Influence of the floods from different sediment source areas on the relationship between discharge and sediment concentration of the lower Yellow River
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摘要: 根据1950-1960年及1974-1985年实测洪峰水沙资料,分析了不同来源区洪水对黄河下游花园口、高村、艾山、利津水文站流量 含沙量关系的影响,以河口镇至龙门区间、马莲河和北洛河总来水量占三门峡、黑石关、小董总水量的20%或25%以上作为中游粗沙来源区洪水,以河口镇至龙门区间、马莲河和北洛河总来水量占三门峡、黑石关、小董总水量的20%或25%以下作为细沙来源区或少沙区洪水。这样,黄河下游花园口、高村、艾山、利津水文站平均流量 平均含沙量关系可分为以增加平均含沙量为主和以增加平均流量为主的两个区。同时,河口镇至龙门区间、马莲河和北洛河的洪水,大大增加了黄河下游平均来沙系数和平均含沙量,并导致全下游河段的必然淤积。Abstract: Based on the measurements during 1950-1960 and 1974-1985,the analysis are made on the influence of the floods from different sediment source areas on the relationship between the discharge and the sediment concentration at stations of Huayuankou,Caocun,Aishan and Lijin on the lower Yellow River. When the runoff between Hekou and Longmen,Malian River and Beiluo River accounts for rmre than 20% or 25% of the total water wlumes at stations of Sanmenxia,Heishiguan and Xiaodng,the flood is referred to as from the coarse sediment source area of the Yellow River. When the runoff between Hekou and Longmen,Malian River and Beiluo River covers less 20% or 25% of the total runoff at stations of Sanmenxia, Heishiguan and Xiaodong,the flood is referred to as from the fine-sediment source area or from the area with small sediment concentrations. As a result,the relationship between the mean discharge and the mean sediment concentration at stations of Huayuankou,Caocun,Aishan and Lijin on the lower Yellow River is divided into two classes:(1) the mean sediment concen-tration increases greatly for small variation in the mean discharge,and (2) the concentration does not increase much even when the mean discharge increases by several times. Meanwhile,the flood between Hekou and Longmen,Malian River and Beiluo River causes great increase in the mean inflow sediment coefficient and the mean sediment concentration of the lower Yellow River and consequently leads to a large amount of the deposition.
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[1] Picouet C, Hingray B, Olivry J C. Empirical and conceptual modeling of the suspended sediment dynamics in a large tropical African river:the Upper Niger river basin[J]. Journal of Hydrology, 2001, 250 (1-4): 19-39. [2] Lenzi M A, Marchi L. Suspended sediment load during floods in a small stream of the dolomites (northeastern Italy)[J]. CATENA, 2000, 39(4):267-282. [3] Syvitski J P, Morehead M D, Bahr D B, et al. Estimating fluvial sediment transport:the rating parameters[J]. Water Resources Research,2000, 36(9):2747-2760. [4] Hicks D M, Gomez B, Trustrum N A. Erosion thresholds and suspended sediment yields, Waipaoa River Basin, New Zealand[J]. Water Re-sources Research, 2000, 36(4): 1 129-1 142. [5] 钱宁.关于"床沙质"和"冲泻质"的概念的说明[J].水利学报,1957,(1):29-45. [6] 麦乔威,赵业安,潘贤娣,等.黄河下游来水来沙特性及河道冲淤规律的研究[A].麦乔威论文集编辑委员会主编.麦乔威论文集[C].郑州:黄河水利出版社,1995.165-204. [7] 赵文林.黄河泥沙[M].郑州:黄河水利出版社,1996.99-103. [8] 钱宁,等.黄河下游挟沙能力自动调整机理的初步探讨[J].地理学报,1981,36(2):143-156. [9] 赵业安.二十一世纪黄河泥沙处理的基本思路和对策[A].黄河研究会,台湾交通大学.第四届海峡两岸多沙河川整治与管理学术研讨会论文集[C].郑州:黄河研究会,2001.1-12. [10] 张红武,赵业安,温善章.论大柳树水利枢纽工程的战略地位与作用[A].全国政协人口资源环境委员会.西部大开发与水资源文集[C].北京:中国水利水电出版社,2000.59-67. [11] 齐璞.对黄河下游河道认识的突破[J].科技导报,2000,(11):22-25. [12] 蔡为武.黄河水资源矛盾及其出路探讨[J].人民黄河,1996,18(6):54-57. [13] 温善章,赵业安.充分开发利用黄河水资源的战略措施[J].山西水利科技,1994,24(1):9-11,41. [14] 钱宁.高含沙水流运动[M].北京:清华大学出版社,1989. [15] 苏人琼,杨勤业,关志华,等.黄河流域灾害环境综合治理对策[M].郑州:黄河水利出版社,1997.68-69. [16] 景可,李钜章,李凤新.黄河多沙粗沙区产水产沙对中游来水来沙的贡献率[J].土壤侵蚀与水土保持学报,1999,5(1):13-18,26. [17] 钱宁,王可钦,阎林德,等.黄河中游粗泥沙来源区对黄河下游冲淤的影响[A].第一次河流泥沙国际学术讨论会论文集[C].北京:光华出版社,1980.53-62. [18] 姚文艺,王卫东.黄河泥沙来源研究评述[J].人民黄河,1997,19(6):14-17. [19] 徐建华,吕光圻.黄河粗泥沙定界论证[J].人民黄河,1999,21(12):6-8. [20] 钱宁,张仁,周志德.河床演变学[M].北京:科学出版社,1987.205. -
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