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中国河流地貌研究进展——纪念沈玉昌先生100年诞辰

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许炯心, 蔡强国, 李炳元, 吴积善, 金德生, 尤联元, 师长兴, 张青松
中国科学院地理科学与资源研究所,北京 100101

Research progress in river geomorphology in China: In memory of 100-year anniversary of Shen Yuchang's birth

XUJiongxin, CAIQiangguo, LIBingyuan, WUJishan, JINDesheng, YOULianyuan, SHIChangxing, ZHANGQingsong
Institute of Geographic Sciences and Natural Resources Research, CAS, Beijing 100101, China
通讯作者:通讯作者:许炯心(1948-), 男, 四川绵阳人, 研究员, 中国地理学会会员(S110000878H), 主要从事河流地貌研究。E-mail: xujx@igsnrr.ac.cn
收稿日期:2016-08-6
修回日期:2016-10-16
网络出版日期:2016-11-25
版权声明:2016《地理学报》编辑部本文是开放获取期刊文献,在以下情况下可以自由使用:学术研究、学术交流、科研教学等,但不允许用于商业目的.
基金资助:国家自然科学基金项目(41371037)

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摘要
2016年是中国现代河流地貌研究的开拓者和奠基人沈玉昌先生100年诞辰,本文对中国河流地貌研究进展进行综述,以资纪念。研究涉及4个方面:① 水系发育与河谷地貌演变,包括大江大河水系历史发育和山区河流地貌;② 侵蚀与产沙过程,包括有物理成因基础的侵蚀产沙模型、侵蚀产沙过程的尺度效应、植被对侵蚀的影响及临界现象、坡面细沟发育过程模拟等;③ 河床过程与河型,包括河道冲淤过程、河床演变、河型成因与演变等;④ 河流地貌系统研究,包括流域系统不同子系统的耦合关系、河流地貌系统中的高含沙水流和多营力地貌过程、河流地貌系统对于自然因素变化和人类活动的响应、河流地貌系统中的泥沙灾害和河流地貌系统的实验研究等。50年前沈玉昌先生与钱宁先生提出在地貌学与河流动力学相结合的基础上发展中国河流学科。文中对此方面的进展进行了综述,并提出了需要深化和解决的问题。

关键词:河流地貌学;研究进展;中国河流
Abstract
2016 is the 100th anniversary of Professor Shen Yuchang, the founder of river geomorphology in China. To commemorate this event, we reviewed the advances in river geomorphology in China in the past 20 years, which cover the following four topics: (1) river system development and river valley evolution, including the historical development of the Yellow and Yangtze rivers and mountain region river geomorphology; (2) erosion and sediment production processes, including the physically based erosion and sediment yield modeling, scale effect of sediment yield, influence of vegetation on erosion and thresholds, and simulation of hillslope rill development; (3) river channel processes and river patterns, including channel fill and scour behaviors, channel changes and the formative cause of river channel patterns; and (4) study of river geomorphology in the framework of fluvial system, including the couplings between sub-systems, hyperconcentated flows and multiple-agent geomorphologic processes, response of fluvial system to climate change and human activity, sediment-related disasters and the laboratory experiments on fluvial systems. Around 50 years ago, Professors Shen Yuchang and Qian Ning together put forward a strategy for Chinese river researches on the basis of combination of geomorphology with hydrodynamics. In this right direction the river geomorphology in China has achieved an initial breakthrough. In addition, some issues that need to be deepened or solved in the future are addressed.

Keywords:river geomorphology;research progress;Chinese rivers

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许炯心, 蔡强国, 李炳元, 吴积善, 金德生, 尤联元, 师长兴, 张青松. 中国河流地貌研究进展——纪念沈玉昌先生100年诞辰[J]. , 2016, 71(11): 2020-2036 https://doi.org/10.11821/dlxb201611012
XU Jiongxin, CAI Qiangguo, LI Bingyuan, WU Jishan, JIN Desheng, YOU Lianyuan, SHI Changxing, ZHANG Qingsong. Research progress in river geomorphology in China: In memory of 100-year anniversary of Shen Yuchang's birth[J]. 地理学报, 2016, 71(11): 2020-2036 https://doi.org/10.11821/dlxb201611012

1 引言

沈玉昌先生1916年12月26日生于浙江湖州市,1936-1940年成为浙江大学史地系首届本科生,1940-1942年为中国近代地貌学一代宗师叶良辅先生的首批研究生。1947年到中国地理研究所工作,从1958年中国科学院地理研究所成立地貌研究室起到1987年退休,任地貌研究室主任,退休后仍关心地貌学发展,直至1996年病故。他精于河流地貌、地貌区划与地貌制图研究,十分重视地貌学的理论与应用实践以及地貌人才的培养,并为此作出重要贡献[1]
河流地貌学是地貌学的重要分支学科,与经济建设和人类活动有密切关系,一直受人们的重视。沈玉昌先生是中国现代河流地貌研究的开拓者和奠基人,致力于河流地貌研究40余年,逐步形成了具有中国特色的河流地貌研究体系。早在1942年做研究生时就开始接触河流的地貌研究,主要是引进西方习用的方法,研究水系发育的历史,完成了《湘江附近地形初步研究》等论文。新中国成立以后,沈玉昌先生为了配合国家大规模水利工程建设的需要,展开了河谷地貌研究。20世纪50年代早期,在汉江流域地理调查中系统地展开汉江流域河谷地貌研究[2]。20世纪50年代末至60年代初,沈玉昌先生带领中国科学院地理研究所地貌研究室的同志们,系统地开展了长江及其重要支流的河谷地貌研究,他发现了长江三峡河床上一系列低于海平面的深槽洼地,并阐明其成因与分布规律,其代表性成果集中体现在专著《长江上游河谷地貌》(1965)中[3]。他的研究成果为丹江口水库选址、三峡大坝选址、南水北调中线方案选择等国家重大建设项目决策做出了重要贡献。
20世纪60年代中期以后,沈玉昌先生根据国际河流地貌研究的新趋势和国家对治理大江大河的需要,将河流地貌研究重点由以河谷地貌为主转移到以河床地貌为主,研究对象也由山区河流转向平原河流。研究内容主要是河型与河床现代过程,研究方法由单纯的地貌学方法,转变为地理学与水力学、数学、物理学以及系统论等多学科相结合,研究手段也由单一的野外考察转变为野外考察、定位观测、物理模型实验与数学模拟相结合。1960年以来,沈玉昌和钱宁共同倡导并力行河流地貌学与河流动力学相结合的河流研究新方向[4]。积20余年努力,先后对长江中下游、黄河下游、渭河下游、以及汉江中下游等河流的河型、现代河床过程问题进行了深入研究,不断取得有重要国内外影响的成果,出版了《渭河下游河流地貌》、《长江中下游河道特性及其演变》、《黄河下游河流地貌》等专著[5-7],中国河流地貌学科焕然一新。
沈玉昌等于1986年出版了《河流地貌概论》一书[8],系统总结了现代河床过程的基本规律,可概括为:水流与河床相互制约,河床变形的滞后现象,泥沙运动是水流与河床相互作用的纽带,河床自动调节作用,平衡条件下河床几何形态与水流泥沙及边界条件之间具有函数关系等。沈玉昌概括的这些规律,对研究中国冲积河流河床过程起到了十分重要的指导作用。该书是中国第一本河流地貌学专著,书中首次建立了河流地貌学的理论体系,在中国河流地貌学发展史上占有重要的地位。
20世纪90年代以来,中国河流地貌研究有了进一步的发展,不再局限于研究某一条河流的具体过程,更扩展到将河谷演化、流域侵蚀产沙、河流泥沙输移沉积、河床演变、三角洲造陆等集成在流域地貌系统的理论框架中,形成了有中国特色的河流地貌理论体系。近半个多世纪的时间证明,沈玉昌先生倡导的发展中国河流地貌学的方向是正确的。沈先生筚路蓝缕、呕心沥血,在中国开创了河流地貌学,并在包括河流地貌在内的中国地貌学研究中作出了杰出的贡献。今天,我们在深切缅怀沈先生不朽贡献的同时,对于中国河流地貌研究的新进展进行回顾和展望,以此来纪念先生100年诞辰。

2 水系发育与河谷地貌演变

2.1 大江大河水系历史发育

大江大河水系发育历史是中国地貌研究中的重大问题,尤其长江黄河两条大河,为人们关注,近百年来针对河流大拐弯、峡谷与沿河湖泊切割成因及其形成时代等河流发育的关键问题进行了大量研究。20世纪80年代以来,各种现代测年技术蓬勃发展,为河流发育史研究提供了新手段,使研究更深入和更精细。
黄河研究发现,黄河上游在距今1.2 Ma前发生的黄河运动使黄河切开积石峡流入临夏—兰州盆地,兰州黄河段最早形成于距今约1.7 Ma前,1.7 Ma以来形成了7级阶地[9]。1.2 Ma时不仅晋陕峡谷黄河出现,而且三门峡被切开,黄河东流的格局最终形成[10]。对于三门峡切开并形成东流入海的完整黄河时代,还有很多研究,但尚未取得一致。一些研究表明,小浪底以东黄河峡谷出口,最高级阶地砾石层上堆积的风成黄土的年代为距今1.165 Ma,由此推断,现代黄河东流入海的格局至少在1.165 Ma前就出现了[11]。另一些研究表明,三门湖盆沉积记录反映古三门湖水开始外流或三门峡部分切开的时代最早出现在0.41-0.35 Ma BP,黄河完全切穿三门峡、贯通东流入海的时代为0.15 Ma BP[12]
长江发育史研究集中在石鼓“长江第一湾”的金沙江袭夺、长江三峡切开和长江形成贯通水系的时代等问题上。沈玉昌先生曾对此研究,认为石鼓大拐弯系受地质构造所控制的先成河,而不是河流袭夺的结果,长江三峡远在古近纪已经形成[13]。近20年来对此又有许多研究,赵希涛等发现了虎跳峡出口处的大具盆地底部1.95 Ma BP和1.77 Ma BP的金沙江砾石层、攀枝花地区金沙江谷地昔格达组沉积之下沉积了距今4.2-5.0 Ma的金沙江砾石层,以此推论,在上新世早期古金沙江就已经存在了,此后不可能再发生金沙江袭夺问题[14]。但杨达源等认为,新近纪时期古长江为内陆水系,江汉盆地、洞庭盆地和四川盆地互不相通,长江三峡贯通的年代为1.00±0.20 Ma BP[15]。他根据在金沙江石鼓—宜宾河段发现一些地点存在“高阶地”堆积物等的测年数据,推测金沙江自下而上发生过袭夺贯通:云南永善—四川宜宾河段的袭夺贯通发生在距今103万年左右;禄劝乌东德峡谷—金坪子河段的袭夺贯通是在距今约80万年左右;虎跳峡峡谷的贯通并袭夺古中甸河大约发生在距今98万年前后[16]。最近,郑洪波等测定了与长江下游河流冲积物互层的玄武岩的40Ar/39Ar年代,同时还测定了这些沉积物中锆石砂粒的U-Pb年代。据此判断,从青藏高原而下贯通流入东海的长江,应该形成于距今2300万年以前,为长江水系的形成年代提供了新成果和新证据[17]。由上可见,河流发育历史的研究是个十分复杂问题,确定河流发育的时代还需综合深入研究。

2.2 山区河流地貌

对于山区河流的地貌研究取得新的进展。通过分析怒江、澜沧江和金沙江等山地河流流域内不同级别支流、不同河段支流和研究区所有支流的流域面积与其河道长度、河道比降之间关系,发现了构造作为主控因素的滇西河流演变的相似性和澜沧江上下两段演变的差异性,查明了滇西三江分水岭间横断面及纵剖面演化特点及分布规律[18-19]。以怒江、澜沧江以及金沙江的4个水文站的资料为基础,建立了历年及多年的流量—河宽、流量—水深、流量—流速关系,结果显示:河相关系理论对于非冲积性河流仍然适用,山地非冲积性河流与冲积河流在河道演变中遵循类似的规律;3条河流其河相关系的年际变化幅度逐渐减小,与它们受到构造抬升的影响减弱相适应[20]。对雅鲁藏布江的水系发育和河谷地貌进行了研究,发现总体呈现格状水系特点,同时具有树枝状水系的拓扑性质,这是由于河网发育过程中受到南北向挤压和东西向拉伸的新构造运动影响的结果;青藏高原阶段性不均匀抬升形成了宽窄相间的藕节状河道形态,宽阔河段为辫状河型、窄深河段为深切的V型河谷和单一顺直河型,纵剖面上构成裂点;裂点河段地块相对上升较快,阻滞了水流,使得大量卵石堆积,形成了平整而宽阔的U型河谷[21]。通过调查研究和分析发现,藏北长江源地区具有平行式水系格局,河谷地貌以形态不同的窄谷和宽谷为特点,其原因是新近纪以来该区主要经历了早期挤压和晚期伸展构造演化过程,产生了褶皱—逆冲、走滑剪切、正断层和地堑构造3种构造变形样式;新构造运动不仅控制了河谷地貌形态与水系格局,而且影响了河流阶地分布以及洪(冲)积扇的形态结构[22]。通过识别裂点和利用水力侵蚀模型计算,得出张家界世界地质公园索溪河谷侵蚀下切速率,推断张家界地貌(砂岩石柱地貌)发育起始于早更新世晚期[23]

3 侵蚀与产沙过程

3.1 有物理成因基础的侵蚀产沙模型

基于泥沙运动力学的基本概念,在概化的坡面上考虑影响侵蚀产沙的主要因素及其水力学关系,推导出坡面产沙量的计算公式,作为预测坡面产沙的计算模型;在此基础上利用数字流域模型框架建立了黄土高原多沙粗沙区产流产沙数学模型,该模型不仅模拟了产汇流过程、流水侵蚀与泥沙输移过程,而且也对重力侵蚀进行了定量表达。模型计算了黄土高原多沙粗沙区典型年份汛期的产流产沙量,得到了多沙粗沙区的汛期径流深分布图和产沙模数分布图。计算结果能够较好地解释黄河流域的“少水多沙”现象,为多沙粗沙区的水土保持工作提供了科学依据[24]。构建了由坡面子模型和沟坡子模型耦合而成的黄土高原丘陵沟壑区小流域侵蚀产沙模型,其坡面子模型引入坡面发生细沟侵蚀的判别计算,沟道子模型引入了泥沙输移比计算,并考虑了重力侵蚀和洞穴侵蚀的影响[25]

3.2 侵蚀产沙过程的尺度效应

大量研究揭示了侵蚀产沙过程对于空间和时间尺度的依赖。建立了考虑流域尺度影响的岔巴沟流域次暴雨泥沙输移比表达式,揭示了流域径流过程、侵蚀产沙过程、水沙关系随流域面积变化的规律[26]。通过对黄土丘陵沟壑区岔巴沟小流域的研究,发现了产沙模数与流域面积之间存在M型非线性关系,即随流域面积增大,出现了两个峰值[27];发现在不同的时间尺度上,含沙量—流量关系的滞后环性质是不同的,在次洪水尺度上出现逆时针滞后环,说明泥沙主要来源于坡面,不存在泥沙供应不足的现象;在月、年尺度上,出现顺时针滞后环,表明存在着泥沙的存贮—释放过程[28]。发现尺度效应方程与流域自然地理条件有关,在流域降雨、地貌、岩性和植被比较均一的情况下,流域产沙量随着流域面积的增大而减小;但当流域由多雨区向少雨区过渡、由风沙区、土石或基岩山地为主向以黄土丘陵沟壑为主转化、流域植被由覆盖茂密向稀疏状况转化等情况出现时,产沙模数将随流域面积增大而增大[29]。对黄土高原地区产沙模数的尺度效应进行分区研究表明,由于各分区的黄土、风沙、基岩的空间分布与组合关系不同、地形(坡度)不同,其产沙模数随流域面积变化的规律也不同;基于不同类型建立了校正方程,制作了消除尺度影响后的黄土高原产沙模数图[30]。通过对于黄土高原小流域水沙关系的研究,发现次洪总水、总沙关系可以用简单的比例函数来表示;植被减沙机制依赖于空间尺度,在坡面尺度上植被不仅通过减水来减沙,而且也通过改变水沙关系来减沙[31]。利用长江上游DEM、降雨、土地利用、土壤类型数据库和268个水文站的资料,研究了上游侵蚀输沙的尺度效应,发现长江上游输沙模数与流域面积之间呈负幂函数回归关系,这一关系主要产生于降雨侵蚀力因子和土壤可蚀性因子随流域面积的变化;在考虑了影响侵蚀产沙因子对输沙模数的作用后,输沙模数与流域面积之间呈正幂函数相关[32]

3.3 植被对侵蚀的影响及临界现象

开拓了植被—侵蚀动力学研究的新领域,讨论了作用于植被的各种生态应力,给出了定量表达式并且统一在植被—侵蚀动力学方程组中,推导得出了动力学方程组的理论解,并以理论解成功地模拟黄土高原安家沟流域和云南小江流域的植被侵蚀演变过程[33]。研究了降水—植被耦合关系及其对黄土高原侵蚀的影响,发现了森林覆盖率和降雨侵蚀力随年降水量的变化过程中的两个临界点,以及侵蚀强度随年降水量和植被覆盖度变化的临界点,为国际著名的Langbein-Schumm曲线的形成机理提供了新的解释[34]。研究了黄河中游不同自然带植被类型的变化、林、草的分布界线及植被的恢复能力,发现年降雨量530 mm是黄河中游林、草分布的临界年降雨量;在影响流域产沙的地带性、非地带性环境要素中,悬移质泥沙中径和林木覆盖率起主要作用[35]

3.4 坡面细沟发育过程模拟

利用自组织模型对坡面细沟发育过程和产沙动态变化进行了定量模拟,有效区分了坡面产沙过程中面蚀与沟蚀的贡献率;发现面蚀与沟蚀在侵蚀机理上有本质的区别,当坡度小于20°时,面蚀在总体侵蚀中所占的比例随坡度的增大而迅速减小,当坡度大于20°时,减小速度随坡度的继续增加明显变缓[36]

4 河床过程与河型

4.1 河道冲淤过程

基于非均匀不平衡泥沙运动基本理论建立了适合黄河下游特点的泥沙数学模型,并利用该模型研究了小浪底水库调水调沙运用对下游河道的减淤作用、区间引水与河道冲淤关系以及下游河道临界平衡等问题,得到了河道冲淤临界平衡阈值[37]。基于河床自动调整原理建立了水库泥沙淤积滞后响应的理论模型,利用该模型分析了三门峡库区累计淤积量对流量加权平均坝前水位的响应、潼关高程对年入库水量的响应及水库末端比降对年平均坝前水位的响应,表明这一理论模型能够描述泥沙淤积的特征,为三门峡等水库泥沙淤积的研究提供了一种新的方法[38]
基于不同粒径组的来沙量和淤积量的资料建立了统计模型,发现进入下游河道的> 0.025 mm的泥沙中,有43.73%淤积在河道中;进入下游河道的> 0.05 mm的泥沙中,有76.61%淤积在河道中;进入下游河道的> 0.10 mm的泥沙中,有97.68%淤积在河道中。在上中游拦减每1 t > 0.10 mm的泥沙在下游产生的减淤效果,是拦减每1 t > 0.05 mm泥沙产生的减淤效果的1.275倍;是拦减每1 t > 0.025 mm泥沙产生的减淤效果的2.234倍。这一成果为集中治理黄河中游> 0.10 mm泥沙产出区提供了重要依据[39]。以E. W. Lane所提出的关系式QJ~QsD50(Q为流量,J为比降,Qs为床沙质输沙率,D50为床沙中径)表示输沙平衡,运用黄河下游141次洪水的观测资料,建立了有一定物理意义的河道冲淤临界关系式,该关系式的判别准确率为86.5%,基于此式对于黄河下游河道治理提出了4种可能的选择[40]。建立河流河床比降与均衡比降关系模型,定量估算了黄河下游沿程淤积与溯源淤积对比关系随时间的变化,对于黄河下游长期淤积的原因进行了解释[41]

