汶川地震灾区坡面和沟谷泥石流冲出距离计算方法
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摘要
坡面型和沟谷型泥石流是2种不同的泥石流,不能用单一模型来计算它们的冲出距离。经分类研究,发现它们冲出距离的主影响因子有很大不同:对于沟谷型泥石流,主要是沟道内的松散物质储量;而对于坡面型泥石流,主要是坡面松散体的高度以及体积。2种泥石流的冲出角分布也存在很大差别:研究区沟谷型泥石流的冲出角在29.6°～82.9°之间,表现出"高量级、高冲出角"的特征;坡面型泥石流的冲出角在25°～47°之间,且大部分的冲出角在30°左右,表现出"低量级、低冲出角"的特征。在此分析的基础上,用回归分析方法建立了汶川地震灾区2种不同类型泥石流冲出距离的计算方法。最后,将经验计算方法用陈家坝文家坪坡面泥石流和红椿沟泥石流进行验证,与实际值较为吻合。
Hillslope debris flow and channelized debris flow are very different in formation and movement.This indicates their runout distances cannot be described by a single model.Investigation of the two kinds of debris flow in the Wenchuan earthquake zone shows that the principal factors influencing the runout distances are different.For channelized debris flow,the principal factor is volume of sediment supply,while for hillslope debris flow the factors are relative height and volume of debris.Comparing with debris flow in Alps area,the run-out angle of the two kinds of debris flow in the earthquake area also exhibits different characteristics.The run-out angle of channelized debris flow ranges from 29.6° to 82.9°,which is characterized by "great magnitude and large runout angle",whereas the angle of slope debris flow from 25° to 47°,which is characterized by "small magnitude and small runout angle".The data of debris-flow events in Beichuan and Qingping of the earthquake zone were used to respectively derive the empirical formulas for calculating the runout distance of hillslope debris flow and channelized debris flow by statistical regressive method.The resulted formulas were verified by two cases,and can be applied to post-quake debris flow.
Hillslope debris flow and channelized debris flow are very different in formation and movement.This indicates their runout distances cannot be described by a single model.Investigation of the two kinds of debris flow in the Wenchuan earthquake zone shows that the principal factors influencing the runout distances are different.For channelized debris flow,the principal factor is volume of sediment supply,while for hillslope debris flow the factors are relative height and volume of debris.Comparing with debris flow in Alps area,the run-out angle of the two kinds of debris flow in the earthquake area also exhibits different characteristics.The run-out angle of channelized debris flow ranges from 29.6° to 82.9°,which is characterized by "great magnitude and large runout angle",whereas the angle of slope debris flow from 25° to 47°,which is characterized by "small magnitude and small runout angle".The data of debris-flow events in Beichuan and Qingping of the earthquake zone were used to respectively derive the empirical formulas for calculating the runout distance of hillslope debris flow and channelized debris flow by statistical regressive method.The resulted formulas were verified by two cases,and can be applied to post-quake debris flow.
引文
[1]Fannin R J,Wise M P.An empirical statistical modelfor debris flow travel distance[J].CanadianGeotechnical Journal,2001,(38):982-994.
[2]Matteo B,Alessandro S.Prediction of debris flowinundation areas using empirical mobility relationships[J].Geomorphology,2007,(90):144-161.
[3]Adam B P,Paul M S,Jerry D H,et al.Debris-flowrunout predictions based on the average channel slope(ACS)[J].Engineering Geology,2008,(98):29-40.
[4]Rickenmann D.Empirical relationships for debrisflows[J].Natural Hazards,1999,(19):47-77.
[5]Hungr O.A model for the runout analysis of rapidflow slides,debris flows,and avalanches[J].Canadian Geotechnical Journal,1995,(32):610-623.
[6]Rickenmann D.Runout Prediction Methods[M]∥Debris-flow Hazards and Related Phenomena.Springer:Praxis Publishing Ltd,Chichester,UK,2005.305-324.
[7]Cannon S H,Savage W Z.A mass-change model forthe estimation of debris-flow runout[J].Journal ofGeology,1988,(96):221-227.
[8]Hungr O,Morgan G C,Kellerhals R.Quantitativeanalysis of debris torrent hazards for design of reme-dial measures[J].Canadian Geotechnical Journal,1984,(21):663-677.
[9]Okura Y,Kitahara H,Sammori T,et al.The effectsof rockfall volume on runout distance[J].EngineeringGeology,2000,(8):109-124.
[10]刘希林,莫多闻.泥石流风险评价[M].成都:四川科学技术出版社,2002.Liu X L,Mo D W.The Risk Evaluation of DebrisFlow[M].Chengdu:Sichuan Publishing House ofScience&Technology,2002.
[11]陈晓清,崔鹏,赵万玉.汶川地震区泥石流灾害工程防治时机的研究[J].四川大学学报(工程科学版),2009,41(3):125-130.Chen X Q,Cui P,Zhao W Y.Optimal timing for thecontrol of debris flow in Wenchuan earthquake area[J].Journal of Sichuan University(EngineeringScience Edition),2009,41(3):125-130.
[12]唐川,铁永波.汶川震区北川县城魏家沟暴雨泥石流灾害调查分析[J].山地学报,2009,27(5):625-630.Tang Ch,Tie Y B.Reconnaissance and analysis onthe rainstorm induced debris flow in Weijiagou valleyof Beichuan city after the Wenchuan earthquake[J].Journal of Mountain Science,2009,27(5):625-630.
[13]许强.四川省8.13特大泥石流灾害特点、成因与启示[J].工程地质学报,2010,18(5):596-609.Xu Q.The 13 August 2010 catastrophic debris flow inSichuan province:characteristics,genetic mechanismand suggestions[J].Journal of Engineering Geology,2010,18(5):596-609.
