无定河流域不同地貌区水沙过程对比

doi:10.11821/yj2007030011

地理研究 ›› 2007, Vol. 26 ›› Issue (3): 508-517.doi: 10.11821/yj2007030011

无定河流域不同地貌区水沙过程对比

王随继

中国科学院地理科学与资源研究所中国科学院陆地水循环及地表过程重点实验室,北京 100101

收稿日期:2006-08-06 修回日期:2006-11-23 出版日期:2007-05-25 发布日期:2007-05-25
作者简介:王随继 (1966-),男,甘肃静宁人,副研究员。从事沉积学、地貌学、水土保持等方面的研究工作。E-mail :wangsj@igsnrr.ac.cn。
基金资助:
国家自然科学基金项目 (40271019、50239080)和中国科学院地理科学与资源所知识创新项目资助。

Comparison of sediment and runoff yield processes between different geomorphic regions in the Wudinghe River Basin

WANG Sui-ji

Key Laboratory of Water Cycle and Related Land Surface Processes, Institute of Geographic Sciences and Natural Resources Research, CAS, Beijing 100101, China

Received:2006-08-06 Revised:2006-11-23 Online:2007-05-25 Published:2007-05-25
Supported by:
国家自然科学基金项目 (40271019、50239080)和中国科学院地理科学与资源所知识创新项目资助。

摘要/Abstract

摘要： 为了查明人为影响程度较低时期无定河流域内不同地貌区的水沙过程及其变化规律,选取1970年以前一段时期该流域内风沙区和黄土丘陵沟壑区河流的有关水文站的水文泥沙实测数据进行对比分析。结果表明,风沙区河流的流量变率较黄土丘陵沟壑区的小;风沙区河流的含沙量远小于黄土丘陵沟壑区河流的含沙量。黄土丘陵沟壑区河流具有极高的输沙率,而风沙区河流的输沙率微不足道。风沙区和黄土丘陵沟壑区河流的产流模数基本相近,但产沙模数非常悬殊,前者的产沙模数很小,为118.58~725.38t /km² · a,而后者的达到1879.36~25112.15t /km² · a。显然,无定河流域黄土丘陵沟壑区的河流是侵蚀产沙的主要来源区,因而是水土保持工作的重点区域。

关键词: 流量, 含沙量, 输沙率, 产流模数, 风沙区, 黄土丘陵沟壑区, 无定河

Abstract: The Wudinghe River Basin is a representative basin in the eolian-loess transitional zone of the Loess Plateau. Some projects actualized during the last three decades for soil and water loss has led the sediment and runoff processes of the river basin no longer being in a pure natural state but also affected by anthropogenic activities.In order to put forward effective measures to prevent soil and water loss, it is necessary to find the natural processes of sediment and runoff yield of the Wudinghe River Basin. In this work the varying processes and rules of sediment and runoff yield in the eolian and loess hilly-gully regions of the river basin were analyzed systematically according to the data measured in a certain period of time before 1970 because limited human activities had been thrown to the river system during this period. The results are as below. In the near natural state the varying ratio of discharge of the river in the eolian region is smaller than that in the loess hilly-gully region.The river sediment concentration in the eolian region is far smaller than that in the loess hilly-gully region, accordingly, sediment delivery ratio is very high in the rivers of the loess hill gully region but inappreciable in the rivers of the eolian region. The specific runoff yield of the rivers in both eolian and loess hilly-gully regions is very close, but great disparities of the specific sediment yield occur in different regional rivers: it is 118.58~725.38 t/km² · a for the eolian region and 1879.36~25112.15 t/km² · a for the loess hilly-gully region. Obviously, the tributaries located in the loess hilly-gully region are the main source of the sediment yield in the Wudinghe River Basin. So, these tributary basins are the main regions needed to prevent soil and water loss and the control of sediment yield in gullies of these tributaries is the key task.

Key words: discharge, sediment concentration, sediment delivery ratio, specific sediment yield, eolian region, loess hilly-gully region, Wudinghe River

王随继. 无定河流域不同地貌区水沙过程对比[J]. 地理研究, 2007, 26(3): 508-517.

WANG Sui-ji. Comparison of sediment and runoff yield processes between different geomorphic regions in the Wudinghe River Basin[J]. GEOGRAPHICAL RESEARCH, 2007, 26(3): 508-517.

参考文献

[1] Xu J, Yang J, Yan Y.Erosion and sediment yields as influenced by coupled eolian and fluvial processes: The Yellow River, China. Geomorphology,2006,73: 1~15.

[2] 唐克丽.黄河流域的侵蚀与径流变化.北京:中国科学技术出版社,1993.

[3] 赵文林主编.黄河泥沙.郑州:黄河水利出版社,1996.1~807.

[4] 张胜利,陈发中.黄河中游多沙粗沙区风蚀产沙对黄河粗泥沙影响分析.中国水土保持,1999,13~18.