4.2 河床演变

发现冲积河流在能量转换过程中存在着一个特殊的平衡状态,并在此基础上建立了冲积河流平衡理论,该理论明确了决定冲积河流达到平衡状态时的水动力学条件为输沙效率最大,包含能坡最小或输沙量最大两个等同条件;冲积河流达到平衡时,河道过水断面形态具有唯一解,其具体表达式与基于实际观测资料建立起来的经验模型高度一致;冲积河流达到平衡状态时河道形态将以线性方式自动调整,这一特性可由一个不随尺度变化的无量纲数反映[42-45]。在悬移质泥沙对流扩散方程中增加了横向输沙项,引入适合游荡型河流的塌岸模式及局部动网格技术和网格融合技术,开发出可模拟游荡性河流河床演变且可反映河道整治工程作用的平面二维水沙数学模型,模拟出了黄河下游游荡型河流独特的河床演变过程[46]。将水深平均二维数字模型与河岸侵蚀模型结合,建立了水深平均二维水动力模型,数字模型与河岸侵蚀模型,成功地模拟了弯曲河道的侧向移动过程[47];将正弦派生曲线形河道流场分析解与河岸侵蚀后退模型相结合,研究了弯曲河道水流特性,区分了与曲率有关的次生流和与地形有关的次生流,深化了对于弯曲河道主流线移动过程的认识[48]
采用时间序列分析法对黄河下游河道断面形态参数变化趋势及其变异点进行了分析,发现20世纪50年代以来,特别是90年代以来,黄河下游花园口站、高村站、艾山站和利津站断面形态参数发生了趋势性变化,平滩流量下降,平滩面积、平滩河宽、平均水深、最大水深均出现不同程度的减小,平滩宽深比增大;变异点分析表明黄河下游河道主河槽总体上在1970-1975年开始萎缩,1990年以后进入严重萎缩期[49]。建立了黄河下游河道滩槽分流比的综合影响关系式,表明滩槽分流比随滩槽过水宽度比、过水深度比、过水面积比、流速比和主槽宽深比的增大而增大,随滩槽糙率比的增大而减小[50]。研究了黄河下游不同含沙量洪水过程中河床形态的调整,发现宽深比的变化剧烈,且与含沙量呈非线性相关,当含沙量较小时,洪水后宽深比随含沙量增大;但含沙量足够大以后,宽深比随含沙量减小[51]。利用1975-2011年多期遥感影像分析获得了宁蒙河段河道摆动速率、河道宽度和心滩数量变化过程,发现了整体萎缩趋势[52-53]。通过遥感影像、地貌沉积、历史文献与地图等研究发现,公元前2世纪时黄河上游后套冲积扇上黄河向东移,分为南北两汊,主流位于河套平原北部山前;18世纪早期至末期,黄河主河道南移至平原南部;19世纪中叶北汊淤塞,现代黄河形成[54]
基于黄河口河道的演变特征,提出了河口河道水位和纵比降变化的概化模式,采用滞后响应模型建立了河口河道同流量水位的计算方法,该计算方法能够连续地模拟河口淤积延伸及改道过程中河口河道特征水位的长期变化过程[55]。研究了黄河河口河道形态调整机理,揭示了影响河槽横断面形态自动调整的主要矛盾,提出河口河道治理的一种方法[56]。对于黄河小浪底工程建成后黄河河口区清水沟流路的淤积特征和变化趋势进行了研究,表明在小浪底水库初期蓄水拦沙运用阶段,淤积减少、河口砂嘴发展速度变缓;在后期正常调水调沙运用阶段,淤积又有所恢复,河口砂嘴发展加快[57]

4.3 河型成因与演变

对河型成因与判别方法研究取得新进展。在提出河床纵向稳定性和横向稳定性指标的基础上建立了河床综合稳定性指标Zw,当Zw < 5时,出现游荡型;当5 ≤ Zw ≤ 15时,出现分汊型;当Zw > 15时,出现弯曲型。经过近100条河流资料检验,效果较好[58]。基于输沙平衡程度概念认为不同冲积河流河型形成的根本原因在于其输沙平衡程度的不同,据此提出了冲积河流稳定程度公式,建立了河型分类与判别的模糊聚类计算方法[59]。在建立砂质河流和砾石河流河型的统一判别模式方面进行了尝试,利用包括国内外河流的大样本,基于能耗率、水流剪切力等水力学变量和河床约束性指标,建立了砂质河流和砾质河流河型的统一判别模式[60-61]。从河流阻力规律出发,通过分析河流断面形态、河床质中值粒径、河床水力半径与河流流态等参量之间的关系,得到河流形态参数的表达形式,提出了砂质和砾质河流河型的判别方法[62]。研究了来沙系数对河型的影响,发现给定流量时,高含沙曲流型的来沙系数最大,游荡型次之、弯曲型再次之,江心洲型最小;据此建立了基于来沙系数—流量关系的河型判别模式,确定了4种河型间的临界线[63]
对不同河型河道的演变与河型转化问题进行了深入研究,获得了新的成果。从辫状河、曲流河和网状河的河型转化实例,归纳了6种时间演化模式和5种空间转化模式,并讨论了河型时空演变模式间的相互关系;发现河型的时空演变受控于构造运动、海平面变化、气候、植被、沉积体系的物质组成、流域的水沙供给状况和水动力条件等,各因素在不同河型演变模式中的作用有所不同[64]。根据遥感影像和野外调查发现,冲积河道的沙洲大多遵循洲头淤积、洲体向上游逆向生长的发育模式;推导了沙洲沿程水头损失表达式,发现沙洲只有通过洲头向上游生长才能使沙洲河段的沿程水头损失达到最小,从而使这一模式得到合理的解释[65]。对黄河下游不同河型河段的沉积动力特征进行了比较,发现平滩流量时的流速辫状(游荡)河段较大,年际间变幅也较大,弯曲河段次之,顺直河段最小;单位河长能耗率辫状河段最大,弯曲河段次之,顺直河段最小;单位面积能耗率在辫状河段最小,弯曲河段最大,顺直河段次之[66]。对黄河源玛曲河段的研究发现,在270 km的流程上冲积河型发生了4次河型变化,其成因可归结为受地形限制、河床比降发生变化、支流入汇和河岸组成物质变化等[67]
对于长江、黄河不同河型河道的演变特性进行了研究。依据三峡水库蓄水以来大量原型观测资料的分析,发现长江中游各分汊河段普遍出现中枯水支汊分流比增加,支汊冲刷发展,中低滩冲刷变形,高滩滩缘崩退等现象,其原因是三峡水库蓄水后坝下游含沙量锐减、局部节点作用发生的变化以及主支汊河床组成存在差异[68]。对于三峡工程蓄水以来荆江沙质河段不同类型河床的演变特性进行了研究,发现蓄水初期上荆江深泓下切明显,但分汊放宽段航深不足问题突出;下荆江深泓冲淤相间,顺直(微弯)河段的深槽过渡段下移,弯道进口处水流较分散,致使航槽不稳定。基于数学模型计算结果预测了蓄水5~10年和15~20年后荆江河段航道的变化趋势[69]。研究了小浪底水库下游的河型变化,发现自1999年水库拦沙运用以来,游荡河段的整体游荡程度显著减弱,河势趋于稳定,主流线弯曲系数增大,这主要是由于水库长期下泄低含沙小流量过程、水流动力减弱,加之不断完善的河道整治工程所导致的结果[70];游荡型河段主河槽弯曲系数由1.12 增大到1.29,有向弯曲型转化的趋势;过渡性河段的主河槽弯曲系数由1.23增大到1.35,基本转变为弯曲型;限制性弯曲型河段的主河槽弯曲系数由1.19增大到1.25,其原因是水库的滞洪沉沙作用使下泄水流含沙量减小、泥沙粒径变细、洪峰调平,游荡型有向弯曲型转化的趋势[71]
对于以黄河为代表的游荡河流进行的研究,揭示了游荡河流演变的基本规律,阐明了水沙变化与河道整治对于黄河游荡河道演变的影响,提出了游荡河流演变的数值模拟技术和模型试验技术并运用于实际工程,将中国游荡河流的研究提高到一个新的水平[72]

5 河流地貌系统研究

S. A. Schumm建立的流域地貌系统理论和相关概念和方法[73],为河流地貌学研究提供了重要的理论框架。在这一框架中,中国河流地貌****研究从坡面、沟道、各级支流和河道的侵蚀和泥沙输移沉积过程,取得了进展。

5.1 黄河流域不同子系统的耦合关系

发现除了整个黄河流域地貌系统可以分为产水产沙系统、输移系统和沉积系统之外,以河口镇为界,黄河流域上游和中下游两部分也分别具有对应的产水系统、产沙系统和河道输移系统,二者间存在强耦合关系[74]。对于黄河流域从源到汇的泥沙侵蚀、输移和沉积进行了研究,发现黄河流域系统中存在着3个巨大的泥沙沉积汇,即上游宁蒙河段泥沙沉积汇、中游小北干流泥沙沉积汇、下游河道泥沙沉积汇,揭示了近60年尺度上3个沉积汇的来沙量、沉积量、输移比的变化规律及其与影响因素的关系;通过统计模型计算发现,来自黄河流域多沙粗沙区的每1 t泥沙,淤积在黄河下游河道的为0.455 t,而来自多沙细沙区的每1 t泥沙,淤积在黄河下游河道的仅为0.154 t,从而为多沙粗沙区水土流失的集中治理提供了重要的的决策依据[75-77];提出以“稀释效应”来解释子系统间的耦合机理,以河口镇以上清水区来水加入后多沙粗沙区洪水含沙量的减小幅度来定量表达稀释效应,得出河口镇以上清水区来水的稀释作用可以使黄河下游场次洪水的淤积量减少34%,并基于稀释效应指标计算出黄河下游冲淤临界值[78]

5.2 河流地貌系统中的高含沙水流和多营力地貌过程

开辟了以高含沙水流原理研究多泥沙河流地貌过程的新领域,发现:黄河多沙粗沙区高含沙水流的形成与风水两相作用密切相关;高含沙水流搬运与重力侵蚀的强耦合关系导致了黄土丘陵沟壑区的高强度侵蚀;高含沙水流形成于峁坡下部和沟坡,并在各级沟道中进一步发展;在坡面—沟道系统中,存在着泥沙的存贮—释放机制。提出宽变幅水沙两相流的概念,发现了宽变幅水沙两相流冲淤过程中的两个临界值;以冲淤双临界现象解释了黄河下游河道形态调整复杂响应现象和冲积河流河型对于含沙量变化的复杂响应现象[79-80]。基于284个水文站的资料研究了黄土高原区高含沙水流发生频率的空间分布规律及其与各影响因素之间的关系,发现高含沙水流发生频率高值区为东北—西南带状分布,存在3个高值中心区;灌木林、丘陵旱地、有林地面积百分比,黄土厚度,年平均降水量等因素对高含沙水流发生频率的相对贡献率依次为17%、4%、7%、30%、42%[81]。提出了多营力地貌过程新概念,系统地展开了风沙—黄土转换带多营力侵蚀过程的研究。提出了风力水力两相作用下的侵蚀产沙过程模式,为多沙粗沙区的高强度产沙机理提出了新的解释;研究了风水两相作用对高含沙水流的影响,提出一个简单的“运载工具”模式来描述高含沙水流的形成特性;发现随着风水两相作用指标的变化,悬沙中粗细颗粒存在着一种最优的搭配关系,使得含沙量达到最大;阐明了风力和水力作用对不同粒径组泥沙产沙行为的影响,发现较细粒径组的产沙模数在风水两相作用占优势的流域中最大,由此向以风力作用为主的流域过渡,或者向以水力为主的流域过渡,分组粒径产沙模数均减小[82-85]

5.3 河流地貌系统对于自然因素变化和人类活动的响应

水库的修建使河道成为受人为控制的系统。通过对长江上游资料的分析,发现当流域内水库对径流的实际调节系数小于10%时,宜昌站输沙量略有减小的趋势;当调节系数大于10%以后,输沙量迅速减小;在水库的建设、截流、蓄水拦沙的过程中,水库下游输沙量和含沙量的变化表现为先增大、达到峰值后再减小的复杂响应过程[86]。黄河上游刘家峡、龙羊峡水库修建后下游河道冲淤出现复杂响应现象,分为两个阶段,第一阶段为:刘家峡水库建成→拦截泥沙→库下游河道冲刷→随着水库的淤积库容减小拦沙作用减弱→库下游河道冲刷减弱;第二阶段为:龙羊峡水库修建→汛期和年流量减小→库下游区间来沙(支流来沙、入河风成沙)不能被搬走→河道淤积加剧,共同构成复杂响应的旋回,使得兰州以下河段经历了冲刷→冲刷减弱→淤积的变化过程[87]。研究揭示了黄河上游内蒙段泥沙冲淤阶段变化和河床演变过程及其与气候变化、水库建设、引水引沙等因素的定量关系,发现20世纪90年代前后内蒙河段强烈淤积的主要原因是相对前期上游来水减少、多沙支流来沙增加和水库拦沙量降低,大型水库径流调蓄增淤贡献较小[88-89]。阐明了黄河三角洲造陆过程对于夏季风强度变化和人类活动的响应,发现从20世纪60年代中期以来夏季风强度的持续减弱和人类活动减沙,是黄河三角洲造陆速率减慢的重要原因,三角洲造陆速率随夏季风强度指数的减弱而减少,随年气温的升高而减小,随梯田林草面积的增加而减小,随年净引水量的增加而减小[90]。提出河道输沙功能的定量指标,研究了流域自然因子和人类活动因子对黄河上游宁蒙河段和下游河道输沙功能的影响,分别建立了多元回归方程,对下游河道输沙功能降低的原因进行了定量解释,并提出了提高输沙功能的对策[91-92]
为了揭示在更长时间尺度上流域地貌系统对于自然与人为因素变化的响应,运用各种代用资料研究了黄河下游沉积速率和沉积量及黄河输沙量历史变化过程。依据14C测年数据及相关资料重建了全新世黄淮海平原的沉积历史,得到全新世黄河上中游的年平均来沙量约为8.0亿t,并确定人类活动增沙占现代黄河总来沙量的41%;通过大量沉积剖面与沉积物定年数据等资料分析,得到了黄河河口三角洲的泥沙淤积分布、1855年以来黄河泥沙输移系统的泥沙淤积分布以及近2600年来黄河下游沉积量和上中游产沙量变化过程,探讨了不同时间尺度上沉积量和产沙量变化与人类活动及其他影响因素的关系[93-96]。建立了黄河下游2300年以来的沉积速率的变化曲线,揭示了黄河流域地貌系统对气候变化及人类活动所导致的土地覆被、土地利用方式变化的响应过程,发现在人类活动导致沉积加速的过程中,公元7世纪至10世纪以及18世纪中叶以后表现为两个突变时期[97]

5.4 河流地貌系统中的泥沙灾害

对于流域系统的泥沙灾害类型及其划分原则进行了研究,将泥沙灾害按驱动力、灾害发生的地貌学系统、灾害的表现形式及具体灾害系统,分层次逐级进行分类;提出泥沙灾害具有自然地理地带性、垂直分带性、群发性、继发性、周期性、渐发性和突发性,以及复杂性和非线性等特征[98]。认为黄河下游“小水大灾”现象是黄河流域的一条典型的泥沙灾害链,链首是中游的渐发性侵蚀型泥沙灾害,链尾是放大的突发性洪水灾害,表现了泥沙灾害的异地传输性和时间积累效应,也表现了灾害的转移和放大过程[99]。对于黄河下游断流灾害进行了研究,基于径流量与河流基本功能之间的关系,提出了黄河功能性断流的概念,探讨了能够反映黄河功能性断流严重状况的基本因子,并基于聚类分析得出关于黄河功能性断流严重程度的分级标准,计算了黄河功能断流的级别[100]。研究了地震—山体滑坡—河道堰塞湖组成的泥沙灾害链,针对四川汶川“5.18”特大地震引起的滑坡堵塞河道形成的唐家山堰塞湖开发了平面二维水沙数学模型,揭示了堰塞湖泄流过程以及堰塞体冲刷发展的机制,计算得到的泄流流量、堰塞湖水位与实际观测值吻合较好[101]。将黄河上游支流十大孔兑高含沙水流淤堵黄河干流作为泥沙灾害事件,研究了淤堵洪水与非淤堵洪水的差异,通过统计分析提出了发生淤堵的水沙临界条件,建立了淤堵指标与干支流水沙条件的统计关系[102]
在泥石流的基础理论和泥石流对于河流地貌影响方面取得了新进展,为泥石流灾害的防治提供了依据。查明了中国泥石流、滑坡等山地灾害特征与分布规律,创建了较完善的中国泥石流、滑坡数据库,已经完成了580条典型泥石流沟和350个典型滑坡的编目;阐明了泥石流、滑坡等山地灾害的水平和垂直地带性,更科学地揭示了泥石流、滑坡的活动规律;研究了泥石流、滑坡的侵蚀和堆积机理,提出了确定侵蚀(冲刷)的深度和堆积范围的计算公式;对灾难性泥石流、滑坡进行了深入研究,阐明了与冰湖溃决相关的泥石流洪水灾害链和与雪崩(冰崩)、岩崩、滑坡相关的泥石流灾害链的形成机理及其对流域环境的影响[103]。着眼于泥石流产流的两个紧密相连的过程即含水量饱和或局部饱和土体的起动过程与起动后的流体化过程,提出了粘性泥石流产流的4种理想化情况及其相应的公式,划分了粘性泥石流产流的4种类型,深化了对粘性泥石流产流机理的认识[104]。统计获得中国受泥石流危害与威胁的县级及其以上的城镇达150余个,分布在20个省级行政区及特别行政区内,占省级行政区总数的58.82%。由于城镇的人口密度大、建筑物多,经济相对发达,故泥石流活动造成的人口伤亡多、财产损失重,严重影响城镇的安全和发展[105]。通过原型观测和试验对粘性泥石流泥深与残留层的关系进行了研究,发现在后继粘性泥石流作用下,除底部很薄的一层不动外,残留层是运动的;并提出了基于泥石流容重和沟床比降等计算残留层厚度和确定当时泥深的方法[106]。基于西藏东南部4条典型泥石流沟的观测资料,研究了泥石流堵塞坝形成的主要因素和机理,发现冰雪崩、冰湖溃决或大规模滑坡活动所激发的首阵或前几阵大流量、高速度、多巨砾并与主河正交的粘性泥石流,最容易形成堵塞坝[107]

5.5 河流地貌系统的实验研究

对于实验室河流模拟中的地貌作用行为相似准则进行了扩展,提出其内涵应包括地貌形态统计特征、物质组成比例与层次结构比例、相对时间尺度及相对速率、因果关系以及消能率及消能方式等方面的相应或相似[108-109]
通过室内人工降雨条件下的模型试验研究了水系的发育过程,发现产沙过程具有波动振荡衰减特征,水系发育以增加河道(沟道)数目及弯曲拉伸长度两种方式进行最小消能,水系分数维值随时间呈不对称上凹型曲线;产沙过程的振荡性、衰减率随物质变粗而加强,河道数目随物质变细而增多[110-112]。模拟了侵蚀基准面下降对流域水系演变及产沙的影响,发现水系发育以增加河道(沟道)数目及流域出口段河道下切、溯源侵蚀延伸长度两种方式进行消能,在时间上产沙过程具有复杂响应特征,在空间上其影响随远离流域出口而减弱[113]。通过黄土坡面发育实验发现侵蚀过程主要经历三个阶段:面蚀与细沟侵蚀为主阶段,侵蚀量不平衡的细沟和浅沟侵蚀为主阶段,以及侵蚀量相对稳定的浅沟和细沟侵蚀为主阶段;坡面地貌形态的时间变化反映了黄土地貌由幼年期、中年期及侵蚀趋于平衡时的老年期组成的完整过程[114]
通过对游荡型模型小河塑造和发育的时空演变过程的研究,发现其时间和空间演替过程可以相互替代,为空代时假说提供了新的证据;揭示了游荡河型发育过程中出现的时空复杂响应现象[115]。对于网状河的实验模拟表明,网状河流的形成是河漫滩上的河道化过程,决口漫流对原泛滥盆地区下切侵蚀,逐渐归并为几条相互连通的河道;网状河道成熟阶段,局部河段的淤积导致个别河道的决口及废弃[116]。发现基面下降导致复杂响应普遍存在于江心洲分汊河型及游荡河型的发育过程中,当江心洲河型受到一次侵蚀基面下降影响时,出现新老江心洲套叠现象,而游荡河型表现为时间复杂响应和空间复杂响应[117-119]。模型小河发育过程中,其纵剖面存在非线性分形特征[120]
在弯曲—游荡性过渡型河道造床实验基础上模拟了穹隆抬升对弯曲—游荡性过渡型河道发育影响实验及坳陷沉降对弯曲—游荡性过渡型河道发育影响实验,发现弯曲—游荡过渡型的发育过程比江心洲河型来得快,只需江心洲河型发育时间的三分之一;冲积河道对构造活动的影响具有强烈的敏感性。构造运动的速率与河道水流的造床速率差别很大,如何在实验中进行协调是需要解决的问题[121]