[14]游勇,柳金峰,陈兴长.“5.12”汶川地震后北川苏保河流域泥石流危害及特征[J].山地学报,2010,28(3):358-366.You Y,Liu J F,Chen X Ch.Debris flow and itscharacteristics of Subao river in Beichuan County after“5.12”Wenchuan earthquake[J].Journal ofMountain Science,2010,28(3):358-366.
[15]张健楠,马煜,张惠惠,等.四川省都江堰市大干沟地震泥石流[J].山地学报,2010,28(5):623-627.Zhang J N,Ma Y,Zhang H H,et al.Study onearthquake in Dagan gully,Dujiangyan,Sichuan[J].Journal of Mountain Science,2010,28(5):623-627.
[16]Shreve R L.Sherman landslide,Alaska[J].Science,1966,(154):1639-1643.
[17]Scheidegger A E.On the prediction of the reach andvelocity of catastrophic landslides[J].RockMechanics,1973,(5):231-236.
[18]Li Y F,Wang Z Y,Shi W J,et al.Slope debrisflows in the Wenchuan earthquake area[J].Journal ofMountain Science,2010,(7):226-233.
[19]Corominas J.The angle of reach as a mobility indexfor small and large landslides[J].CanadianGeotechnical Journal,1996,(33):260-271.
[20]Tang C,Zhu J,Chang M,et al.An empirical-statistical model for predicting debris-flow runoutzones in The Wenchuan earthquake area[J].Quaternary International,2012,(250):63-73.
[2]Matteo B,Alessandro S.Prediction of debris flowinundation areas using empirical mobility relationships[J].Geomorphology,2007,(90):144-161.
[3]Adam B P,Paul M S,Jerry D H,et al.Debris-flowrunout predictions based on the average channel slope(ACS)[J].Engineering Geology,2008,(98):29-40.
[4]Rickenmann D.Empirical relationships for debrisflows[J].Natural Hazards,1999,(19):47-77.
[5]Hungr O.A model for the runout analysis of rapidflow slides,debris flows,and avalanches[J].Canadian Geotechnical Journal,1995,(32):610-623.
[6]Rickenmann D.Runout Prediction Methods[M]∥Debris-flow Hazards and Related Phenomena.Springer:Praxis Publishing Ltd,Chichester,UK,2005.305-324.
[7]Cannon S H,Savage W Z.A mass-change model forthe estimation of debris-flow runout[J].Journal ofGeology,1988,(96):221-227.
[8]Hungr O,Morgan G C,Kellerhals R.Quantitativeanalysis of debris torrent hazards for design of reme-dial measures[J].Canadian Geotechnical Journal,1984,(21):663-677.
[9]Okura Y,Kitahara H,Sammori T,et al.The effectsof rockfall volume on runout distance[J].EngineeringGeology,2000,(8):109-124.
[10]刘希林,莫多闻.泥石流风险评价[M].成都:四川科学技术出版社,2002.Liu X L,Mo D W.The Risk Evaluation of DebrisFlow[M].Chengdu:Sichuan Publishing House ofScience&Technology,2002.
[11]陈晓清,崔鹏,赵万玉.汶川地震区泥石流灾害工程防治时机的研究[J].四川大学学报(工程科学版),2009,41(3):125-130.Chen X Q,Cui P,Zhao W Y.Optimal timing for thecontrol of debris flow in Wenchuan earthquake area[J].Journal of Sichuan University(EngineeringScience Edition),2009,41(3):125-130.
[12]唐川,铁永波.汶川震区北川县城魏家沟暴雨泥石流灾害调查分析[J].山地学报,2009,27(5):625-630.Tang Ch,Tie Y B.Reconnaissance and analysis onthe rainstorm induced debris flow in Weijiagou valleyof Beichuan city after the Wenchuan earthquake[J].Journal of Mountain Science,2009,27(5):625-630.
[13]许强.四川省8.13特大泥石流灾害特点、成因与启示[J].工程地质学报,2010,18(5):596-609.Xu Q.The 13 August 2010 catastrophic debris flow inSichuan province:characteristics,genetic mechanismand suggestions[J].Journal of Engineering Geology,2010,18(5):596-609.
[14]游勇,柳金峰,陈兴长.“5.12”汶川地震后北川苏保河流域泥石流危害及特征[J].山地学报,2010,28(3):358-366.You Y,Liu J F,Chen X Ch.Debris flow and itscharacteristics of Subao river in Beichuan County after“5.12”Wenchuan earthquake[J].Journal ofMountain Science,2010,28(3):358-366.
[15]张健楠,马煜,张惠惠,等.四川省都江堰市大干沟地震泥石流[J].山地学报,2010,28(5):623-627.Zhang J N,Ma Y,Zhang H H,et al.Study onearthquake in Dagan gully,Dujiangyan,Sichuan[J].Journal of Mountain Science,2010,28(5):623-627.
[16]Shreve R L.Sherman landslide,Alaska[J].Science,1966,(154):1639-1643.
[17]Scheidegger A E.On the prediction of the reach andvelocity of catastrophic landslides[J].RockMechanics,1973,(5):231-236.
[18]Li Y F,Wang Z Y,Shi W J,et al.Slope debrisflows in the Wenchuan earthquake area[J].Journal ofMountain Science,2010,(7):226-233.
[19]Corominas J.The angle of reach as a mobility indexfor small and large landslides[J].CanadianGeotechnical Journal,1996,(33):260-271.
[20]Tang C,Zhu J,Chang M,et al.An empirical-statistical model for predicting debris-flow runoutzones in The Wenchuan earthquake area[J].Quaternary International,2012,(250):63-73.
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