岷江上游和中游几个河段的下蚀率对比研究
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摘要
岷江中、上游从我国地势的第一阶梯穿入第二阶梯,是中国西部地质、地貌、气候的陡变带,因而研究其下蚀率具有重要的理论和实际意义。利用河流阶地与阶地形成年龄间的线性关系分别研究了岷江上游和中游几个河段的河流下蚀率,通过计算分别得出岷江上游和中游几个河段的河流下蚀率,在此基础上对岷江上游和中游的几个河段的下蚀率作了对比,得出岷江上游几个河段的年平均下蚀率(1.40 mm/a)大于岷江中游几个河段的年平均下蚀率(1.08 mm/a)的结论,并分析了产生这种现象的原因。
Minjiang River is a very important tributary of Changjiang River and is located in eastern margin of Tibetan Plateau which is an important constitute of geotectonic units of China.It is also a changed area of geology,geomorphology and climate.The authors according the linear relation between river terrace and river incision studied the incision rate of Minjiang River's upper and middle reaches,and reached a conclusion that the average incision rate of Minjiang River's upper reaches is 29.62% larger than the average incision rate of Minjiang River's middle reach.The reasons are the difference in the channel gradients of Minjiang River's upper reaches and middle reaches,and the elevation movement of earth crust which is different under the river channel.
Minjiang River is a very important tributary of Changjiang River and is located in eastern margin of Tibetan Plateau which is an important constitute of geotectonic units of China.It is also a changed area of geology,geomorphology and climate.The authors according the linear relation between river terrace and river incision studied the incision rate of Minjiang River's upper and middle reaches,and reached a conclusion that the average incision rate of Minjiang River's upper reaches is 29.62% larger than the average incision rate of Minjiang River's middle reach.The reasons are the difference in the channel gradients of Minjiang River's upper reaches and middle reaches,and the elevation movement of earth crust which is different under the river channel.
引文
[1]长江水利委员会.长江年鉴[M].武汉:长江年鉴社,2000~2004.
[2]唐荣昌,韩渭宾.四川活动断裂与地震[M].北京:地震出版社,1993.1~1192.
[3]赵小麟,邓起东,陈社发,等.岷山隆起的构造地貌学研究[J].地震地质,1994,16(4):429~439.
[4]Kirby E,Whipple K X,Burchfiel B C,et al.Neotectoniics ofthe Min Shan,China:implications driving Quaternary deform-ation along the eastern margin of the Tibetan Plateau[J].GSABulletin,2000,112(3):375~393.
[5]Maddy D.Uplift-driven valley incision and ricer terrace forma-tion in southern England[J].JWS,1997,12(6):539~545.
[6]叶延琼,陈国阶,樊宏.岷江上游脆弱生态环境刍论[J].长江流域资源与环境,2002,11(4):384~387.
[7]蔡述明.研究长江中游地区水资源开发利用的新成果[J].长江流域资源与环境,2004,13(1):356~360.
[8]郭晓东,牛叔文.长江流域资源环境与区域发展研究的回顾及展望[J].长江流域资源与环境,2005,14(3):393~396.
[9]励强.自然侵蚀和加速侵蚀的理论与方法[J].水土保持学报,1989,3(3):1~8.
[10]张玉芬,李长安.长江中游现代河流沉积物磁组构参数值特征研究[J].长江流域资源与环境,2003,12(4):370~376.
[11]程江,何青,王元叶.长江河口细颗粒泥沙絮凝体粒径的谱分析[J].长江流域资源与环境.2005,14(4):460~464.
[12]Ewen J,Parkin G.Validation of catchments models for pre-dicting land-use and climate change impacts[J].Hydrology,1996,175:583~504.
[13]Beven K J.Future of distributed modeling[J].HydrologicalProcess,1992,6:253~268.
[2]唐荣昌,韩渭宾.四川活动断裂与地震[M].北京:地震出版社,1993.1~1192.
[3]赵小麟,邓起东,陈社发,等.岷山隆起的构造地貌学研究[J].地震地质,1994,16(4):429~439.
[4]Kirby E,Whipple K X,Burchfiel B C,et al.Neotectoniics ofthe Min Shan,China:implications driving Quaternary deform-ation along the eastern margin of the Tibetan Plateau[J].GSABulletin,2000,112(3):375~393.
[5]Maddy D.Uplift-driven valley incision and ricer terrace forma-tion in southern England[J].JWS,1997,12(6):539~545.
[6]叶延琼,陈国阶,樊宏.岷江上游脆弱生态环境刍论[J].长江流域资源与环境,2002,11(4):384~387.
[7]蔡述明.研究长江中游地区水资源开发利用的新成果[J].长江流域资源与环境,2004,13(1):356~360.
[8]郭晓东,牛叔文.长江流域资源环境与区域发展研究的回顾及展望[J].长江流域资源与环境,2005,14(3):393~396.
[9]励强.自然侵蚀和加速侵蚀的理论与方法[J].水土保持学报,1989,3(3):1~8.
[10]张玉芬,李长安.长江中游现代河流沉积物磁组构参数值特征研究[J].长江流域资源与环境,2003,12(4):370~376.
[11]程江,何青,王元叶.长江河口细颗粒泥沙絮凝体粒径的谱分析[J].长江流域资源与环境.2005,14(4):460~464.
[12]Ewen J,Parkin G.Validation of catchments models for pre-dicting land-use and climate change impacts[J].Hydrology,1996,175:583~504.
[13]Beven K J.Future of distributed modeling[J].HydrologicalProcess,1992,6:253~268.
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