,2007,24(6):801-804.
[29]马世威.风沙流结构的研究[J].中国沙漠,1988,3(1):822.
[30]李钢铁.乌兰布和沙漠风沙流结构的研究[J].干旱区资源与环境,2004,18(1):276-278.
[31]张克存.戈壁风沙流结构和风速廓线特征的研究[J].水土保持研究,2005(2):55-58.
[32]张华.科尔沁沙地不同下垫面风沙流结构与变异特征[J].水土保持学报,2002,16(2):21-28.
[33] Butterfield G R. Near-bed mass flux profiles in aeolian sand transport:high-resolution measurements in a wind tunnel[J].Earth Surface Processes and Land forms,1999,24(5):393-412.
[34]董玉祥,马骏.风速对海岸沙丘表面风沙流结构影响的实证研究[J].干旱区资源与环境,2009,23(9):179-183.
[35]张伟民,汪万福,张克存,等.不同沙源供给条件下砾石床面的风沙流结构与蚀积量变化风洞实验研究[J].中国沙漠,2009,29(6):1015-1020.
[36] Lancaster N,Baas A.Influence of vegetation cover on sand transport by wind:field studies at Owens Lake,California[J].Earth Surface Processes and Land forms,1998,23(1):69-82.
[37]陈智,麻硕士,赵永来,等.保护性耕作农田地表风沙流特性[J].农业工程学报,2010,26(1):118-122.
[38]邹学勇,董光荣.戈壁风沙流若干特征研究[J].中国沙漠,1995,15(4):369-373.
[39]朱震达.中国沙漠、沙漠化、荒漠化及其治理的对策[C].北京:中国环境科学出版社,1999:108-136.
[40] Williams G. Some aspects of the aerolian load[J].Sedimentology,1964,3:257-287.
[2]张伟民,汪万福,张克存,等.不同沙源供给条件下砾石床面的风沙流结构与蚀积量变化风洞试验研究[J].中国沙漠,2009,29(6):1005-1010.
[3]夏建新,石雪峰,吉祖稳.植被覆盖条件下地表输沙率模型[J].应用基础与工程科学学报,2006,14(2):218-227.
[4]拜格诺,风沙和荒漠沙丘物理学[M].钱宁译.北京:科学出版社,1959:57-65.
[5]拓万全,杨根生.流动沙丘表面输沙率的理论计算方程[J].干旱区资源与环境,1996,10(4):50-54.
[6] Wolfe S A,Nickeling W G. The protective role of spares vegetation in wind erosion[J]. Progress in Physical Geography,1993,17(1):50-68.
[7] Wasson R J,Nanina P M. Estimating wind transport of sand on vegetated surfaces[J]. Earth Surface Process and Landforms,1986,N(11):505-514.
[8] Buckley R. The effect of sparse vegetation on the dune sand by wind[J]. Nature,1987,325:426-428.
[9] Land caster N,Baas A. Influence of vegetation on cover on sand transport by wind:field studies at Owens Lake,California[J]. Earth Surface Processes and Landforms,1982,23:69-82.
[10]黄福祥,牛海山,王明星,等.毛乌素沙地植被覆盖率与风蚀输沙率定量关系[J].地理学报,2001,56(6),700-710.
[11]程皓,李霞,侯平,等.塔里木河下游不同植被覆盖度灌木防风固沙功能野外观测研究[J].中国沙漠,2007,27(6),1022-1026.
[12] Living Stone I,Wiggs G F S,Weaver C M. Geomorphology of desert sand dunes,A review of recent progress[J].Earth Science Reviews,2007,80(3-4):239-257.
[13]吴正,凌裕泉.风沙运动的若干规律及风沙危害问题的初步研究[M].北京:科学出版社,1965:7-14.
[14]王训明,陈广庭,韩致文,等.塔里木沙漠公路沿线的起沙风与输沙强度[J].中国沙漠,1997,17(2):168-172.
[15]王训明,董志宝,陈广庭,等.塔克拉玛干沙漠中部部分地区风沙环境特征[J].中国沙漠,2001,21(1):55-61.
[16]赵景峰,李崇舜,何清,等.塔克拉玛干沙漠腹地塔中一井地区起沙风分析和输沙量的估算[J].干旱区地理,1995,18(3):40-47.
[17]何清,魏文寿,李祥余,等.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分析[J].沙漠与绿洲气象,2008(6):6-11.
[18]薛红,胡列群,王旭.塔中地区沙尘暴天气气候学分析[J].新疆气象,1999,22(3):13-15.
[19]杨兴华,何清,丁国峰,等.塔克拉玛干沙漠腹地风蚀观测试验[J].沙漠与绿洲气象,2012,6(5):67-72.
[20]杨兴华,何清,霍文,等.沙漠地区不同下垫面近地表沙尘水平通量研究[J].干旱区研究,2014,31(3):564-569.
[21]钱正安,宋敏红,李万元.近50年来中国北方沙尘暴的分布及变化趋势[J].中国沙漠,2002,22(2):106-111.
[22]李新周,刘晓东.21世纪中蒙干旱-半干旱地区干旱化趋势的模拟研究[J].干旱区研究,2012,29(2):262-272.
[23]金莉莉,塔克拉玛干沙漠腹地紫外辐射特征研究[D].新疆师范大学,2010.
[24]雷加强,王雪芹.塔里木沙漠公路风沙危害形成研究[J].干旱区研究,2003,20(1):1-6.
[25]何清,买买提艾力·买买提依明.一种地表微梯度集沙仪:中国,200923010758.[P].2009-9.
[26]徐宏明,张庆河.粉沙质海岸泥沙特性实验研究[J].泥沙研究,2000.(3):42-49.
[27]何艺峰,刘春雨,王志强,等.跃移层风沙输运数值模拟[J].环境科学与技术,2012(增刊):74-77.
[28]李志勇,李荫堂.近地层输沙率数值模拟研究[J].干旱区研究,2007,24(6):801-804.
[29]马世威.风沙流结构的研究[J].中国沙漠,1988,3(1):822.
[30]李钢铁.乌兰布和沙漠风沙流结构的研究[J].干旱区资源与环境,2004,18(1):276-278.
[31]张克存.戈壁风沙流结构和风速廓线特征的研究[J].水土保持研究,2005(2):55-58.
[32]张华.科尔沁沙地不同下垫面风沙流结构与变异特征[J].水土保持学报,2002,16(2):21-28.
[33] Butterfield G R. Near-bed mass flux profiles in aeolian sand transport:high-resolution measurements in a wind tunnel[J].Earth Surface Processes and Land forms,1999,24(5):393-412.
[34]董玉祥,马骏.风速对海岸沙丘表面风沙流结构影响的实证研究[J].干旱区资源与环境,2009,23(9):179-183.
[35]张伟民,汪万福,张克存,等.不同沙源供给条件下砾石床面的风沙流结构与蚀积量变化风洞实验研究[J].中国沙漠,2009,29(6):1015-1020.
[36] Lancaster N,Baas A.Influence of vegetation cover on sand transport by wind:field studies at Owens Lake,California[J].Earth Surface Processes and Land forms,1998,23(1):69-82.
[37]陈智,麻硕士,赵永来,等.保护性耕作农田地表风沙流特性[J].农业工程学报,2010,26(1):118-122.
[38]邹学勇,董光荣.戈壁风沙流若干特征研究[J].中国沙漠,1995,15(4):369-373.
[39]朱震达.中国沙漠、沙漠化、荒漠化及其治理的对策[C].北京:中国环境科学出版社,1999:108-136.
[40] Williams G. Some aspects of the aerolian load[J].Sedimentology,1964,3:257-287.