6 结语与展望

6.1 结语

综观20年来中国河流地貌学的发展,我们深深感到,沿着沈玉昌先生与钱宁先生倡导的地貌学与河流动力学、泥沙运动力学相结合的方向展开河流研究已经取得了初步突破。河流地貌学****不断学习和吸收河流动力学、泥沙运动力学的理论和方法,建立地貌学概念与物理学原理相结合的模型,定量化程度大为提高;河流动力学和泥沙运力学****吸收某些地貌学的概念和理论(如地貌临界、地貌过程复杂响应和流域地貌系统原理),致力于以物理和数学方法解决地貌****提出但尚未很好解决的某些问题(如黄土高原侵蚀模型中重力侵蚀的定量化、地貌临界与地貌过程复杂响应的定量表达),使泥沙数学模型更能适应不同时空尺度下流域产沙与河流演变模拟的需要。中国在高含沙水流及多泥沙河流地貌过程、河流泥沙和河床演变数学模型及工程应用等方面已跻身国际先进水平,若干重要成果为黄河、长江等大江大河的治理和重大工程决策提供了依据。值得高兴的是,中国科学院地理科学与资源所地貌研究室从国外引进河流动力学背景的高层次人才,建立了河流动力学研究方向;水利学****提出“从河流泥沙到流域泥沙”的泥沙研究方向,为河流地貌学与水力学研究的进一步融合发展提供了新的机遇。我们相信,如果能够亲眼目睹上述进展,两位中国河流学科研究的先行者自会感到十分欣慰。

6.2 展望

为了使中国河流地貌学研究继续前进,需要对以下方面予以深化:
(1)基于多种测年技术定年、物理模型实验与数学模拟的大江大河水系发育史研究,如长江水系发育史、黄河水系发育史;
(2)河流地貌系统对于新构造运动、气候变化和人类活动响应的模拟研究;
(3)非稳定状态下的河流动力地貌过程(Morphodynamics of rivers beyond steady state)研究[122],揭示其复杂性、敏感性及前兆性特征;
(4)河流地貌系统中以水为载体的多元物质(泥沙、污染物、生源要素)迁移过程及其生态效应;
(5)河流地貌学中若干难题的进一步破解,如河型的成因与模拟(如弯曲河型的成因与模拟)、河相关系方程组的封闭求解等;
(6)加强科研、大专院校及工程部门间,地学、水利泥沙及环境学专业等的河流地貌研究力量的协作与融合。
The authors have declared that no competing interests exist.

参考文献 原文顺序
文献年度倒序
文中引用次数倒序
被引期刊影响因子

[1]Editorial Group of Geomorphology Selections from Shen Yuchang. Prof. Shen Yuchang and Modern Geomorphology
. Geographical Research, 1997, 16(1): 77-84.
Magsci [本文引用: 1]摘要
沈玉昌教授是我国着名的地理学家和杰出的地貌学家。在60年的地理科学工作中,他对我国现代地貌学发展做出了卓越的贡献。从河流地貌、地貌区划与地貌制图、应用地貌等方面进行了综述。
[沈玉昌地貌学文选编辑组. 沈玉昌与中国现代地貌学
. 地理研究, 1997, 16(1): 77-84.]
Magsci [本文引用: 1]摘要
沈玉昌教授是我国着名的地理学家和杰出的地貌学家。在60年的地理科学工作中,他对我国现代地貌学发展做出了卓越的贡献。从河流地貌、地貌区划与地貌制图、应用地貌等方面进行了综述。
[2]Shen Yuchang.River valley geomorphology and development history of Hanjiang River
. Acta Geographica Sinica, 1956, (4): 296-323.
https://doi.org/10.11821/xb195604002URL [本文引用: 1]摘要
正汉水亦称汉江,为我国古代所谓四渍之一,禹贡云:“幡冢导漾,东流为汉,”故汉水在沔县以上又有汉水和沔水之称;过襄阳以后又名襄河(图1)。
[沈玉昌, 1956. 汉水河谷的地貌及其发育史
. 地理学报, 1956(4): 296-323. ]
https://doi.org/10.11821/xb195604002URL [本文引用: 1]摘要
正汉水亦称汉江,为我国古代所谓四渍之一,禹贡云:“幡冢导漾,东流为汉,”故汉水在沔县以上又有汉水和沔水之称;过襄阳以后又名襄河(图1)。
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[沈玉昌. 长江上游河谷地貌. 北京: 科学出版社, 1965.] [本文引用: 1]
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[沈玉昌. 走地理水利共同协作的道路//《纪念钱宁同志》文集. 北京: 清华大学出版社, 水利电力出版社, 1987: 172-176.] [本文引用: 1]
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[中国科学院地理所渭河研究组. 渭河下游河流地貌. 北京: 科学出版社, 1983.]URL [本文引用: 1]
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[中国科学院地理研究所, . 长江下游河道特性及其演变. 北京: 科学出版社, 1985.]URL
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[叶青超, 陆中臣, 杨毅芬, . 黄河下游河流地貌. 北京: 科学出版社, 1990.]URL [本文引用: 1]
[8]Shen Yuchang, Gong Guoyuan.An Introduction to River Geomorphology. Beijing: Science Press, 1986.URL [本文引用: 1]

[沈玉昌, 龚国元. 河流地貌概论. 北京: 科学出版社, 1986.]URL [本文引用: 1]
[9]Li Jijun, Fang Xiaomin, Ma Haizhou, et al.Geomorphological and environmental evolution in the upper reaches of the Yellow River during the late Cenozoic
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[本文引用: 1]