[5] 董治宝,李振山.风成沙粒度特征对其风蚀可蚀性的影响.土壤侵蚀与水土保持学报,1998,4(4): 1~5.

[6] 许炯心.黄河中游多沙粗沙区的风水两相侵蚀产沙过程.中国科学(D辑),2000,30(5): 540~548.

[7] Shi H, Shao M. Soil and water loss from the Loess Plateau in China. Journal of Arid Environments,2000, 45: 9~20.

[8] 张平仓.水蚀风蚀交错带水风两相侵蚀时空特征研究——以神木六道沟小流域为例.土壤侵蚀与水土保持学报,1999,5(3): 93~94.

[9] Zhu Z, Zhou H, An Z, Liu T.A river erosion estimate on the Loess Plateau: A case study from Luohe River, a second-order tributary of the Yellow River. Global and Planetary Change, 2004, 41: 215~220.

[10] 李景宗,张玫.浅谈加快红柳河坝库群综合治理的必要性.中国水土保持,2002,(6): 6~7.

[11] 钱云平,董雪娜,林银平,陈端良.无定河水沙特性变化分析.人民黄河,1999,21(8): 25~27.

[12] 许炯心.无定河流域侵蚀产沙过程对水土保持措施的响应.地理学报,2004,59(6): 972~981.

[13] 杨新,延军平,刘宝元.无定河年径流量变化特征及人为驱动力分析.地球科学进展,2005,20(6):637~642.

[14] 师长兴.风力侵蚀对无定河流域产沙作用定量分析.地理研究,2006, 25(2): 285~293.

[15] 王随继.黄河中游冻融侵蚀的表现方式及其产沙能力评估.水土保持通报,2004,(6): 1~5.

[16] 许炯心.黄河中游支流悬移质粒度与含沙量、流量间的复杂关系.地理研究,2003,22(1): 39~48.

无定河流域不同地貌区水沙过程对比

Comparison of sediment and runoff yield processes between different geomorphic regions in the Wudinghe River Basin

PDF (PC)

赞

可视化

被引次数

摘要/Abstract

引用本文

使用本文

参考文献

相关文章 15

Metrics

本文评价

推荐阅读 0

[1]	初楠臣, 张平宇, 吴相利, 李鹤. 基于日流量视角的俄罗斯首府城市铁路客运网络空间特征[J]. 地理研究, 2021, 40(1): 247-262.
[2]	李涛, 张维阳, 曹小曙, 汪丽, 张隆. 珠江三角洲城际轨道网络结构：基于连接、容量和流量的对比[J]. 地理研究, 2019, 38(11): 2730-2744.
[3]	初楠臣, 张平宇, 姜博. 基于日高铁流量视角的中国高速铁路网络空间特征[J]. 地理研究, 2018, 37(11): 2193-2205.
[4]	吴江, 张秀香, 叶玲翠, 黄震方, 曹芳东. 不同时间尺度周期的旅游客流量波动特征研究——以西藏林芝市为例[J]. 地理研究, 2016, 35(12): 2347-2362.
[5]	葛淼, 薛然尹, 何进伟, 胡燕宇. 中国男性儿童呼气高峰流量参考值地理分布[J]. 地理研究, 2014, 33(3): 451-466.
[6]	王随继, 李玲, 颜明. 气候和人类活动对黄河中游区间产流量变化的贡献率[J]. 地理研究, 2013, 32(3): 395-402.
[7]	姚允龙, 王蕾, 吕宪国, 于洪贤. 挠力河流域河流径流量对气候变化的敏感性分析[J]. 地理研究, 2012, 31(3): 409-416.
[8]	孔岩, 王红, 任立良. 黄河入海径流变化及影响因素[J]. 地理研究, 2012, 31(11): 1981-1990.
[9]	孙鹏, 张强, 陈晓宏. 鄱阳湖流域枯水径流演变特征、成因与影响[J]. 地理研究, 2011, 30(9): 1702-1712.
[10]	邵爱军, 左丽琼, 王丽君. 气候变化对河北省海河流域径流量的影响[J]. 地理研究, 2010, 29(8): 1502-1509.
[11]	许炯心. 无定河流域的人工沉积汇及其对泥沙输移比的影响[J]. 地理研究, 2010, 29(3): 397-407.
[12]	吴普, 葛全胜. 海南旅游客流量年内变化与气候的相关性分析[J]. 地理研究, 2009, 28(4): 1078-1084.
[13]	方海燕, 蔡强国, 李秋艳. 黄土丘陵沟壑区坡面产流能力及影响因素研究[J]. 地理研究, 2009, 28(3): 583-591.
[14]	马元旭, 许炯心. 无定河及其各支流的断面水力几何形态[J]. 地理研究, 2009, 28(2): 345-353.
[15]	王随继, 冉立山. 无定河流域产沙量变化的淤地坝效应分析[J]. 地理研究, 2008, 27(4): 811-818.