[李吉均, 方小敏, 马海洲, . 晚新生代黄河上游地貌演化与青藏高原隆起
. 中国科学D辑, 1996, 26(4): 316-322.]
[本文引用: 1]
[10]Pan Baotian, Hu Zhenbo, Hu Xiaofei, et al.Time-slice of the fluvial evolution in the northern Jinshaan Gorge during late Cenozoic
. Quaternary Sciences, 2012, 32(1): 111-120.
Magsci [本文引用: 1]摘要
晋陕峡谷黄河形成的时代是地学界十分关注的科学问题,长期存在比较大的意见分歧,至今没有得到比较好的解决。山西保德地区发育一套晚中新世-早上新世的河湖相沉积,年代为&gt;8.3~3.7Ma, 地貌与地层分析表明,它们是唐县期夷平面的相关沉积。河湖相地层所含砾石层的组构和岩性统计揭示,当时汇入古湖的河流是发源于周围抬升区的短小河流,形成一个局地规模的湖泊水系。晋陕峡谷北段唐县期夷平面之上分布两期红粘土覆盖的河流砾石层,形成年代分别在4.9Ma前和3.7Ma前; 砾石组构和岩性统计揭示,它们所指示的河流流向向北,与黄河流向相反,是一个不同于现代黄河的古河流,它将保德古湖水系与河套盆地联系起来。3.7Ma前,强烈的地面上升导致河湖相沉积结束和唐县期夷平面抬升,风成红粘土堆积其上,地形起伏增大,河流溯源侵蚀加剧,水系进入重新组织阶段; 1.2Ma前,黄土高原南部的河流将原北流水系袭夺,黄河形成; 最近1.2Ma的强烈地面上升,导致黄河不断下切并发育多级阶地,逐渐形成现代壮观的深切峡谷地貌。
[潘保田, 胡振波, 胡小飞, . 晋陕峡谷北段晚新生代河流演化初步研究
. 第四纪研究, 2012, 32(1): 111-120.]
Magsci [本文引用: 1]摘要
晋陕峡谷黄河形成的时代是地学界十分关注的科学问题,长期存在比较大的意见分歧,至今没有得到比较好的解决。山西保德地区发育一套晚中新世-早上新世的河湖相沉积,年代为&gt;8.3~3.7Ma, 地貌与地层分析表明,它们是唐县期夷平面的相关沉积。河湖相地层所含砾石层的组构和岩性统计揭示,当时汇入古湖的河流是发源于周围抬升区的短小河流,形成一个局地规模的湖泊水系。晋陕峡谷北段唐县期夷平面之上分布两期红粘土覆盖的河流砾石层,形成年代分别在4.9Ma前和3.7Ma前; 砾石组构和岩性统计揭示,它们所指示的河流流向向北,与黄河流向相反,是一个不同于现代黄河的古河流,它将保德古湖水系与河套盆地联系起来。3.7Ma前,强烈的地面上升导致河湖相沉积结束和唐县期夷平面抬升,风成红粘土堆积其上,地形起伏增大,河流溯源侵蚀加剧,水系进入重新组织阶段; 1.2Ma前,黄土高原南部的河流将原北流水系袭夺,黄河形成; 最近1.2Ma的强烈地面上升,导致黄河不断下切并发育多级阶地,逐渐形成现代壮观的深切峡谷地貌。
[11]Pan Baotian, Wang Junping, Gao Hongshan, et al.Paleomagnetic dating of the topmost terrace in Kouma, Henan and its indication to the Yellow River's running through Sanmen Gorges
. Chinese Science Bulletin, 2005, 50(3): 255-261.
Magsci [本文引用: 1]摘要
小浪底以东的黄河峡谷的出口地区发育有多级阶地, 其中以河南堰师市扣马附近黄河南岸的阶地最为典型. 在那里黄河发育了三级阶地, 其中最高级阶地砾石层高出河面30~35 m, 其上堆积60 m厚的风成黄土, 黄土地层中夹多条棕红色古土壤, 最底部发育了S14. 系统的磁性地层学和黄土、古土壤系列对比研究表明, 最高级阶地上黄土的年代为1165 ka. 由此推断, 该级黄河阶地至少形成于此前, 现代黄河东流入海的格局至少在1.165 Ma前就出现了.
[潘保田, 王均平, 高红山, . 河南扣马黄河最高级阶地古地磁年代及其对黄河贯通时代的指示
. 科学通报, 2005, 50(3): 255-261.]
Magsci [本文引用: 1]摘要
小浪底以东的黄河峡谷的出口地区发育有多级阶地, 其中以河南堰师市扣马附近黄河南岸的阶地最为典型. 在那里黄河发育了三级阶地, 其中最高级阶地砾石层高出河面30~35 m, 其上堆积60 m厚的风成黄土, 黄土地层中夹多条棕红色古土壤, 最底部发育了S14. 系统的磁性地层学和黄土、古土壤系列对比研究表明, 最高级阶地上黄土的年代为1165 ka. 由此推断, 该级黄河阶地至少形成于此前, 现代黄河东流入海的格局至少在1.165 Ma前就出现了.
[12]Wang Sumin, Wu Xihao, Zhang Zhenke, et al.Sedimentary records of environmental evolution in the Sanmen Lake Basin and the Yellow River running through the Sanmenxia Gorge eastward into the sea
. Science in China Series D: Earth Sciences, 2002, 31(9): 760-768.
https://doi.org/10.3321/j.issn:1006-9267.2001.09.008URL [本文引用: 1]摘要
晚新生代黄河中游地区发育一系列独立的湖盆, 其中三门湖盆发育了巨厚的三门系地层, 是研究黄河中游地质环境变迁的构造-气候旋回和黄河形成演化的理想之地. 对三门峡水库左岸山西省平陆境内黄底沟附近天然剖面沉积记录的磁性地层、孢粉、有机碳和碳酸盐含量进行了分析, 建立了近5.0 MaBP以来的环境演化序列、区域构造活动和湖盆演化过程. 古三门湖盆沉积记录的气候变迁显示: 大约5.4 MaBP构造成盆, 3.6 MaBP构造运动之后, 湖泊扩张, 夏季风降水增加; 相当于黄土底界的2.60 MaBP左右并未出现气候的巨大转折, 奥杜维尔正向事件之后(约从1.77 MaBP开始)沉积记录中云冷杉出现, 气候转向偏冷; 1.2 MaBP构造运动造成上下三门系之间的轻度角度不整合; 黄土旺盛堆积时期(L15, L9, L6)古三门湖沉积记录显示冷湿的气候特征. 三门湖盆沉积记录的区域构造活动加强时段和青藏高原隆升的构造活动具有时间上的一致性. 沉积记录反映古三门湖水开始外流或三门峡部分切开的时代最早出现在0.41~0.35 MaBP, 黄河完全切穿三门峡、贯通东流入海的时代为0.15 MaBP, 标志现代意义上的黄河形成, 并对中下游地貌和环境演化产生巨大影响.
[王苏民, 吴锡浩, 张振克, . 三门古湖沉积记录的环境变迁与黄河贯通东流研究
. 中国科学(D辑), 2001, 31(9): 760-768.]
https://doi.org/10.3321/j.issn:1006-9267.2001.09.008URL [本文引用: 1]摘要
晚新生代黄河中游地区发育一系列独立的湖盆, 其中三门湖盆发育了巨厚的三门系地层, 是研究黄河中游地质环境变迁的构造-气候旋回和黄河形成演化的理想之地. 对三门峡水库左岸山西省平陆境内黄底沟附近天然剖面沉积记录的磁性地层、孢粉、有机碳和碳酸盐含量进行了分析, 建立了近5.0 MaBP以来的环境演化序列、区域构造活动和湖盆演化过程. 古三门湖盆沉积记录的气候变迁显示: 大约5.4 MaBP构造成盆, 3.6 MaBP构造运动之后, 湖泊扩张, 夏季风降水增加; 相当于黄土底界的2.60 MaBP左右并未出现气候的巨大转折, 奥杜维尔正向事件之后(约从1.77 MaBP开始)沉积记录中云冷杉出现, 气候转向偏冷; 1.2 MaBP构造运动造成上下三门系之间的轻度角度不整合; 黄土旺盛堆积时期(L15, L9, L6)古三门湖沉积记录显示冷湿的气候特征. 三门湖盆沉积记录的区域构造活动加强时段和青藏高原隆升的构造活动具有时间上的一致性. 沉积记录反映古三门湖水开始外流或三门峡部分切开的时代最早出现在0.41~0.35 MaBP, 黄河完全切穿三门峡、贯通东流入海的时代为0.15 MaBP, 标志现代意义上的黄河形成, 并对中下游地貌和环境演化产生巨大影响.
[13]Shen Yuchang, Yang Yichou.New research on the problem of river-capture of Ching-Sha-Chiang (the upper Yangtze), western Yunnan, China
. Acta Geographica Sinica, 1963, 29(2): 87-108.
https://doi.org/10.11821/xb196302001URL [本文引用: 1]摘要
正金沙江在云南丽江县石鼓以上自西北流向东南,到石鼓附近突然拐了一个大弯,向东北流去,造成了一个马蹄形的弯曲。这个奇特的大弯曲一向被称为“长江第一弯”,很早就引起了中外地理学家和地貭学家的注意,并提出了各种各样的解释。过去多数****认为
[沈玉昌, 杨逸畴. 滇西金沙江袭夺问题的新探讨
. 地理学报, 1963, 29(2): 87-108.]
https://doi.org/10.11821/xb196302001URL [本文引用: 1]摘要
正金沙江在云南丽江县石鼓以上自西北流向东南,到石鼓附近突然拐了一个大弯,向东北流去,造成了一个马蹄形的弯曲。这个奇特的大弯曲一向被称为“长江第一弯”,很早就引起了中外地理学家和地貭学家的注意,并提出了各种各样的解释。过去多数****认为
[14]Zhao Xitao, Hu Daogong, Zhang Yongshuang.Genesis and age of the gravels underlying the Xigeda formation of Panzhihua, Sichuan, China, and valley development of the ancient Jinsha River
. Acta Geoscientica Sinica, 2008, 29(1): 1-12.
https://doi.org/10.3321/j.issn:1006-3021.2008.01.001URL [本文引用: 1]摘要
本文主要描述和讨论了四川省攀枝花市沿金沙江分布、并以炳草岗地龙箐剖面为代表的昔格达组湖相沉积下伏的砾石层的沉积特征及其河流相成因。根据前人对昔格达组湖相沉积的磁性地层学研究结果,为4.2/3.28-2.6/2.12/1.78MaBP的上新世中、晚期或至早更新世早期,表明其下伏厚达50m的砾石层的形成时代约为4.2-4.5/5MaBP的上新世早期。早上新世金沙江河流相砾石层在接近金沙江谷底位置的发现,表明金沙江很早就已经从青藏高原主夷平面下切了2000m以上、已在接近其现今谷底的位置上存在。这对于探讨古金沙江的河谷发育及其与青藏高原隆升的关系,具有重要的指示意义。
[赵希涛, 胡道功, 张永双. 四川攀枝花昔格达组下伏砾石层成因和时代探讨与古金沙江河谷发育
. 地球学报, 2008, 29(1): 1-12.]
https://doi.org/10.3321/j.issn:1006-3021.2008.01.001URL [本文引用: 1]摘要
本文主要描述和讨论了四川省攀枝花市沿金沙江分布、并以炳草岗地龙箐剖面为代表的昔格达组湖相沉积下伏的砾石层的沉积特征及其河流相成因。根据前人对昔格达组湖相沉积的磁性地层学研究结果,为4.2/3.28-2.6/2.12/1.78MaBP的上新世中、晚期或至早更新世早期,表明其下伏厚达50m的砾石层的形成时代约为4.2-4.5/5MaBP的上新世早期。早上新世金沙江河流相砾石层在接近金沙江谷底位置的发现,表明金沙江很早就已经从青藏高原主夷平面下切了2000m以上、已在接近其现今谷底的位置上存在。这对于探讨古金沙江的河谷发育及其与青藏高原隆升的关系,具有重要的指示意义。
[15]Yang Dayuan.Studies on the Yangtze River. Nanjing: Hohai University Press, 2004.https://doi.org/10.3969/j.issn.1000-0690.2004.01.015URL [本文引用: 1]摘要
三峡库区以山地为主,人口密度较大,三峡工程引起的移民搬迁以及 经济建设的需要,造成坡地上人类活动强度越来越大,从而造成现代坡地剥蚀作用的加剧.采用简便、实用且操作方便的地貌测量方法,对三峡库区草堂河流域三个 坡段进行了现代坡地剥蚀速率研究.结果表明,<15°的缓坡、15°~45°的斜坡和>45°的陡坡的现代剥蚀速率分别为4.0、4.9和7.1 mm/a.当地平均现代坡地剥蚀速率已达4.9 mm/a(7 902 t/km2·a),即达到强度剥蚀标准,未来三峡库区坡地退耕还林(草)以及水土保持等生态建设任务十分艰巨.
[杨达源. 长江研究. 南京:河海大学出版社, 2004.]https://doi.org/10.3969/j.issn.1000-0690.2004.01.015URL [本文引用: 1]摘要
三峡库区以山地为主,人口密度较大,三峡工程引起的移民搬迁以及 经济建设的需要,造成坡地上人类活动强度越来越大,从而造成现代坡地剥蚀作用的加剧.采用简便、实用且操作方便的地貌测量方法,对三峡库区草堂河流域三个 坡段进行了现代坡地剥蚀速率研究.结果表明,<15°的缓坡、15°~45°的斜坡和>45°的陡坡的现代剥蚀速率分别为4.0、4.9和7.1 mm/a.当地平均现代坡地剥蚀速率已达4.9 mm/a(7 902 t/km2·a),即达到强度剥蚀标准,未来三峡库区坡地退耕还林(草)以及水土保持等生态建设任务十分艰巨.
[16]Yang Dayuan, Han Zhiyong, Ge Zhaoshuai, et al.Geomorphic process of the formation and incision of the section from Shigu to Yinbin of the Jinshajiang River
. Quaternary Sciences, 2008, 28(4): 564-568.
https://doi.org/10.3321/j.issn:1001-7410.2008.04.007URL [本文引用: 1]摘要
近年来,在长江金沙江石鼓-宜宾河段进行了大量的调查研究,发现了云南巧家附近的古河谷;并在金沙江永善-宜宾河段两岸多处发现了"高阶地","高阶地"堆积物的物质成分比较单一,而且互相之间有明显差别.根据各地"高阶地"堆积物的测年资料,推测金沙江云南永善-四川宜宾河段的袭夺贯通,发生在距今103万年左右;禄劝乌东德峡谷-金坪子河段的袭夺贯通是在距今约80万年左右;虎跳峡峡谷的贯通并袭夺古中甸河大约发生在距今98万年前后.金沙江贯通以来强烈深切,平均深切速率为25~30cm/ka,但近十多万年以来平均深切速率达到99~77cm/ka.
[杨达源, 韩志勇, 葛兆帅, . 金沙江石鼓—宜宾河段的贯通与深切地貌过程的研究
. 第四纪研究, 2008, 28(4): 565-568.]
https://doi.org/10.3321/j.issn:1001-7410.2008.04.007URL [本文引用: 1]摘要
近年来,在长江金沙江石鼓-宜宾河段进行了大量的调查研究,发现了云南巧家附近的古河谷;并在金沙江永善-宜宾河段两岸多处发现了"高阶地","高阶地"堆积物的物质成分比较单一,而且互相之间有明显差别.根据各地"高阶地"堆积物的测年资料,推测金沙江云南永善-四川宜宾河段的袭夺贯通,发生在距今103万年左右;禄劝乌东德峡谷-金坪子河段的袭夺贯通是在距今约80万年左右;虎跳峡峡谷的贯通并袭夺古中甸河大约发生在距今98万年前后.金沙江贯通以来强烈深切,平均深切速率为25~30cm/ka,但近十多万年以来平均深切速率达到99~77cm/ka.
[17]Zheng Hongbo, Peter D Clift, Wang Ping, et al.Pre-Miocene birth of the Yangtze River
. Proceedings of the National Academy of Sciences, 2013, 110(19): 7529-960.
https://doi.org/10.1073/pnas.1216241110URLPMID:23610418 [本文引用: 1]摘要
The development of fluvial systems in East Asia is closely linked to the evolving topography following India-Eurasia collision. Despite this, the age of the Yangtze River system has been strongly debated, with estimates ranging from 40 to 45 Ma, to a more recent initiation around 2 Ma. Here, we present (40)Ar/(39)Ar ages from basalts interbedded with fluvial sediments from the lower reaches of the Yangtze together with detrital zircon U-Pb ages from sand grains within these sediments. We show that a river containing sediments indistinguishable from the modern river was established before ~23 Ma. We argue that the connection through the Three Gorges must postdate 36.5 Ma because of evaporite and lacustrine sedimentation in the Jianghan Basin before that time. We propose that the present Yangtze River system formed in response to regional extension throughout eastern China, synchronous with the start of strike-slip tectonism and surface uplift in eastern Tibet and fed by strengthened rains caused by the newly intensified summer monsoon.
[18]Wang Suiji, Wu Shaohong, Dai Erfu.Statistical relationships between geomorphic parameters: A case study of the Yunnan reach of the Lancangjiang River in southwestern China
. International Journal of Sediment Research, 2007, 22(2): 131-141.
https://doi.org/10.1002/hyp.6800URL [本文引用: 1]摘要
The properties of rivers and their catchments can be expressed by statistical relationships between geomorphic parameters. These statistical relationships may reveal some inherent differences in geomorphic evolution for different reaches or different order tributaries of a river basin. A case study was undertaken of the Yunnan reach of the Langcangjiang River. The catchment area, channel length and gradient of the first-, second- and third-order tributaries all with catchment areas larger than 100 km(2) in the Yunnan reach were the main geomorphic parameters evaluated. The correlation between catchment area and channel length as well as between catchment area and channel gradient with respect to the total tributaries, different reach tributaries, and different order tributaries were revealed using statistical methods. In general, the channel length as a function of catchment area, was best expressed by a quadratic function where channel length increases with increasing catchment area (half parabola), while the channel gradient as a function of catchment area is best expressed by an exponential decay function. Comparison of the best-fit formulas revealed the following phenomena: the lower Yunnan reach tributaries and the first-order tributaries have a dominant effect on geomorphic parameters of the total tributaries. In addition, the statistical relationships indicate that the river geomorphic system in the upper and lower Yunnan reaches evolved differently. This study method used to differentiate river characteristics by determining statistical relationships between geomorphic parameters may be extended to other rivers and their catchments.
[19]Wang Suiji, Wu Shaohong, He Daming, et al.Comparability in geomorphic evolution among the three rivers in the northern longitudinal range-gorge region: Evidence of statistic relationships between geomorphic parameters and analyses of cause of formation
. Chinese Science Bulletin, 2006, 51(Suppl): 39-49
https://doi.org/10.1007/s11434-006-0039-2URL [本文引用: 1]摘要
Nujiang River; Lancang River; Jinsha River; geomorphic parameter; statistical relationship; northwestern Yunnan Province
[20]Wang Suiji, Wei Quanwei, Tan Lihua, et al.River regime and its variety of the mountainous rivers
. Journal of Mountain Science, 2009, 27(1): 5-13.
https://doi.org/10.3969/j.issn.1008-2786.2009.01.002URL [本文引用: 1]摘要
河相关系理论迄今总是应用于冲积河流的研究中并取得了很好的效果,但尚未应用在非冲积性山地河流的研究中。河相关系理论是否适用于非冲积性河流的研究?该研究选取滇西山地河流,以怒江道街坝、澜沧江旧州和景洪、以及金沙江石鼓4个水文站的历年实测水文资料为基础,探讨了上述4站有水文资料记载时段的历年及多年的流量~河宽、流量~水深、流量~流速关系,揭示其年际变化特征。结果显示,河相关系理论在研究非冲积性河流当中同样存在很好的效果,表明山地非冲积性河流与冲积河流在河道演变中遵循类似的规律。研究区北段从西部的怒江到中部的澜沧江,再到东部的金沙江,其河相关系的年际变化幅度逐渐减小,与它们受到构造抬升的影响减弱相适应。澜沧江河相关系的年际变化在北部相对不明显,在南部则相对显著,这与其南北两段的地貌分异有关,也与中下游的大坝建设等人类活动引起南部河床的冲淤强度的增大有关。系数积及指数和表明,山地河流由于受到基岩边界的影响,其流水断面的调整中河宽、水深和流速之间的协调能力比冲积性河流的小。另外,建立了流水断面宽深比与流量之间的河相关系式,丰富了河相关系的研究内容,并在研究区不同河流、不同河段的流量预测或断面形态预测中具有重要的意义。
[王随继, 魏全伟, 谭利华, . 山地河流的河相关系及其变化趋势
. 山地学报, 2009, 27(1): 5-13.]
https://doi.org/10.3969/j.issn.1008-2786.2009.01.002URL [本文引用: 1]摘要
河相关系理论迄今总是应用于冲积河流的研究中并取得了很好的效果,但尚未应用在非冲积性山地河流的研究中。河相关系理论是否适用于非冲积性河流的研究?该研究选取滇西山地河流,以怒江道街坝、澜沧江旧州和景洪、以及金沙江石鼓4个水文站的历年实测水文资料为基础,探讨了上述4站有水文资料记载时段的历年及多年的流量~河宽、流量~水深、流量~流速关系,揭示其年际变化特征。结果显示,河相关系理论在研究非冲积性河流当中同样存在很好的效果,表明山地非冲积性河流与冲积河流在河道演变中遵循类似的规律。研究区北段从西部的怒江到中部的澜沧江,再到东部的金沙江,其河相关系的年际变化幅度逐渐减小,与它们受到构造抬升的影响减弱相适应。澜沧江河相关系的年际变化在北部相对不明显,在南部则相对显著,这与其南北两段的地貌分异有关,也与中下游的大坝建设等人类活动引起南部河床的冲淤强度的增大有关。系数积及指数和表明,山地河流由于受到基岩边界的影响,其流水断面的调整中河宽、水深和流速之间的协调能力比冲积性河流的小。另外,建立了流水断面宽深比与流量之间的河相关系式,丰富了河相关系的研究内容,并在研究区不同河流、不同河段的流量预测或断面形态预测中具有重要的意义。
[21]Yu Guoan, Wang Zhaoyin, Liu Le, et al.Drainage network and fluvial morphology features of Yarlung Tsangpo River under the impact of neotectonic movement
. Advances in Water Science, 2012, 23(2): 163-169.
https://doi.org/CNKI: 32.1309.P.20120224.2003.012Magsci [本文引用: 1]摘要
雅鲁藏布江(雅江)水系发育和河流地貌演变受新构造运动的强烈影响。通过野外调查,结合SRTM(航天飞机雷达地形测绘使命)数据分析和Google Earth三维地图功能,对雅江河网形态及河流地貌特征进行了分析,并采用EH4电磁成像系统测量了雅江及其支流宽谷河道淤沙深度。研究发现,雅江河网呈现格状水系特点,同时具有枝状河网的拓扑性质,这主要是由于新构造运动的影响,河网发育过程中受到南北向挤压和东西向拉伸所至。青藏高原阶段性不均匀抬升形成了宽窄相间的藕节状河道形态,宽阔河段河道为辫状河型,而窄深河段为深切的V型河谷、单一顺直河型,纵剖面上构成裂点。裂点河段地块相对上升较快,阻滞了水流和泥沙,上游河段大量卵石和泥沙在河谷里淤积深达800多米,形成了平整而宽阔的U型河谷。整个雅江宽谷段泥沙淤积量约0.9万亿m<sup>3</sup>。
[余国安, 王兆印, 刘乐, . 新构造运动影响下的雅鲁藏布江水系发育和河流地貌特征
. 水科学进展, 2012, 23(2): 163-169.]
https://doi.org/CNKI: 32.1309.P.20120224.2003.012Magsci [本文引用: 1]摘要
雅鲁藏布江(雅江)水系发育和河流地貌演变受新构造运动的强烈影响。通过野外调查,结合SRTM(航天飞机雷达地形测绘使命)数据分析和Google Earth三维地图功能,对雅江河网形态及河流地貌特征进行了分析,并采用EH4电磁成像系统测量了雅江及其支流宽谷河道淤沙深度。研究发现,雅江河网呈现格状水系特点,同时具有枝状河网的拓扑性质,这主要是由于新构造运动的影响,河网发育过程中受到南北向挤压和东西向拉伸所至。青藏高原阶段性不均匀抬升形成了宽窄相间的藕节状河道形态,宽阔河段河道为辫状河型,而窄深河段为深切的V型河谷、单一顺直河型,纵剖面上构成裂点。裂点河段地块相对上升较快,阻滞了水流和泥沙,上游河段大量卵石和泥沙在河谷里淤积深达800多米,形成了平整而宽阔的U型河谷。整个雅江宽谷段泥沙淤积量约0.9万亿m<sup>3</sup>。
[22]Li Yalin, Wang Chengshan, Wang Mou, et al.Morphological features of river valleys in the source of the Yangtze River, northern Tibet, and their response to Neotectonic Movement
. Geology in China, 2006, 33(2): 374-382.
https://doi.org/10.3969/j.issn.1000-3657.2006.02.016URL [本文引用: 1]摘要
对藏北长江源地区河谷地貌和新构造变形调查发现,该区具有平行式水系格局,河谷地貌以形态不同的窄谷和宽谷为特点,新近纪以来该区主要经历了早期挤压和晚期伸展构造演化过程,产生了褶皱-逆冲、走滑剪切、正断层和地堑构造3种构造变形样式.长江源区河谷地貌的形成演化明显受新构造运动的影响,新构造运动不仅控制了河谷地貌形态与水系格局,而且影响了河流阶地分布以及洪(冲)积扇的形态、结构.长江源地区主要水系至少自全新世以来是沿新构造运动产生的不同性质断裂构造溯源侵蚀发育而成.
[李亚林, 王成善, 王谋, . 藏北长江源地区河流地貌特征及其对新构造运动的响应
. 中国地质, 2006, 33(2): 374-382.]
https://doi.org/10.3969/j.issn.1000-3657.2006.02.016URL [本文引用: 1]摘要
对藏北长江源地区河谷地貌和新构造变形调查发现,该区具有平行式水系格局,河谷地貌以形态不同的窄谷和宽谷为特点,新近纪以来该区主要经历了早期挤压和晚期伸展构造演化过程,产生了褶皱-逆冲、走滑剪切、正断层和地堑构造3种构造变形样式.长江源区河谷地貌的形成演化明显受新构造运动的影响,新构造运动不仅控制了河谷地貌形态与水系格局,而且影响了河流阶地分布以及洪(冲)积扇的形态、结构.长江源地区主要水系至少自全新世以来是沿新构造运动产生的不同性质断裂构造溯源侵蚀发育而成.
[23]Shi C X, Shao W W.Knickpoints within the Suoshui watershed and the implication for the age of sandstone pillars in Zhangjiajie, China
. Geomorphology, 2014, 221(15): 261-273.
https://doi.org/10.1016/j.geomorph.2014.06.018URL [本文引用: 1]摘要
Using DEM and topographic and geological maps alongside field surveys, this study investigated the characteristics and retreat processes of the knickpoints along the mainstream and major tributaries of the Suoshui watershed. Seven disequilibrium transient knickpoints are found along the mainstream, and 0-6 are on the trunk of each of the major tributaries. The knickpoints are labeled from KP0 to KP7 from the lowest to the highest according to their spatial position. The average drop across each knickpoint is in the range of 9-19 m, and the cumulative fall from KP7 to KP0 is about 107 m. Using a brute force two-parameter search, the coefficient m in the stream power incision model for the Suoshui watershed is found to be 0.525, and the coefficient K is variable with an inverse relationship with channel steepness. Using the stream power incision model with these parameters, the time for the highest knickpoint (KP7) to retreat from the mouth of the Suoshui River to its present location is found to be ca. 0.454 Ma. Based on the relationship between the cumulative fall and migration time of knickpoints, the average downcutting rate of the Suoshui River is estimated to be 0.224 mm/a in the past 0.454 Ma. By comparing the downcutting rates with the height of typical sandstone pillars in the Suoshui watershed, the formation of these pillars might commence in the early Pleistocene. (C) 2014 Elsevier B.V. All rights reserved.
[24]Wang Guangqian, Liu Jiahong.Digital Models of Drainage Basins. Beijing: Science Press, 2006.URL [本文引用: 1]

[王光谦, 刘家宏. 数字流域模型. 北京: 科学出版社, 2006.]URL [本文引用: 1]
[25]Cai Qiangguo, Lu Zhaoxiong, Wang Guiping.Process-based soil erosion and sediment yield model in a small basin in the hilly loess region
. Acta Geographica Sinica, 1996, 51(2): 108-117.
https://doi.org/10.11821/xb199602003URL [本文引用: 1]摘要
在分析现存土壤侵蚀产沙模型基础上,依据大量小流域野外试验小区观测与模拟降雨试验资料,建立了一个适用于黄土丘陵沟壑区小流域预测侵蚀产沙量的侵蚀产沙过程模型。由于黄土丘陵沟壑区小流域的复杂地形和侵蚀产沙的垂直分带规律,土壤侵蚀产沙的空间变化要比现有模型复杂得多,因此,本模型由三个子模型组成:坡面子模型、沟坡子模型、沟道子模型,它可以计算小流域每场暴雨的径流量与侵蚀产沙量。本文较为详细地描述了模型中计算所用的方程和子模型运算框图。
[蔡强国, 陆兆熊, 王贵平. 黄土丘陵沟壑区典型小流域侵蚀产沙过程模型
. 地理学报, 1996, 51(2): 108-117.]
https://doi.org/10.11821/xb199602003URL [本文引用: 1]摘要
在分析现存土壤侵蚀产沙模型基础上,依据大量小流域野外试验小区观测与模拟降雨试验资料,建立了一个适用于黄土丘陵沟壑区小流域预测侵蚀产沙量的侵蚀产沙过程模型。由于黄土丘陵沟壑区小流域的复杂地形和侵蚀产沙的垂直分带规律,土壤侵蚀产沙的空间变化要比现有模型复杂得多,因此,本模型由三个子模型组成:坡面子模型、沟坡子模型、沟道子模型,它可以计算小流域每场暴雨的径流量与侵蚀产沙量。本文较为详细地描述了模型中计算所用的方程和子模型运算框图。
[26]Liu Jigen, Cai Qiangguo, Liu Qianjin, et al.Study on the regularity of sediment yield processes in catchments under different scales
. Journal of Sediment Research, 2005(4): 7-13.
URLMagsci [本文引用: 1]摘要
寻求不同尺度下侵蚀产沙过程的变化规律和普遍规律,是进行尺度转换的基础.本文以岔巴沟流域及其团山沟径流场实测水文数据为基础,探讨了不同尺度下流域径流过程、侵蚀产沙过程、水沙关系随尺度的变化规律.通过对峁坡、全坡面、毛沟、支沟、干沟的径流和泥沙分析表明,全坡面将流域径流过程、侵蚀产沙过程、水沙关系有机的区分开为坡面和沟道两种类型的变化过程,而全坡面又对毛沟的径流和泥沙起主导作用.
[刘纪根, 蔡强国, 刘前进, . 流域侵蚀产沙过程随尺度变化规律研究
. 泥沙研究, 2005(4): 7-13.]
URLMagsci [本文引用: 1]摘要
寻求不同尺度下侵蚀产沙过程的变化规律和普遍规律,是进行尺度转换的基础.本文以岔巴沟流域及其团山沟径流场实测水文数据为基础,探讨了不同尺度下流域径流过程、侵蚀产沙过程、水沙关系随尺度的变化规律.通过对峁坡、全坡面、毛沟、支沟、干沟的径流和泥沙分析表明,全坡面将流域径流过程、侵蚀产沙过程、水沙关系有机的区分开为坡面和沟道两种类型的变化过程,而全坡面又对毛沟的径流和泥沙起主导作用.
[27]Fang Haiyan, Cai Qiangguo, Chen Hao, et al.Scale effect on sediment yield from sloping surface to basins in hilly loess region on the Loess Plateau in China
. Environmental Geology, 2007, 52: 753-760.
https://doi.org/10.1007/s00254-006-0513-9URLMagsci [本文引用: 1]摘要
<a name="Abs1"></a>Based on data from two runoff plots and ten stations in hilly loess region Dalihe drainage basin ranging in area from 0.0006 to 3983&nbsp;km<sup>2</sup> on the Loess Plateau, the relationship between mean annual specific sediment yield (<i>Y</i> <sub>s</sub>) and drainage area (<i>A</i>) is studied, which is different from those for many other drainage areas of the world, neither at the scale of whole basin nor at local scale on the Loess Plateau. With increasing drainage area, the mean annual specific sediment yield experiences two peak values: the first peak value appears at 0.00408&nbsp;km<sup>2</sup> in area corresponding to the whole slope surface, and the second peak value appears at 96.1&nbsp;km<sup>2</sup> in area. The non-linear variation in the <i>Y</i> <sub>s</sub>&#8211;<i>A</i> can be explained as follows: the first peak value can be explained by the abrupt increase in slope gradient and flow shear stress resulting in highly increased sediment concentration and specific sediment yield. And the second peak value can be explained by the combined influence of flow shear stress and drainage density, represented by dimensionless variable &#937;.
[28]Fang Haiyan, Cai Qiangguo, Chen Hao.Temporal changes in suspended sediment concentration in a gullied loess basin: the lower Chabagou Creek on the Loess Plateau in China
. Earth Surface Processes and Landforms, 2008, 33: 1977-1992.
https://doi.org/10.1002/esp.1649URL [本文引用: 1]摘要
Suspended sediment dynamics are still imperfectly understood, especially in the loess hilly region on the Loess Plateau, with strong temporal variability, where few studies heretofore have been conducted. Using a dataset up to eight years long in the Lower Chabagou Creek, the variability in suspended sediment load at different temporal scales (within-flood variability, monthly-seasonal and annual) is analyzed in this paper. The results show that, on the within-flood scale, most of the sediment peaks lag behind peak discharges, implying that slope zones are the main sediment source area; independent of the occurring sequences of the peaks of sediment and discharge, all the events could present an anti-clock wise hysteresis loop resulting from the abundant material and the influence of hyperconcentrated flows on suspended sediment concentration. At monthly and seasonal scales, there is a 'store-release' process, i.e. sediment is prepared in winter, spring and late autumn, and exported in summer and early autumn. At the annual scale, the high variability in concentration and sediment yield are highly correlated with water yield, resulting from the number and magnitude of floods recorded yearly, and almost all the suspended load is transported during these events. Copyright (c) 2008 John Wiley & Sons, Ltd.
[29]Lu Jinfa, Huang Xiuhua.Effect of basin morphology on sediment yield in the middle reaches of the Yellow River
. Geographical Research, 2002, 21(2): 171-178.
Magsci [本文引用: 1]摘要
<p>在黄河中游地区 ,选择了 5 0多个面积约 5 0 0~ 2 5 0 0平方公里的水文测站流域 ,分别代表 6种不同自然地理类型 ,在流域沟壑密度、沟间地坡度小于 15&deg;面积百分比等地貌形态指标量计的基础上 ,进行了流域产沙量与地貌形态指标相关分析。结果表明 ,对于不同类型流域 ,流域产沙量随流域地貌的变化遵循不同的响应规律 ,而且视流域其它下垫面环境条件的均一程度 ,其相关程度和响应速率各不相同。受地面物质、植被、地貌发育阶段等流域其它下垫面环境条件的制约 ,除沟壑密度外 ,流域产沙量与流域地貌形态的关系都没有人们以前所预期的好。</p>
[卢金发, 黄秀华. 黄河中游流域地貌形态对流域产沙量的影响
. 地理研究, 2002, 21(2): 171-178.]
Magsci [本文引用: 1]摘要
<p>在黄河中游地区 ,选择了 5 0多个面积约 5 0 0~ 2 5 0 0平方公里的水文测站流域 ,分别代表 6种不同自然地理类型 ,在流域沟壑密度、沟间地坡度小于 15&deg;面积百分比等地貌形态指标量计的基础上 ,进行了流域产沙量与地貌形态指标相关分析。结果表明 ,对于不同类型流域 ,流域产沙量随流域地貌的变化遵循不同的响应规律 ,而且视流域其它下垫面环境条件的均一程度 ,其相关程度和响应速率各不相同。受地面物质、植被、地貌发育阶段等流域其它下垫面环境条件的制约 ,除沟壑密度外 ,流域产沙量与流域地貌形态的关系都没有人们以前所预期的好。</p>
[30]Yan Yunxia, Xu Jiongxin.A study of scale effect on specific sediment yield in the Loess Plateau, China
. Science in China Series D: Earth Sciences, 2006, 36(8): 767-776.
https://doi.org/10.3321/j.issn:1006-9267.2006.08.009URL [本文引用: 1]摘要
以黄河流域水文站的观测数据为基础,对黄土高原地区产沙模数的尺度效应进行了分区研究.研究表明,不同分区的黄土、风沙、基岩的空间分布与组合关系不同、地形(坡度)不同,其产沙模数随流域面积变化的趋势也不相同,可以分为单调减小、单调增大、先增大而后减小、先减小而后增大等类型.在对数据进行双对数转换后,对上述尺度效应关系进行了线性和二次函数的拟合,并分别针对这两种函数形式给出了校正方程.依据所建立的校正方程,将所有分区内各站点的产沙模数进行了1000km2标准面积的校正以消除尺度的影响.在此基础上使用Kriging插值法制作了消除尺度影响后的产沙模数图,并将其与未进行尺度校正的产沙模数图进行了分析比较.结果表明,经尺度校正后,重点侵蚀区域的位置大致相同,但面积显著增大.这主要是因为,位于重点侵蚀区河流下游的站点经校正后,其产沙模数有所增大.
[闫云霞, 许炯心. 黄土高原地区侵蚀产沙的尺度效应研究初探
. 中国科学D辑: 地球科学, 2006, 36(8): 767-776.]
https://doi.org/10.3321/j.issn:1006-9267.2006.08.009URL [本文引用: 1]摘要
以黄河流域水文站的观测数据为基础,对黄土高原地区产沙模数的尺度效应进行了分区研究.研究表明,不同分区的黄土、风沙、基岩的空间分布与组合关系不同、地形(坡度)不同,其产沙模数随流域面积变化的趋势也不相同,可以分为单调减小、单调增大、先增大而后减小、先减小而后增大等类型.在对数据进行双对数转换后,对上述尺度效应关系进行了线性和二次函数的拟合,并分别针对这两种函数形式给出了校正方程.依据所建立的校正方程,将所有分区内各站点的产沙模数进行了1000km2标准面积的校正以消除尺度的影响.在此基础上使用Kriging插值法制作了消除尺度影响后的产沙模数图,并将其与未进行尺度校正的产沙模数图进行了分析比较.结果表明,经尺度校正后,重点侵蚀区域的位置大致相同,但面积显著增大.这主要是因为,位于重点侵蚀区河流下游的站点经校正后,其产沙模数有所增大.
[31]Zheng M G, Cai Q G, Cheng Q J.Modeling the runoff-sediment yield relationship using a proportional function in hilly areas of the Loess Plateau, North China
. Geomorphology, 2008, 93: 288-301.
[本文引用: 1]
[32]Shi Changxing.Scaling effects on sediment yield in the upper Yangtze River
. Geographical Research, 2008, 27(4): 800-810.
Magsci [本文引用: 1]摘要
<p>利用长江上游DEM、降雨、土地利用、土壤类型数据库,计算出通用土壤流失方程中代表影响侵蚀产沙的各因子,建立这些因子以及流域面积与长江上游268个水文站以上流域输沙模数回归关系,探讨上游侵蚀输沙的尺度效应。结果显示长江上游输沙模数与流域面积之间呈负幂函数单元回归关系,而且这一关系主要产生于降雨侵蚀力因子和土壤可蚀性因子随流域面积的变化。长江上游输沙模数随流域面积增大而降低主要发生在大约1&times;10<sup>4</sup>~1.58&times;10<sup>5</sup>km<sup>2</sup>之间。在考虑了影响侵蚀产沙因子对输沙模数的作用后,输沙模数与流域面积之间呈正幂函数相关,反映出上游输沙近源沉积的特征。分析还发现长江上游各主要支流输沙模数变化与流域尺度大小的关系和原因有明显不同。</p>
[师长兴. 长江上游输沙尺度效应研究
. 地理研究, 2008, 27(4): 800-810.]
Magsci [本文引用: 1]摘要
<p>利用长江上游DEM、降雨、土地利用、土壤类型数据库,计算出通用土壤流失方程中代表影响侵蚀产沙的各因子,建立这些因子以及流域面积与长江上游268个水文站以上流域输沙模数回归关系,探讨上游侵蚀输沙的尺度效应。结果显示长江上游输沙模数与流域面积之间呈负幂函数单元回归关系,而且这一关系主要产生于降雨侵蚀力因子和土壤可蚀性因子随流域面积的变化。长江上游输沙模数随流域面积增大而降低主要发生在大约1&times;10<sup>4</sup>~1.58&times;10<sup>5</sup>km<sup>2</sup>之间。在考虑了影响侵蚀产沙因子对输沙模数的作用后,输沙模数与流域面积之间呈正幂函数相关,反映出上游输沙近源沉积的特征。分析还发现长江上游各主要支流输沙模数变化与流域尺度大小的关系和原因有明显不同。</p>
[33]Wang Zhaoyin, Wang Guangqian, Li Changzhi, et al.A preliminary study on vegetation-erosion dynamics and its applications
. Science in China Series D: Earth Sciences, 2003, 33(10): 1013-1023.
https://doi.org/10.3321/j.issn:1006-9267.2003.10.013URL [本文引用: 1]摘要
植被侵蚀动力学是一个新的边缘学科,研究流域植被与侵蚀在人类活动影响下的演变规律.讨论了作用于植被的各种生态应力,给出了定量表达式并且统一在植被一侵蚀动力学方程组中.推导得出了动力学方程组的理论解并且用于模拟黄土高原安家沟流域和云南小江流域的植被侵蚀演变过程,结果表明动力学方程组精确地模拟了实际演变过程.利用动力学方程组和特征参数作出了植被侵蚀状态图,由此可以预测在停止人类干预后的植被发展趋势,说明了有效治理所需的治理强度和控制侵蚀对植被发育的重要性.植被侵蚀状态图还说明在雨量较丰、气温较高的云南高原小江流域,减少侵蚀是改善植被的重要措施,植被改善后比较稳定.而在比较干旱、水土流失严重的黄土高原上,增加植被能够明显地减少侵蚀,但控制侵蚀对于促进植被发育没有太大的作用.即使植被已经大大改善,仍然不稳定,还需要不断地护理才能维持植被的良性发育。
[王兆印, 王光谦, 李昌志, . 植被—侵蚀动力学的初步探索和应用
. 中国科学D辑: 地球科学, 2003, 33(10): 1013-1023.]
https://doi.org/10.3321/j.issn:1006-9267.2003.10.013URL [本文引用: 1]摘要
植被侵蚀动力学是一个新的边缘学科,研究流域植被与侵蚀在人类活动影响下的演变规律.讨论了作用于植被的各种生态应力,给出了定量表达式并且统一在植被一侵蚀动力学方程组中.推导得出了动力学方程组的理论解并且用于模拟黄土高原安家沟流域和云南小江流域的植被侵蚀演变过程,结果表明动力学方程组精确地模拟了实际演变过程.利用动力学方程组和特征参数作出了植被侵蚀状态图,由此可以预测在停止人类干预后的植被发展趋势,说明了有效治理所需的治理强度和控制侵蚀对植被发育的重要性.植被侵蚀状态图还说明在雨量较丰、气温较高的云南高原小江流域,减少侵蚀是改善植被的重要措施,植被改善后比较稳定.而在比较干旱、水土流失严重的黄土高原上,增加植被能够明显地减少侵蚀,但控制侵蚀对于促进植被发育没有太大的作用.即使植被已经大大改善,仍然不稳定,还需要不断地护理才能维持植被的良性发育。
[34]Xu J X.Precipitation-vegetation coupling and its influence on erosion on the Loess Plateau, China
. Catena, 2005, 64: 103-116.
https://doi.org/10.1016/j.catena.2005.07.004URLMagsci [本文引用: 1]摘要
<h2 class="secHeading" id="section_abstract">Abstract</h2><p id="">The relationships between precipitation, vegetation and erosion are important and are unsolved issues in the field of earth surface processes. Based on data from the Loess Plateau of China, some non-linear relationships between forest cover (<em>C</em><sub>f</sub>), mean annual rainfall erosivity (<em>R</em><sub>e</sub>) and annual precipitation (<em>P</em><sub>m</sub>) have been found. A threshold has been identified at <em>P</em><sub>m</sub>&#xA0;=&#xA0;450 mm, that is, when <em>P</em><sub>m</sub> is &lt;&#xA0;450 mm, <em>C</em><sub>f</sub> is low and basically does not vary with <em>P</em><sub>m</sub>; when <em>P</em><sub>m</sub> exceeds 450 mm, <em>C</em><sub>f</sub> increases rapidly. Furthermore, two thresholds are identified in the relationship between rainfall erosivity and annual precipitation. When <em>P</em><sub>m</sub> is &lt;&#xA0;300 mm, <em>R</em><sub>e</sub> is low and basically does not vary with <em>P</em><sub>m.</sub> When <em>P</em><sub>m</sub> exceeds 300 mm, <em>R</em><sub>e</sub> increases rapidly; when <em>P</em><sub>m</sub> becomes &gt;&#xA0;530 mm, the rate at which <em>R</em><sub>e</sub> increases with <em>P</em><sub>m</sub> becomes higher. Based on these relationships, the non-linear relationship between erosion intensity and annual precipitation (i.e., the erosion intensity increases with annual precipitation to a peak and then declines) is explained. The implication of these thresholds for erosion control on the Loess Plateau is discussed.</p>
[35]Chen Hao, Zhou Jinxing, Cai Qiangguo, et al.The impact of vegetation restoration on erosion-induced sediment yield in the middle Yellow River and management prospect
. Science in China Series D: Earth Sciences, 2005, 35(5): 452-463.
[本文引用: 1]

[陈浩, 梁广林, 周金星, . 黄河中游植被恢复对流域侵蚀产沙的影响与治理前景
. 中国科学D辑: 地球科学, 2005, 35(5): 452-463.]
[本文引用: 1]
[36]Ni Jinren, Han Peng, Zhang Jian.Characteristics of evolution of rills on loess slopes based on concept of self-organization
. Journal of Hydraulic Engineering, 2002, 33(1): 6-15.
[本文引用: 1]

[倪晋仁, 韩鹏, 张剑. 基于自组织理论的黄土坡面细沟发育特征分析
. 水利学报, 2002, 33(1): 6-15.]
[本文引用: 1]
[37]Hu Chunhong, Guo Qingchao.Modeling sediment transport in the lower Yellow River and dynamic equilibrium threshold value
. Science in China Series E: Technological Sciences, 2004, 34(Suppl.1): 133-143.
[本文引用: 1]

[胡春宏, 郭庆超. 黄河下游河道泥沙数学模型及动力平衡临界阈值探讨
. 中国科学E辑: 技术科学, 2004, 34(Suppl.1): 133-143.]
[本文引用: 1]
[38]Wu Baosheng, You Tao.Theoretical model for delayed response of reservoir sedimentation
. Journal of Hydraulic Engineering, 2008, 39(5): 627-632.
https://doi.org/10.3321/j.issn:0559-9350.2008.05.018URL [本文引用: 1]摘要
河床演变中普遍存在着滞后响应现象,而以往的水库泥沙研究对滞后响应现象很少考虑。本文在作者近期关于水库泥沙淤积滞后现象研究的基础上,从河床演变学的自动调整原理出发,建立了水库泥沙淤积滞后响应的理论模型。并以三门峡水库泥沙淤积为例,利用提出的理论模型分析了库区累计淤积量对流量加权平均坝前水位的响应、潼关高程对年入库水量的响应及水库末端比降对年平均坝前水位的响应,结果表明所建理论模型能够描述泥沙淤积的特征,为水库泥沙淤积的研究提供了一种新的方法。
[吴保生, 游涛. 水库泥沙淤积滞后响应的理论模型
. 水利学报, 2008, 39(5): 627-632.]
https://doi.org/10.3321/j.issn:0559-9350.2008.05.018URL [本文引用: 1]摘要
河床演变中普遍存在着滞后响应现象,而以往的水库泥沙研究对滞后响应现象很少考虑。本文在作者近期关于水库泥沙淤积滞后现象研究的基础上,从河床演变学的自动调整原理出发,建立了水库泥沙淤积滞后响应的理论模型。并以三门峡水库泥沙淤积为例,利用提出的理论模型分析了库区累计淤积量对流量加权平均坝前水位的响应、潼关高程对年入库水量的响应及水库末端比降对年平均坝前水位的响应,结果表明所建理论模型能够描述泥沙淤积的特征,为水库泥沙淤积的研究提供了一种新的方法。
[39]Xu Jiongxin, Hu Chunhong, Chen Jianguo.Effect of suspended sediment grain size on channel sedimentation in the lower Yellow River and some implications
. Science in China Series E: Technological Sciences, 2009, 39(2): 310-317.
https://doi.org/10.1016/S1874-8651(10)60084-1URL [本文引用: 1]摘要
以不同粒径组的来沙量和淤积量的资料为基础,建立了三门峡-利津河段的年冲淤量与进入下游河道的年沙量的关系,从中得到了下游河道泥沙从存贮到释放的临界值.这一临界值随泥沙粒径组的变粗而减小.三门峡-利津河段的年冲淤量与进入下游河道的年沙量的相关系数值,随泥沙粒径组的变粗而增大,即来沙越粗,来沙量与河道淤积的关系越密切.单位输入沙量的变化所导致的淤积量增加量,随着粒径的变粗而增大.研究表明,在已经对大于0.05mm粗泥沙来源区进行治理并取得成效的基础上,集中治理大于0.10mm粗泥沙的产出区,具有重要意义.
[许炯心, 胡春宏, 陈建国. 不同粒径组泥沙对黄河下游沉积的影响及其在黄河治理中的意义
. 中国科学E辑: 技术科学, 2009, 39(2): 310-317.]
https://doi.org/10.1016/S1874-8651(10)60084-1URL [本文引用: 1]摘要
以不同粒径组的来沙量和淤积量的资料为基础,建立了三门峡-利津河段的年冲淤量与进入下游河道的年沙量的关系,从中得到了下游河道泥沙从存贮到释放的临界值.这一临界值随泥沙粒径组的变粗而减小.三门峡-利津河段的年冲淤量与进入下游河道的年沙量的相关系数值,随泥沙粒径组的变粗而增大,即来沙越粗,来沙量与河道淤积的关系越密切.单位输入沙量的变化所导致的淤积量增加量,随着粒径的变粗而增大.研究表明,在已经对大于0.05mm粗泥沙来源区进行治理并取得成效的基础上,集中治理大于0.10mm粗泥沙的产出区,具有重要意义.
[40]Xu Jiongxin.A study of the scour-fill threshold based on Lane's equilibrium relation: The lower Yellow River
. Geomorphology, 2015, 250: 140-146.
https://doi.org/10.1016/j.geomorph.2015.08.009URL [本文引用: 1]摘要
The scour-fill threshold in river channels is an expression of scour-fill equilibrium, which may be understood as the balance between the river's sediment carrying capability and the sediment load imposed by the drainage basin. In the present study, the above capability-load relation is quantified using Lane's relation, γQJ-QD, wherein Q is water discharge, J is channel slope, Qis sediment transport rate, Dis median size of bed material, and γ is the specific weight of water. On this basis, we have established scour-fill thresholds for the lower Yellow River based on data from 141 flood events. The results show that the QD-γQJ relation may well distinguish between the scour and fill flood events. The following equation has been established: SDR= 0.00099(γQJ)(QD), wherein SDRis channel sediment delivery ratio. From the equation, the scour-fill threshold is established as: QD= 0.00001(γQJ). Starting from this formula, four possible options are proposed for sediment management of the lower Yellow River.
[41]Shi C X.Causes for continuous siltation of the lower Yellow River
. Geomorphology, 2005, 68: 213-223.
https://doi.org/10.1016/j.geomorph.2004.11.015URL [本文引用: 1]摘要
Previous studies indicate that aggradation of a river channel is caused by upriver and/or downriver controls, but the evaluation of their relative importance is often difficult. A method is proposed to isolate the effect of the downriver control based on the slopes of the existing river profile, those of the graded profile estimated from the discharge-sediment relationship and slope reduction due to local base-level rise. The method was applied to the rapidly aggrading lower Yellow River. The downriver control in this case refers to the local base-level rise associated with deltaic extension during the period under discussion. The result shows that the main portion of siltation along the river is not caused by downriver control but by the slope difference between the existing and the graded profiles over a period within the last 700 years, assuming conditions of discharge and sediment load during the period from 1962 to 1985 are reflective of the long term. The marked slope difference between the existing and the graded profiles of the river is a result of changes in the river environment in the past several thousand years including the increase of sediment load, local base-level rise associated with river lengthening by deltaic growth, and relative sea-level rise due to tectonic subsidence of the coastal alluvial plain.
[42]Huang H Q, Chang, H H.Scale independent linear behavior of alluvial channel flow
. Journal of Hydraulic Engineering, 2006, 132(7): 721-730.
[本文引用: 1]
[43]Huang H Q, Chang H H, Nanson G C.Minimum energy as a general form of critical flow and maximum flow efficiency and for explaining variations in river channel pattern
. Water Resources Research, 2004, 40, W04502. doi: 10.1029/2003WR002539.
URL摘要
[1] Although the B langer-B ss theorem of critical flow has been widely applied in open channel hydraulics, it was derived from the laws governing ideal frictionless flow. This study explores a more general expression of this theorem and examines its applicability to flow with friction and sediment transport. It demonstrates that the theorem can be more generally presented as the principle of minimum energy (PME), with maximum efficiency of energy use and minimum friction or minimum energy dissipation as its equivalents. Critical flow depth under frictionless conditions, the best hydraulic section where friction is introduced, and the most efficient alluvial channel geometry where both friction and sediment transport apply are all shown to be the products of PME. Because PME in liquids characterizes the stationary state of motion in solid materials, flow tends to rapidly expend excess energy when more than minimally demanded energy is available. This leads to the formation of relatively stable but dynamic energy-consuming meandering and braided channel planforms and explains the existence of various extremal hypotheses.
[44]Huang H Q, Nanson G C.A stability criterion inherent in laws governing alluvial channel flow
. Earth Surface Processes and Landforms, 2002, 27(8): 929-944.
https://doi.org/10.1002/esp.364URL摘要
Abstract The stability criterion of maximum flow efficiency (MFE) has previously been found inherent in typical alluvial channel flow relationships, and this study investigates the general nature of this criterion using a wider range of flow resistance and bedload transport formulae. For straight alluvial channels, in which the effect of sediment sorting is insignificant, our detailed mathematical analysis demonstrates that a flow efficiency factor ε occurs generally as the ratio of sediment (bedload) discharge Q s to stream power Ω (γ QS ) in the form of . When ε is maximized (i.e. Q s is maximized or Ω is minimized), maximally efficient straight channel geometries derived from most flow resistance and bedload transport formulae are found compatible with observed bankfull hydraulic geometry relations. This study provides support for the use of the criteria of MFE, maximum sediment transporting capacity and minimum stream power for understanding the operation of alluvial rivers, and also addresses limitations to the direct application of its findings. Copyright 08 2002 John Wiley & Sons, Ltd.
[45]Huang H Q, Nanson, G C, Fagan S D. Hydraulic geometry of straight alluvial channels and the variational principle of least action
. Journal of Hydraulic Research, 2002, 40(2): 153-160.
https://doi.org/10.1080/00221680209499858URL [本文引用: 1]摘要
Natural rivers exhibit regular hydraulic geometry relationships for which no widely accepted explanation has been given. This paper applies the physical principle of least action to the determination of stable alluvial-channel form. For steady, uniform alluvial-channel flow, both theoretical inferences and a case study show that least action occurs when the criteria of minimum potential energy and MFE (Maximum Flow Efficiency, defined here as the maximum sediment transporting capacity per unit available stream power) are satisfied. The consistency between bankfull hydraulic geometry relationships of natural channels and those of maximally efficient or 'least action' channels identified in this study demonstrates that alluvial channels commonly adjust to a maximally efficient section. Support for the use of the extremal hypotheses of maximum sediment transporting capacity and minimum stream power is provided by illustrating that they are essentially expressions of, and hence subsumed by, the more general principle of MFE.
[46]Zhong Deyu, Zhang Hongwu, Zhang Junhua, et al.Two dimensional numerical model of flow and sediment transport for wandering rivers
. Journal of Hydraulic Engineering, 2009, 40(9): 1040-1047.
URL [本文引用: 1]摘要
为使数学模型能模拟游荡性河流因水流弯曲、分汊等导致的环流输沙作用,本文首先在悬移质泥沙对流扩散方程中增加了横向输沙项,然后引入适合游荡型河流的塌岸模式及局部动网格技术和网格融合技术,解决了河岸变形模拟和河道整治工程导致网格再生、床沙级配变化模拟等关键性难题,开发出可模拟游荡性河流河床演变且可反映河道整治工程作用的平面二维水沙数学模型。最后,以黄河下游柳园口—夹河滩河段为例,应用本文模型对游荡型河流河势变化进行了数值模拟,结果表明本模型能够真实地模拟出游荡型河流独特的河床演变过程。
[钟德钰, 张红武, 张俊华, . 游荡型河流的平面二维水沙数学模型
. 水利学报, 2009, 40(9): 1040-1047.]
URL [本文引用: 1]摘要
为使数学模型能模拟游荡性河流因水流弯曲、分汊等导致的环流输沙作用,本文首先在悬移质泥沙对流扩散方程中增加了横向输沙项,然后引入适合游荡型河流的塌岸模式及局部动网格技术和网格融合技术,解决了河岸变形模拟和河道整治工程导致网格再生、床沙级配变化模拟等关键性难题,开发出可模拟游荡性河流河床演变且可反映河道整治工程作用的平面二维水沙数学模型。最后,以黄河下游柳园口—夹河滩河段为例,应用本文模型对游荡型河流河势变化进行了数值模拟,结果表明本模型能够真实地模拟出游荡型河流独特的河床演变过程。
[47]Chen D, Duan J G.Case study: Two-dimensional model simulation of channel migration processes in West Jordan River, Utah
. Journal of Hydraulic Engineering, 2008, 134(3): 315-327.
https://doi.org/10.1061/(ASCE)0733-9429(2008)134:3(315)URL [本文引用: 1]摘要
The paper presents the application of a two-dimensional depth-averaged numerical model to simulate the lateral migration processes of a meandering reach in the West Jordan River in the state of Utah. A new bank erosion model was developed and then integrated with a depth-averaged two-dimensional hydrodynamic model. The rate of bank erosion is determined by bed degradation, lateral erosion, and bank failure. Because bank material in the West Jordan River is stratified with layers of cohesive and noncohesive materials, a specific bank erosion model was developed to consider stratified layers in the bank surface. This bank erosion model distinguishes itself from other models by relating bank erosion rate with not only flow but also sediment transport near the bank. Additionally, bank height, slope, and thickness of two layers in the bank surface were considered when calculating the rate of bank erosion. The developed model was then applied to simulate the processes of meandering migration in the study reach from 1981 to 1992. Historical real-time hydrographic data, as well as field survey data of channel geometry and bed and bank materials, were used as the input data. Simulated cross-sectional geometries after this 12-year period agreed with field measurements, and the R虏 value for predicting thalweg elevation and bank shift are 0.881 and 0.706, respectively.
[48]Chen D.Evaluating secondary flows in the evolution of sine-generated meanders
. Geomorphology, 2012, 163: 37-44.
https://doi.org/10.1016/j.geomorph.2012.04.010URLMagsci [本文引用: 1]摘要
The development of meanders has been the focus of research for decades because the shifting of bank lines may potentially cause serious problems in river engineering. This study assesses the roles of secondary flows in meander evolution by testing two model parameters, A and As, which represent the effects of momentum redistribution exerted by the topography-driven and curvature-driven secondary currents, respectively. The meander-evolution model couples an analytical solution of flow field in a sine-generated channel with the Bank Erosion and Retreat Model (BERM). The contributions of this study lie in two areas. First, the authors isolated and quantified the roles of curvature-driven and topography-driven secondary flows in meander evolution. Second, the shifting processes of primary flow by secondary flows were investigated in detail by evaluating various variations of the dimensionless scour factor A. (C) 2012 Elsevier B.V. All rights reserved.
[49]Zhang Guogang, Hu Chunhong, Chen Jianguo.Variation of channel cross-section morphological parameters and trend of channel shrinkage in Lower Yellow River
. Journal of Hydraulic Engineering, 2009, 40(10): 1227-1239.
URL [本文引用: 1]摘要
采用时间序列分析法对黄河下游河道断面形态参数变化趋势及其变异点进行了分析。结果表明从20世纪50年代以来,特别是90年代以来黄河下游花园口站、高村站、艾山站和利津站断面形态参数发生了趋势性变化,主河槽变化的最显著特征就是断面平滩流量下降,相应的平滩面积、平滩河宽、平均水深、最大水深均出现不同程度的减小,平滩宽深比增大。变异点分析表明黄河下游河道主河槽总体上在1970—1975年开始萎缩,1990年以后进入严重萎缩期。
[张国罡, 胡春宏, 陈建国. 黄河下游河道断面形态参数变化与主河槽萎缩趋势分析
. 水利学报, 2009, 40(10): 1227-1239.]
URL [本文引用: 1]摘要
采用时间序列分析法对黄河下游河道断面形态参数变化趋势及其变异点进行了分析。结果表明从20世纪50年代以来,特别是90年代以来黄河下游花园口站、高村站、艾山站和利津站断面形态参数发生了趋势性变化,主河槽变化的最显著特征就是断面平滩流量下降,相应的平滩面积、平滩河宽、平均水深、最大水深均出现不同程度的减小,平滩宽深比增大。变异点分析表明黄河下游河道主河槽总体上在1970—1975年开始萎缩,1990年以后进入严重萎缩期。
[50]Hu Chunhong, Zhang Zhihao.Research on separated discharge characteristics of floodplain and main channel of the Lower Yellow River compound channel
. Journal of Hydraulic Engineering, 2013, 44(1): 1-9.
URL [本文引用: 1]摘要
采用实测资料分析和理论探讨相结合的方法,研究了黄河下游复式河 道滩槽分流特征及其主要影响因素.研究结果表明:1986年后,河道萎缩,相同洪水流量下,主槽分流比有所减小,滩地分流比有所增大;1999年后,小浪 底水库蓄水拦沙运用,下游河道持续冲刷,主槽过流能力有所恢复,主槽分流比必然有所增大.运用回归分析方法,建立了黄河下游复式河道滩槽分流比与滩槽过水 宽度比、过水深度比、过水面积比、流速比、糙率比和主槽宽深比的单因素响应关系和多因素综合关系,在此基础上提出,定量方面,可运用多因素综合关系式依据 未来滩槽6项单因素大小对黄河下游复式河道滩槽分流比进行预测;定性方面,在黄河下游滩槽治理过程中,应注意维持主槽一定的平滩流量和较为窄深的断面形 态;注意给滩地留出一定的行洪宽度,在必要的行洪宽度内,尽量减少人类活动对滩地的影响,保持滩地畅通的过水通道,保证滩地相应的过洪能力,减轻河道行洪 压力,从而达到确保全断面行洪安全的目的.
[胡春宏, 张治昊. 黄河下游复式河道滩槽分流特征研究
. 水利学报, 2013, 44(1): 1-9.]
URL [本文引用: 1]摘要
采用实测资料分析和理论探讨相结合的方法,研究了黄河下游复式河 道滩槽分流特征及其主要影响因素.研究结果表明:1986年后,河道萎缩,相同洪水流量下,主槽分流比有所减小,滩地分流比有所增大;1999年后,小浪 底水库蓄水拦沙运用,下游河道持续冲刷,主槽过流能力有所恢复,主槽分流比必然有所增大.运用回归分析方法,建立了黄河下游复式河道滩槽分流比与滩槽过水 宽度比、过水深度比、过水面积比、流速比、糙率比和主槽宽深比的单因素响应关系和多因素综合关系,在此基础上提出,定量方面,可运用多因素综合关系式依据 未来滩槽6项单因素大小对黄河下游复式河道滩槽分流比进行预测;定性方面,在黄河下游滩槽治理过程中,应注意维持主槽一定的平滩流量和较为窄深的断面形 态;注意给滩地留出一定的行洪宽度,在必要的行洪宽度内,尽量减少人类活动对滩地的影响,保持滩地畅通的过水通道,保证滩地相应的过洪能力,减轻河道行洪 压力,从而达到确保全断面行洪安全的目的.
[51]Zhang Ouyang, Xu Jiongxin, Zhang Hongwu.The response of the channel form adjustment at the wandering-braided reaches of the lower Yellow River to flood events
. Acta Geographica Sinica, 2002, 57(6): 649-654.
https://doi.org/10.3321/j.issn:0375-5444.2002.06.003URL [本文引用: 1]摘要
以黄河流域1950~1985年200余场洪水资料为基础,并增加了最近的实验资料,分析了黄河下游游荡河段不同含沙量洪水过程中河床形态的调整过程。结果表明,由洪水过程所导致的河床形态变化是相当剧烈的,且与含沙量密切相关,表现出非线性的变化规律。当含沙量较小时,随含沙量的增大,洪水后河床宽深比增大,当含沙量增大到一定程度后再增大时,宽深比随含沙量的增大而减小。这一结果为修正Schumm关于河床形态变化的定性预测关系提供了新的依据。
[张欧阳, 许炯心, 张红武. 黄河游荡河段河床形态调整对洪水过程的响应
. 地理学报, 2002, 57(6): 649-654.]
https://doi.org/10.3321/j.issn:0375-5444.2002.06.003URL [本文引用: 1]摘要
以黄河流域1950~1985年200余场洪水资料为基础,并增加了最近的实验资料,分析了黄河下游游荡河段不同含沙量洪水过程中河床形态的调整过程。结果表明,由洪水过程所导致的河床形态变化是相当剧烈的,且与含沙量密切相关,表现出非线性的变化规律。当含沙量较小时,随含沙量的增大,洪水后河床宽深比增大,当含沙量增大到一定程度后再增大时,宽深比随含沙量的增大而减小。这一结果为修正Schumm关于河床形态变化的定性预测关系提供了新的依据。
[52]Wang S J, Li L, Cheng W M.Variations of bank shift rates along the Yinchuan Plain Reach of the Yellow River and their influence factors
. Journal of Geographical Sciences, 2014, 24(4): 703-716.
https://doi.org/10.1007/s11442-014-1114-2Magsci [本文引用: 1]摘要
<p>It is important to examine the lateral shift rate variation of river banks in different periods. One of the challenges in this regard is how to obtain the shift rate of river banks, as gauging stations are deficient for the study of river reaches. The present study selected the Yinchuan Plain reach of the Yellow River with a length of 196 km as a case study, and searched each point of intersection of 153 cross-sections (interval between two adjacent cross-sections was 1.3 km) and river banks in 1975, 1990, 2010 and 2011, which were plotted according to remote sensing images in those years. Then the shift rates for the points of intersection during 1975-1990, 1990-2010 and 2010-2011 were calculated, as well as the average shift rates for different sections and different periods. The results show that the left bank of the river reach shifts mostly to the right, with the average shift rates being 36.5 m/a, 27.8 m/a and 61.5 m/a in the three periods, respectively. Contemporarily, the right bank shifts mostly to the right in the first period, while it shifts to the left in the second and third periods, with the average shift rates being 31.7 m/a, 23.1 m/a and 50.8 m/a in the three periods, respectively. The average shift rates for the left and right banks during the period 1975-2011 are 22.3 m/a and 14.8 m/a, respectively. The bank shift rates for sections A, B and C are different. The shift rate ratio of the left bank in the three sections is 1:7.6:4.6 for shift to the left and 1:1.7:3.8 for shift to the right, while that of the right bank is 1:1.8:1.2 for shift to the left and 1:5.6:17.7 for shift to the right during the period 1975-2011. Obviously, the average shift rate is the least in section A, while it is maximum in section B for shift to the left and in section C for shift to the right. The temporal variation of the shift rate is influenced by human activities, while the spatial variation is controlled by the local difference in bank materials.</p>
[53]Yan Ming, Wang Suiji, Yan Yunxia, et al.Planar changes of upper alluvial reaches of the Yellow River in recent thirty years
. Journal of Arid Land Resources and Environment, 2013, 27(3): 74-79.
URL [本文引用: 1]摘要
黄河上游冲积河段的加速淤积已经严重威胁到当地人民的生产生活。为黄河上游冲积河段减淤措施的制定、消除洪灾隐患,文中基于遥感影像和水文资料,结合地质地貌资料,将冲积河段划分为四段,并根据河道的平面特征,将它们归入不同的河型。对比了1978、1990、2002和2010年四期近三十年宁蒙河段河道的平面变化,发现河道总体上表现出萎缩趋势,但在不同河型上变化过程表现不同,具有一定的复杂性。交错复合型和近顺直型河道主流线长度变化较小,游荡型先减小后增大,弯曲型逐渐增大;从河道平均宽度来看,近顺直型和弯曲型河段都是先加宽后束窄,而游荡型的变化却与前两者相反,呈现出先变窄后加宽,仅交错复合型河段逐渐变窄;四个河段河心洲数量变化呈现出两种情形:略微增加和先增加后减少。这些变化与近几十年上游水库的拦水拦沙是息息相关的。
[颜明, 王随继, 闫云霞, . 近三十年黄河上游冲积河段的河道平面形态变化分析
. 干旱区资源与环境, 2013, 27(3): 74-79.]
URL [本文引用: 1]摘要
黄河上游冲积河段的加速淤积已经严重威胁到当地人民的生产生活。为黄河上游冲积河段减淤措施的制定、消除洪灾隐患,文中基于遥感影像和水文资料,结合地质地貌资料,将冲积河段划分为四段,并根据河道的平面特征,将它们归入不同的河型。对比了1978、1990、2002和2010年四期近三十年宁蒙河段河道的平面变化,发现河道总体上表现出萎缩趋势,但在不同河型上变化过程表现不同,具有一定的复杂性。交错复合型和近顺直型河道主流线长度变化较小,游荡型先减小后增大,弯曲型逐渐增大;从河道平均宽度来看,近顺直型和弯曲型河段都是先加宽后束窄,而游荡型的变化却与前两者相反,呈现出先变窄后加宽,仅交错复合型河段逐渐变窄;四个河段河心洲数量变化呈现出两种情形:略微增加和先增加后减少。这些变化与近几十年上游水库的拦水拦沙是息息相关的。
[54]Li Bingyuan, Ge Quansheng, Zheng Jingyun.Evolution of the Yellow River in the Houtao plain of Inner Mongolia in the past 2000 years
. Acta Geographica Sinica, 2003, 58(3): 239-246.
https://doi.org/10.3321/j.issn:0375-5444.2003.02.011URL [本文引用: 1]摘要
通过遥感影像、地貌沉积、历史文献与地图等相关资料分析集成研 究,将后套平原分为西部冲积扇平原,东部是泛滥冲积平原,并详细探讨了近2000年来本区黄河河道的演变.公元前2世纪时,后套西部平原南(上)冲积扇停 止发育,北(下)冲积扇河道发育,黄河主河道的位置与现代不同,它偏于泛滥平原北部的阴山山前东流;公元6世纪后套平原西部北冲积扇上黄河河道向东移,在 东部泛滥平原上黄河明显地分为南北两汊,而黄河主流仍位于河套平原北部山前;18世纪早期至末期,黄河主河道从河套平原的北部山前南移至平原南部;19世 纪中叶北河'淤塞,现代黄河形成.
[李炳元, 葛全胜, 郑景云. 近2000年来内蒙后套平原黄河河道演变
. 地理学报, 2003, 58(3): 239-246.]
https://doi.org/10.3321/j.issn:0375-5444.2003.02.011URL [本文引用: 1]摘要
通过遥感影像、地貌沉积、历史文献与地图等相关资料分析集成研 究,将后套平原分为西部冲积扇平原,东部是泛滥冲积平原,并详细探讨了近2000年来本区黄河河道的演变.公元前2世纪时,后套西部平原南(上)冲积扇停 止发育,北(下)冲积扇河道发育,黄河主河道的位置与现代不同,它偏于泛滥平原北部的阴山山前东流;公元6世纪后套平原西部北冲积扇上黄河河道向东移,在 东部泛滥平原上黄河明显地分为南北两汊,而黄河主流仍位于河套平原北部山前;18世纪早期至末期,黄河主河道从河套平原的北部山前南移至平原南部;19世 纪中叶北河'淤塞,现代黄河形成.
[55]Zheng Shan, Tan Guangming, Wu Baosheng, et al.Calculation method for water stage at Lijin in response to delta evolution
. Journal of Hydraulic Engineering, 2015, 46(3): 315-325.
https://doi.org/10.13243/j.cnki.slxb.2015.03.008URL [本文引用: 1]摘要
本文分析了黄河口的演变特征及 其对利津3 000 m3/s同流量水位的影响。黄河口每次改道后尾闾河道的河长突然缩短,比降陡增,之后河长以先快后慢的速率增长,尾闾河道比降则呈指数衰减,经过约5~6 年调整至平衡比降,其变化过程反映了典型的河床演变滞后响应特性。基于黄河口河道的演变特征,提出了河口河道水位和纵比降变化的概化模式,并采用滞后响应 模型建立了河口河道同流量水位的计算方法,较好地计算了1954—2012年间黄河下游利津3 000 m3/s同流量水位的变化过程。该计算方法不仅考虑了河床演变的滞后响应特性,而且反映了来水来沙和河道淤长与蚀退对利津同流量水位的共同影响,能够连续 地模拟河口淤积延伸及改道过程中河口河道特征水位的长期变化过程。研究成果可为分析黄河口淤积延伸与下游河道相对侵蚀基准面的变化关系提供参考。
[郑珊, 谈广鸣, 吴保生, . 利津水位对河口演变响应的计算方法
. 水利学报, 2015, 46(3): 315-325.]
https://doi.org/10.13243/j.cnki.slxb.2015.03.008URL [本文引用: 1]摘要
本文分析了黄河口的演变特征及 其对利津3 000 m3/s同流量水位的影响。黄河口每次改道后尾闾河道的河长突然缩短,比降陡增,之后河长以先快后慢的速率增长,尾闾河道比降则呈指数衰减,经过约5~6 年调整至平衡比降,其变化过程反映了典型的河床演变滞后响应特性。基于黄河口河道的演变特征,提出了河口河道水位和纵比降变化的概化模式,并采用滞后响应 模型建立了河口河道同流量水位的计算方法,较好地计算了1954—2012年间黄河下游利津3 000 m3/s同流量水位的变化过程。该计算方法不仅考虑了河床演变的滞后响应特性,而且反映了来水来沙和河道淤长与蚀退对利津同流量水位的共同影响,能够连续 地模拟河口淤积延伸及改道过程中河口河道特征水位的长期变化过程。研究成果可为分析黄河口淤积延伸与下游河道相对侵蚀基准面的变化关系提供参考。
[56]Shi C X, Zhang D.Processes and mechanisms of dynamic channel adjustment to delta progradation: The case of the mouth channel of the Yellow River, China
. Earth Surface Processes and Landforms, 2003, 28: 609-624.
https://doi.org/10.1002/esp.465URL [本文引用: 1]摘要
Abstract This paper analyses the processes and mechanisms of a three-stage channel adjustment over a cycle of the Yellow River mouth channel extension based on data comprising hydrologic measurements and channel geometric surveys. Rapid siltation in the mouth channel takes place in the young stage when the channel is being built by deposits and in the old stage when the channel cannot further adjust itself to keep sediment transport in equilibrium. It is disclosed that the bankfull width epth ratio, bed material size and slope decrease in the young and mature stages but do not change in the old stage. The reduction of bankfull width epth ratio and bed material size during the young and mature stages is found to be able to offset the effect of the slope reduction on sediment transport due to continuous mouth progradation. They reach their limits in old stage, and a constant slope is kept by unceasing sediment accumulation. The grain size composition of incoming sediment and the fining mechanism are responsible for the occurrence of lower limit of bed material size. The reason for the existence of a limit of bankfull cross-sectional shape is that the large flows can fully transport the sediment load they are carrying, and siltation in the channel in the old stage takes place mainly in the low flows. It is suggested that the bankfull discharge plays an important role in shaping the channel but that the entire channel form is the product of both the large and low flows plus the effects of interaction between them. Channel pattern change shows a process from a braided pattern in the young stage to a straight pattern in the mature and old stages, and the straight channel becomes gradually sinuous. The occurrence and transformation of the channel patterns are supported by two planform predictors, but are also facilitated by some other conditions. Copyright 2003 John Wiley & Sons, Ltd.
[57]You Liangyuan.Impact of Xiaolangdi water conservation project on deposition reduction of the Huanghe River estuary
. Progress in Geography, 2000, 19(2): 142-149.
https://doi.org/10.11820/dlkxjz.2000.02.007Magsci [本文引用: 1]摘要
本文在整理、分析黄河小浪底工程建成后 ,坝下游来水来沙条件变化的基础上 ,利用若干经验关系式 ,就小浪底工程修建后对黄河河口区清水沟流路的淤积特征和变化趋势进行了研究 ,得到了 :在小浪底水库初期蓄水拦沙运用阶段 ,淤积减少、河口砂嘴发展速度变缓 ;在后期正常调水调沙运用阶段 ,淤积又有所恢复 ,河口砂嘴发展加快的认识。
[尤联元. 小浪底工程修建对黄河河口淤积影响
. 地理科学进展, 2000, 19(2): 142-149.]
https://doi.org/10.11820/dlkxjz.2000.02.007Magsci [本文引用: 1]摘要
本文在整理、分析黄河小浪底工程建成后 ,坝下游来水来沙条件变化的基础上 ,利用若干经验关系式 ,就小浪底工程修建后对黄河河口区清水沟流路的淤积特征和变化趋势进行了研究 ,得到了 :在小浪底水库初期蓄水拦沙运用阶段 ,淤积减少、河口砂嘴发展速度变缓 ;在后期正常调水调沙运用阶段 ,淤积又有所恢复 ,河口砂嘴发展加快的认识。
[58]Zhang Hongwu, Zhao Lianjun, Cao Fengsheng.A study on the causes of formation and transformation of wandering channel pattern
. Yellow River, 1996(1): 10-15.
URL [本文引用: 1]摘要
本文借鉴前人有研究成果,归纳分析后得出河床纵向与横向稳定性指标的表达式,并进一步给出河床的综合性指标NW,将它作为区划河型的判数:ZW〈5,游荡型;5≤ZW≤15,分汊型;ZW〉15,弯曲型,为研究游荡河型转化而进行的自然河工模型试验表明,若要将黄河下游的游荡河型转化为限制性弯曲河型,两岸有效的控导工程总长度至少应占工度的88%,每处工程长度需要达到4km左右,但就现在的整治工程情况而言,即使来多
[张红武, 赵连军, 曹丰生. 游荡河型成因及其河型转化问题的研究
. 人民黄河, 1996(1): 10-15.]
URL [本文引用: 1]摘要
本文借鉴前人有研究成果,归纳分析后得出河床纵向与横向稳定性指标的表达式,并进一步给出河床的综合性指标NW,将它作为区划河型的判数:ZW〈5,游荡型;5≤ZW≤15,分汊型;ZW〉15,弯曲型,为研究游荡河型转化而进行的自然河工模型试验表明,若要将黄河下游的游荡河型转化为限制性弯曲河型,两岸有效的控导工程总长度至少应占工度的88%,每处工程长度需要达到4km左右,但就现在的整治工程情况而言,即使来多
[59]Shi Chuanwen, Wu Baosheng, Ma Jiming.Cause of formation and discrimination of channel patterns for alluvial rivers
. Yellow River, 2007, 26(5): 107-111.
https://doi.org/10.3969/j.issn.1003-1243.2007.05.021URL [本文引用: 1]摘要
本文建立的冲积河流河型成因的输沙平衡程度概念认为,不同冲积河 流河型形成的根本原因在于其输沙平衡程度的不同.根据强平衡输沙概念,建立了冲积河流稳定程度公式.利用黄河、渭河和汉江部分资料进行的初步计算表明,根 据河型成因的输沙平衡程度概念,基于冲积河流稳定程度公式,采用模糊聚类方法,可以建立一套完整的河型分类与判别的模糊聚类计算方法.
[史传文, 吴保生, 马吉明. 冲积河流河型的成因及分类与判别计算方法研究
. 人民黄河, 2007, 26(5): 107-111.]
https://doi.org/10.3969/j.issn.1003-1243.2007.05.021URL [本文引用: 1]摘要
本文建立的冲积河流河型成因的输沙平衡程度概念认为,不同冲积河 流河型形成的根本原因在于其输沙平衡程度的不同.根据强平衡输沙概念,建立了冲积河流稳定程度公式.利用黄河、渭河和汉江部分资料进行的初步计算表明,根 据河型成因的输沙平衡程度概念,基于冲积河流稳定程度公式,采用模糊聚类方法,可以建立一套完整的河型分类与判别的模糊聚类计算方法.
[60]Xu J X.Comparison of hydraulic geometry between sand- and gravel-bed rivers in relation to channel pattern discrimination,
Earth Surface Processes and Landforms, 2004, 29(5): 645-657.
https://doi.org/10.1002/esp.1059URL [本文引用: 1]摘要
A comparison has been made between the hydraulic geometry of sand- and gravel-bed rivers, based on data from alluvial rivers around the world. The results indicate a significant difference in hydraulic geometry among sand- and gravel-bed rivers with different channel patterns. On this basis, some diagrams for discrimination of meandering and braided channel patterns have been established. The relationships between channel width and water discharge, between channel depth and water discharge, between width-depth ratio and water discharge and between channel slope and water discharge can all be used for channel pattern discrimination. The relationship between channel width and channel depth can also be used for channel pattern discrimination. However, the accuracy of these relationships for channel pattern discrimination varies, and the depth-discharge relationship is a better discriminator of pattern type than the classic slope-discharge function. The cause for this difference has been explained qualitatively. To predict the development of channel patterns under different natural conditions, the pattern discriminator should be searched on the basis of independent or at least semi-independent variables. The relationship between stream power and bed material grain size can be used to discriminate channel patterns, which shows a better result than the discriminator using the slope-discharge relationship. Copyright (C) 2004 John Wiley Sons, Ltd.
[61]Xu J X.Discrimination of channel patterns for gravel- and sand-bed rivers
. Zeischrift fur Geomorphology, 2008, 52(4): 503-523.
https://doi.org/10.1127/0372-8854/2008/0052-0503URL [本文引用: 1]摘要
中国科学院机构知识库(中国科学院机构知识库网格(CAS IR GRID))以发展机构知识能力和知识管理能力为目标,快速实现对本机构知识资产的收集、长期保存、合理传播利用,积极建设对知识内容进行捕获、转化、传播、利用和审计的能力,逐步建设包括知识内容分析、关系分析和能力审计在内的知识服务能力,开展综合知识管理。
[62]Li Jiaojiao, Bai Yuchuan, Xu Haijue.Research on the classification method for gravel river based on the law of resistance of natural rivers
. Science in China Series E: Technological Sciences, 2015, 45(7): 721-736.
https://doi.org/10.1360/N092014-00153URL [本文引用: 1]摘要
河流形态特征的变化规律是人类认识与改造河流的主要课题.河流系统分布广泛,与人类活动密切相关,了解其类型特点是河流研究中的重要内容.水流在其行进过程中遵守阻力规律,由于周围环境的不同,其宏观表现形式也多种多样.河流的阻力规律决定于其形态特征,同时河流形态特征也反映其阻力规律.本文考虑影响河流水力损失的多种因素,引入无量纲的河流形态参数,得到自然河流的阻力规律表达式.由该阻力规律出发,得到河流形态参数的表达式,并将其作为河型分类标准.本文还加入了地貌因素的影响,应用得到的表达式细致划分了河流类型.研究结果表明,该分类方法计算简单,对于砂砾质河流应用效果较好.
[李娇娇, 白玉川, 徐海珏. 基于河流阻力规律的砂砾质河型分类方法研究,
中国科学E辑: 技术科学, 2015, 45(7): 721-736.]
https://doi.org/10.1360/N092014-00153URL [本文引用: 1]摘要
河流形态特征的变化规律是人类认识与改造河流的主要课题.河流系统分布广泛,与人类活动密切相关,了解其类型特点是河流研究中的重要内容.水流在其行进过程中遵守阻力规律,由于周围环境的不同,其宏观表现形式也多种多样.河流的阻力规律决定于其形态特征,同时河流形态特征也反映其阻力规律.本文考虑影响河流水力损失的多种因素,引入无量纲的河流形态参数,得到自然河流的阻力规律表达式.由该阻力规律出发,得到河流形态参数的表达式,并将其作为河型分类标准.本文还加入了地貌因素的影响,应用得到的表达式细致划分了河流类型.研究结果表明,该分类方法计算简单,对于砂砾质河流应用效果较好.
[63]Xu J X, Yan M.Discrimination of channel patterns for alluvial rivers based on the sediment concentration to water discharge ratio
. Zeitschrift fur Geomorphologie, 2010, 54(1): 111-125.
https://doi.org/10.1127/0372-8854/2010/0054-0007URL [本文引用: 1]摘要
Although the sediment concentration to water discharge ratio () is an empirical coefficient, it contains manifold physical meanings. Based on data from 107 Chinese alluvial rivers, a study has been made to relate river channel patterns to the index. These rivers can be classified as four channel patterns, i. e., braided, low concentration meandering, hyperconcentration meandering and island. It was found that, when mean annual water discharge () is given, the index for hyperconcentration meandering rivers is the highest, for braided rivers the second, for low-concentration meandering rivers the third, and for island rivers the lowest. A discriminating model has been proposed for the above four channel patterns, based on the relationship between and Q. Three threshold lines between the four channel patterns are well identified. The limits between channel patterns have close relation with the phenomenon of ouble-thresholds for fill-scour behaviors of rivers with wide-range sediment concentrations , which was previously described by the author. The limit between hyperconcentrationmeandering rivers and braided rivers reflects the upper threshold of the double-thresholds phenomenon, and the limit between braided rivers and low-concentration meandering rivers reflects the lower threshold of the double-thresholds phenomenon. Of the 107 Chinese rivers studied, 84.7% are correctly predicted using the proposed model. Based on some Chinese rivers, the index is related to specific stream power () and channel sinuosity, and the result indicates that the complicated variation of with is one of the causes for the complicated variation of river channel patterns with the index. This complicated variation may be regarded as a complex response of river channel pattern to the varying index. This study also shows that the clay content in river bank material is controlled by the index to some degree. Thus, the index also contains some information of erosion-resistance of channel boundary materials. Through the effect of on channel boundary material, channel pattern is affected by . The proposed discriminating model may be used to predict the trend of channel pattern changes. Based on the data of and , the location of a given river for the pre- and post-impact periods can be plot in the diagram. If the river crosses the threshold line between two channel patterns, for instance the line between braided pattern and low concentration meandering pattern, or vice versa, channel pattern transformation may be expected to occur.
[64]Wang Suiji, Ni Jinren, Wang Guangqian.Model and relation of spatial and temporal changes of channel patterns
. Journal of Tsinghua University (Science and Technology), 2000, 40(S1): 96-100.
URL [本文引用: 1]摘要
从辫状河、曲流河和网状河的河型转化实例 ,归纳了 6种时间演化模式和 5种空间转化模式 ,并讨论了河型时空演变模式间的相互关系。河型的时空演变受控于构造运动、海平面变化、气候、植被、沉积体系的物质组成、流域的水沙供给状况和水动力条件等 ,上述因素彼此相关 ,但在不同的河型演变模式中的作用有所不同。
[王随继, 倪晋仁, 王光谦. 河型的时空演变模式及其间关系
. 清华大学学报(自然科学版), 2000, 41(S1): 96-100.]
URL [本文引用: 1]摘要
从辫状河、曲流河和网状河的河型转化实例 ,归纳了 6种时间演化模式和 5种空间转化模式 ,并讨论了河型时空演变模式间的相互关系。河型的时空演变受控于构造运动、海平面变化、气候、植被、沉积体系的物质组成、流域的水沙供给状况和水动力条件等 ,上述因素彼此相关 ,但在不同的河型演变模式中的作用有所不同。
[65]Li Zhiwei, Wang Zhaoyin, Yu Guoan.Development patterns and mechanism of sand bars on alluvial rivers
. Journal of Basic Science and Engineering, 2013, 21(3): 489-500.
https://doi.org/10.3969/j.issn.1005-0930.2013.03.011URL [本文引用: 1]摘要
沙洲是分汉型河道和河口区域重要的地貌特征和组成单元.沙洲的发育对分汉河型的形成和河口演变有重要影响,沙洲的稳定决定了分汉河道和河口航道的稳定.根据遥感影像和野外调查发现,冲积型河流的沙洲存在两种发育模式:)中积河道的沙洲是洲头淤积逆水流向上游的发育模式,河口区域的沙洲是洲尾淤积顺水流向下游的发育模式,两者的发育机理不尽相同.通过分析冲积河道沙洲的沿程水头损失,沙洲向上游发育才能实现其沿程阻力达到最小.冲积河道的沙洲洲头浅滩滞流区和阻挡效应,共同作用促使悬移质在洲头浅滩淤积.洲尾汇流区,左汉和右汉水流汇合,水流挟水沙能力变大,泥沙难以在洲尾淤积,洲尾冲刷削尖成锐三角形.河口区域的沙洲洲头经受径流和潮流的双重作用,冲刷蚀退,而洲尾水面展宽使得流速降低,悬移质落淤促使洲尾不断淤长.沙洲表面的不同植被覆盖情况可验证沙洲必定向上游发育,已为天兴洲和玉带洲的遥感图像证实.
[李志威, 王兆印, 余国安. 冲积河流的沙洲发育模式与机理应用基础与工程科学学报, 2013, 21(3): 489-500.]https://doi.org/10.3969/j.issn.1005-0930.2013.03.011URL [本文引用: 1]摘要
沙洲是分汉型河道和河口区域重要的地貌特征和组成单元.沙洲的发育对分汉河型的形成和河口演变有重要影响,沙洲的稳定决定了分汉河道和河口航道的稳定.根据遥感影像和野外调查发现,冲积型河流的沙洲存在两种发育模式:)中积河道的沙洲是洲头淤积逆水流向上游的发育模式,河口区域的沙洲是洲尾淤积顺水流向下游的发育模式,两者的发育机理不尽相同.通过分析冲积河道沙洲的沿程水头损失,沙洲向上游发育才能实现其沿程阻力达到最小.冲积河道的沙洲洲头浅滩滞流区和阻挡效应,共同作用促使悬移质在洲头浅滩淤积.洲尾汇流区,左汉和右汉水流汇合,水流挟水沙能力变大,泥沙难以在洲尾淤积,洲尾冲刷削尖成锐三角形.河口区域的沙洲洲头经受径流和潮流的双重作用,冲刷蚀退,而洲尾水面展宽使得流速降低,悬移质落淤促使洲尾不断淤长.沙洲表面的不同植被覆盖情况可验证沙洲必定向上游发育,已为天兴洲和玉带洲的遥感图像证实.
[66]Wang Suiji.Comparison of depositional dynamics among the braided, meandering and straight channel reaches in the lower Yellow River
. Acta Sedimentologica Sinica, 2010, 28(2): 307-312.
Magsci [本文引用: 1]摘要
<FONT face=Verdana>黄河下游沿程出现了辫状、弯曲和顺直河型段,河道平面形态的差异势必受到不同的沉积动力特征的制约。本研究根据对收集到的有关实测资料的统计和计算,对可以表征河道沉积动力特征的相关指标进行了量化分析,发现不同河型段间的沉积动力特征存在明显差别。河道比降在辫状河段最大,介于0.2‰~0.14‰之间;弯曲河段的次之,介于0.14‰~0.10‰之间;顺直河段的小于0.10‰。平滩流量时的流速在辫状河段的较大,不同年份间的变幅较大;弯曲河段的次之,不同年份间的变幅较小;顺直河段的最小,不同年份间的变幅不大,并向下游显著减小。单位河长能耗率在辫状河段最大,弯曲河段次之,顺直河段的最小,其间的比值为2.31∶〖KG-*2〗1.35∶1。单位面积能耗率在辫状河段最小,弯曲河段最大,顺直河段次之,其间的比值为0.52∶〖KG-*2〗1.18∶〖KG-*2〗1。河床沉积物粒度较细,并普遍缺失推移质组分,中值粒度在辫状河段、弯曲河段和顺直河段分别为3.0、3.2、3.67;河床沉积物的分选性也依次变好。受制于上述相关沉积动力特性,河床沉积速率在不同河型段有明显差别:中大流量时,辫状河段的最小,弯曲河段的最大,顺直河段的次之;在小流量时,三个河型段的河床沉积速率非常接近,但沿程略有减小。另外,辫状河段河床沉积速率明显依赖于流量的变化,且随流量的增大而明显减小。<BR></FONT>
[王随继. 黄河下游辫状、弯曲和顺直河段间沉积动力特征比较
. 沉积学报, 2010, 28(2): 307-312.]
Magsci [本文引用: 1]摘要
<FONT face=Verdana>黄河下游沿程出现了辫状、弯曲和顺直河型段,河道平面形态的差异势必受到不同的沉积动力特征的制约。本研究根据对收集到的有关实测资料的统计和计算,对可以表征河道沉积动力特征的相关指标进行了量化分析,发现不同河型段间的沉积动力特征存在明显差别。河道比降在辫状河段最大,介于0.2‰~0.14‰之间;弯曲河段的次之,介于0.14‰~0.10‰之间;顺直河段的小于0.10‰。平滩流量时的流速在辫状河段的较大,不同年份间的变幅较大;弯曲河段的次之,不同年份间的变幅较小;顺直河段的最小,不同年份间的变幅不大,并向下游显著减小。单位河长能耗率在辫状河段最大,弯曲河段次之,顺直河段的最小,其间的比值为2.31∶〖KG-*2〗1.35∶1。单位面积能耗率在辫状河段最小,弯曲河段最大,顺直河段次之,其间的比值为0.52∶〖KG-*2〗1.18∶〖KG-*2〗1。河床沉积物粒度较细,并普遍缺失推移质组分,中值粒度在辫状河段、弯曲河段和顺直河段分别为3.0、3.2、3.67;河床沉积物的分选性也依次变好。受制于上述相关沉积动力特性,河床沉积速率在不同河型段有明显差别:中大流量时,辫状河段的最小,弯曲河段的最大,顺直河段的次之;在小流量时,三个河型段的河床沉积速率非常接近,但沿程略有减小。另外,辫状河段河床沉积速率明显依赖于流量的变化,且随流量的增大而明显减小。<BR></FONT>
[67]Li Zhiwei, Wang Zhaoyin, Yu Guoan, et al.River pattern transition and its causes along Maqu reach of Yellow River source region
. Journal of Sediment Research, 2013(3): 51-58.
https://doi.org/10.3969/j.issn.0468-155X.2013.03.010URL [本文引用: 1]摘要
黄河源玛曲河段是一段特殊的冲积平原河道,接连出现了网状河型、分汊河型、弯曲河型和辫状河 型,在270km的流程里,冲积河型发生了4次河型沿程变化。通过遥感图像和野外调查相结合,描述玛曲河段河型多样性和河道的基本特征,分析河型沿程变化 的原因。玛曲河段的冲积河道主要发生4次河型变化,即网状型-分汊型、网状型-弯曲型、弯曲型-辫状型和辫状型-弯曲型。网状型-分汊型变化的原因是地形 限制,泥沙淤积形成沙洲和植被发育。网状型-弯曲型变化的原因是地形限制、河床比降由大变小、河岸物质组成沿程变细。弯曲型-辫状型变化的原因是白河入 汇、河床比降变大。辫状型-弯曲型变化的主原因是下游峡谷段河床下切和黑河入汇。
[李志威, 王兆印, 余国安, . 黄河源玛曲河段河型沿程变化及其原因
. 泥沙研究, 2013(3): 51-58.]
https://doi.org/10.3969/j.issn.0468-155X.2013.03.010URL [本文引用: 1]摘要
黄河源玛曲河段是一段特殊的冲积平原河道,接连出现了网状河型、分汊河型、弯曲河型和辫状河 型,在270km的流程里,冲积河型发生了4次河型沿程变化。通过遥感图像和野外调查相结合,描述玛曲河段河型多样性和河道的基本特征,分析河型沿程变化 的原因。玛曲河段的冲积河道主要发生4次河型变化,即网状型-分汊型、网状型-弯曲型、弯曲型-辫状型和辫状型-弯曲型。网状型-分汊型变化的原因是地形 限制,泥沙淤积形成沙洲和植被发育。网状型-弯曲型变化的原因是地形限制、河床比降由大变小、河岸物质组成沿程变细。弯曲型-辫状型变化的原因是白河入 汇、河床比降变大。辫状型-弯曲型变化的主原因是下游峡谷段河床下切和黑河入汇。
[68]Zhu Lingling, Ge Hua, Li Yitian, et al.Branching channels in the middle Yangtze River, China
. Journal of Basic Science and Engineering, 2015, 23(2): 246-258.
URL [本文引用: 1]摘要
长江中游宜昌-湖口河段分汊河型分布广泛,涵盖了顺直分汊、微弯分汊及鹅头型分汊3种类型.本文依据三峡水库蓄水以来大量原型观测资料,总结归纳了长江中游各分汊河段的演变特征及其内在机理,并初步预测了其发展趋势.研究结果表明,三峡水库蓄水后,沙量大幅减少,同时局部河床边界条件发生变化,长江中游分汊河段普遍出现支汊冲刷发展、中低滩冲刷变形、高滩滩缘崩退等演变现象.伴随着三峡水库调度方式的不断优化,加之河床冲刷下造床质输移水平的沿程恢复,以及大量航道整治工程的作用,城陵矶以下分汊河段稳定性将优于荆江河段.
[朱玲玲, 葛华, 李义天, . 三峡水库蓄水后长江中游分汊河道演变机理及趋势
. 应用基础与工程科学学报, 2015, 23(2): 246-258.]
URL [本文引用: 1]摘要
长江中游宜昌-湖口河段分汊河型分布广泛,涵盖了顺直分汊、微弯分汊及鹅头型分汊3种类型.本文依据三峡水库蓄水以来大量原型观测资料,总结归纳了长江中游各分汊河段的演变特征及其内在机理,并初步预测了其发展趋势.研究结果表明,三峡水库蓄水后,沙量大幅减少,同时局部河床边界条件发生变化,长江中游分汊河段普遍出现支汊冲刷发展、中低滩冲刷变形、高滩滩缘崩退等演变现象.伴随着三峡水库调度方式的不断优化,加之河床冲刷下造床质输移水平的沿程恢复,以及大量航道整治工程的作用,城陵矶以下分汊河段稳定性将优于荆江河段.
[69]Jiang Ling, Li Yitian, Sun Zhaohua, et al.Channel evolution of Jingjiang reach and its influences on waterway after impoundment of the Three Gorges Project
. Journal of Basic Science and Engineering, 2010, 18(1): 1-9.
https://doi.org/10.3969/j.issn.1005-0930.2010.01.001URL [本文引用: 1]摘要
分析了三峡工程蓄水以来荆江沙 质河段不同类型河床的演变特性,预测计算了水库下游河床冲刷过程,进而探讨了河床演变趋势及其对航道的影响.资料分析表明,蓄水初期,上荆江深泓下切明 显,但分汊放宽段航深不足问题突出;下荆江深泓冲淤相间,长顺直(微弯)河段的深槽过渡段下移,弯道进口处水流较分散,致使航槽不稳定.基于数学模型计算 结果预测,蓄水5—10年,太平口—藕池口河段发生强烈冲刷,分汊放宽段中枯水河槽更宽浅,致使航道条件恶化,而且,支汊发展会影响主汊的通航条件;藕池 口以下处于冲刷初期,过渡段浅滩碍航与否主要与退水过程有关,但弯道发展将使航槽位置发生变动.蓄水15—20年,藕池口以上冲刷基本完成,上荆江微弯分 汊河型趋于稳定;藕池口以下发生强烈冲刷,过渡段浅滩高程降低,有利于航深的增加,弯道可能出现局部撇弯,致使航槽移位.
[江凌, 李义天, 孙昭华, . 三峡工程蓄水后荆江沙质河段河床演变及对航道的影响
. 应用基础与工程科学学报, 2010, 18(1): 1-9.]
https://doi.org/10.3969/j.issn.1005-0930.2010.01.001URL [本文引用: 1]摘要
分析了三峡工程蓄水以来荆江沙 质河段不同类型河床的演变特性,预测计算了水库下游河床冲刷过程,进而探讨了河床演变趋势及其对航道的影响.资料分析表明,蓄水初期,上荆江深泓下切明 显,但分汊放宽段航深不足问题突出;下荆江深泓冲淤相间,长顺直(微弯)河段的深槽过渡段下移,弯道进口处水流较分散,致使航槽不稳定.基于数学模型计算 结果预测,蓄水5—10年,太平口—藕池口河段发生强烈冲刷,分汊放宽段中枯水河槽更宽浅,致使航道条件恶化,而且,支汊发展会影响主汊的通航条件;藕池 口以下处于冲刷初期,过渡段浅滩碍航与否主要与退水过程有关,但弯道发展将使航槽位置发生变动.蓄水15—20年,藕池口以上冲刷基本完成,上荆江微弯分 汊河型趋于稳定;藕池口以下发生强烈冲刷,过渡段浅滩高程降低,有利于航深的增加,弯道可能出现局部撇弯,致使航槽移位.
[70]Wang Weihong, Tian Shimin, Meng Zhihua, et al.Evolution processes of river pattern in Lower Yellow River after commissioning of Xiaolangdi Reservoir
. Journal of Sediment Research, 2012(1): 23-31.
https://doi.org/10.3969/j.issn.0468-155X.2012.01.004URL [本文引用: 1]摘要
利用实测资料分析、理论判别和分形维数计算等方法,以黄河下游铁谢—伊洛河口、花园口—黑岗口和夹河滩—高村三个典型游荡性河段为研究对象,分析其1960年以来的主流摆幅、弯曲系数和主河槽宽深比等河势参数变化,以及小浪底水库修建前后下游游荡性河段的河型演化过程。结果表明,自20世纪90年代初,除花园口—黑岗口河段仍表现为游荡河性外,其他两个河段因整治工程不断完善其游荡性均有明显减弱,河型趋于限制性弯曲方向发展。自1999年10月小浪底水库拦沙运用以来,三个研究河段的整体游荡程度显著减弱,河势趋于规划流路方向发展,特别是夹河滩—高村河段河势基本稳定。小浪底水库长期下泄低含沙小流量过程,水流动力减弱,加之不断完善的河道整治工程,是河势游荡程度显著减小、河势归顺及河型发生变化的主要原因。
[王卫红, 田世民, 孟志华, . 小浪底水库运用前后黄河下游河道河型变化及成因分析
. 泥沙研究, 2012(1): 23-31.]
https://doi.org/10.3969/j.issn.0468-155X.2012.01.004URL [本文引用: 1]摘要
利用实测资料分析、理论判别和分形维数计算等方法,以黄河下游铁谢—伊洛河口、花园口—黑岗口和夹河滩—高村三个典型游荡性河段为研究对象,分析其1960年以来的主流摆幅、弯曲系数和主河槽宽深比等河势参数变化,以及小浪底水库修建前后下游游荡性河段的河型演化过程。结果表明,自20世纪90年代初,除花园口—黑岗口河段仍表现为游荡河性外,其他两个河段因整治工程不断完善其游荡性均有明显减弱,河型趋于限制性弯曲方向发展。自1999年10月小浪底水库拦沙运用以来,三个研究河段的整体游荡程度显著减弱,河势趋于规划流路方向发展,特别是夹河滩—高村河段河势基本稳定。小浪底水库长期下泄低含沙小流量过程,水流动力减弱,加之不断完善的河道整治工程,是河势游荡程度显著减小、河势归顺及河型发生变化的主要原因。
[71]Chen Xujian, Chen Qingyang.Theory of river pattern transformation and change of channel sinuosity ratio in Lower Yellow River
. Journal of Sediment Research, 2013(1): 1-6.
https://doi.org/10.3969/j.issn.0468-155X.2013.01.001URL [本文引用: 1]摘要
冲积河流河型转换及弯曲变化机理是一个有争议的自然科学难题,根据河道卫星图片量测结果,分 析了黄河下游各河段的主河槽弯曲系数变化,各河段的主河槽弯曲系数对比表明,小浪底水库运用后,黄河下游各河段的主河槽弯曲系数有所增大,其中游荡型河段 主河槽弯曲系数由1.12增大到1.29,游荡型有向弯曲型转化的趋势;过渡性河段的主河槽弯曲系数由1.23增大到1.35,过渡性河段基本转变为弯曲 型;弯曲型河段的主河槽弯曲系数由1.19增大到1.25。探讨了河道形态弯曲变化的机理,从理论上解释了水库的滞洪沉沙作用使下泄水流含沙量减小、泥沙 粒径变细、洪峰调平,使下游游荡型有向弯曲型转化的趋势,主河槽弯曲系数增大。
[陈绪坚, 陈清扬. 黄河下游河型转换及弯曲变化机理
. 泥沙研究, 2013(1): 1-6. ]
https://doi.org/10.3969/j.issn.0468-155X.2013.01.001URL [本文引用: 1]摘要
冲积河流河型转换及弯曲变化机理是一个有争议的自然科学难题,根据河道卫星图片量测结果,分 析了黄河下游各河段的主河槽弯曲系数变化,各河段的主河槽弯曲系数对比表明,小浪底水库运用后,黄河下游各河段的主河槽弯曲系数有所增大,其中游荡型河段 主河槽弯曲系数由1.12增大到1.29,游荡型有向弯曲型转化的趋势;过渡性河段的主河槽弯曲系数由1.23增大到1.35,过渡性河段基本转变为弯曲 型;弯曲型河段的主河槽弯曲系数由1.19增大到1.25。探讨了河道形态弯曲变化的机理,从理论上解释了水库的滞洪沉沙作用使下泄水流含沙量减小、泥沙 粒径变细、洪峰调平,使下游游荡型有向弯曲型转化的趋势,主河槽弯曲系数增大。
[72]Wang Guangqian, Zhang Hongwu, Xia Junqiang.Changes and Simulation of Wandering Rivers. Beijing: Science Press, 2005: 1-445.URL [本文引用: 1]摘要
本书为作者多年实践工作的总结。本书共分五篇,主要介绍了游荡型河流演变的基本规律、水沙变化与河道整合治对典型游荡型河段演变的影响、游荡型河流演变的模拟技术、数值模拟技术和模型试验技术在游荡型河流演变中的工程应用。本书可供水利水电工程、交通等专业科技人员及高等院校相关专业师生阅读和参考。
[王光谦, 张红武, 夏军强. 游荡型河流演变及模拟. 北京: 科学出版社, 2005: 1-445.]URL [本文引用: 1]摘要
本书为作者多年实践工作的总结。本书共分五篇,主要介绍了游荡型河流演变的基本规律、水沙变化与河道整合治对典型游荡型河段演变的影响、游荡型河流演变的模拟技术、数值模拟技术和模型试验技术在游荡型河流演变中的工程应用。本书可供水利水电工程、交通等专业科技人员及高等院校相关专业师生阅读和参考。
[73]Schumm S A. The Fluvial System
. New York: John Wiley and Sons, 1977: 1-338.
[本文引用: 1]
[74]Zhang Ouyang, Xu Jiongxin.Decoupling of the Yellow River basin system
. Geographical Research, 2002, 21(2): 188-194.
Magsci [本文引用: 1]摘要
<p>根据Schumm提出的河流系统的理论对黄河流域地貌系统进行了划分。结果表明 ,整个黄河流域地貌系统可以很明确地分为产水产沙系统、输移系统和沉积系统 ,其模式与Schumm的理想流域模式非常吻合 ,同时又表现出其特殊性。以河口镇为界 ,黄河流域上游和中下游两部分分别具有对应的产水系统、产沙系统和河道输移系统 ,各子系统处于动态变化过程中 ,存在一种强耦合关系 ,这种特点主要是由黄河流域的历史发育过程决定的。</p>
[张欧阳, 许炯心. 黄河流域产水产沙、输移和沉积系统的划分
. 地理研究, 2002, 21(2): 188-194.]
Magsci [本文引用: 1]摘要
<p>根据Schumm提出的河流系统的理论对黄河流域地貌系统进行了划分。结果表明 ,整个黄河流域地貌系统可以很明确地分为产水产沙系统、输移系统和沉积系统 ,其模式与Schumm的理想流域模式非常吻合 ,同时又表现出其特殊性。以河口镇为界 ,黄河流域上游和中下游两部分分别具有对应的产水系统、产沙系统和河道输移系统 ,各子系统处于动态变化过程中 ,存在一种强耦合关系 ,这种特点主要是由黄河流域的历史发育过程决定的。</p>
[75]Xu J X, Cheng D S.Relation between the erosion and sedimentation zones in the Yellow River, China
. Geomorphology, 2002, 48(4): 365-382.
https://doi.org/10.1016/S0169-555X(02)00145-9Magsci [本文引用: 1]摘要
<h2 class="secHeading" id="section_abstract">Abstract</h2><p id="">Sedimentation in the lower reaches of the Yellow River is a major problem requiring implementation of large-scale control measures in the upper and middle drainage basin. For maximum benefit, major sediment generation areas must be delimited. For this purpose, the upper and middle drainage basin of the Yellow River has been divided into four major sediment and water source areas. A series of databases of runoff and sediment yields from these source areas and for the corresponding quantities of sedimentation in the lower Yellow River channel have been established. On this basis, a set of multiple-regression equations has been established that define the relationships between sedimentation in the lower Yellow River and the yearly or event-based runoff and sediment yields from the four source areas or subsystems. Based on the regression equations obtained, the contribution of the four major source areas to the sedimentation in the lower Yellow River channel can be estimated. The results obtained indicate that, given other factors, for each ton of sediment reduced from the coarse-sediment producing area (CSA), the sediment deposited in the lower Yellow River would be reduced by 0.455 ton; for each ton of sediment reduced from the fine-sediment producing area (FSA), the sediment deposited in the lower Yellow River would be reduced by 0.154 ton only. Therefore, if limited erosion control measures are applied to the coarse-sediment producing area, the benefits for sedimentation reduction in the lower Yellow River will be much larger than if similar resources are applied to the fine-sediment producing area.</p>
[76]Xu Jiongxin.Channel sedimentation in the Lanzhou-Toudaoguai reach of the upper Yellow River influenced by runoff and sediment from different source areas
. Journal of Sediment Research, 2014(5): 1-10.
URL

[许炯心. 异源水沙对黄河上游兰州至头道拐河段悬移质泥沙冲淤的影响
. 泥沙研究, 2014(5): 1-10.]
URL
[77]Xu J X.Sediment storage in the reach of the middle Yellow River located in the Fenwei Graben, China
. Hydrological Processes, 2013, 27: 2623-2636.
https://doi.org/10.1002/hyp.9401URL [本文引用: 1]摘要
Fenwei Graben is a famous sediment sink. The Longmen-Sanmexia sediment sink of middle Yellow River is located in the middle part. Using the sediment budget based on annual data from the period 1920-2006 and flood-event data from 154 flood events from the period 1950-1985, the variations in sediment storage, release and transport have been analysed. Data from different methods and sources indicate that, during an 1800-year period, the variation of sedimentation rate in this sink has undergone a cycle from increase to decline; the cause for this can be found in the changes in the manner and intensity of human activities. Over 87 years, sediment storage in this sink can be separated into four stages which showed different trends, depending on changing human activities, such as reservoir construction, soil and water conservation and water diversion. Stepwise multiple regression shows that the runoff and sediment yield from three major source areas have differing influences on sediment storage in the sink. Copyright (C) 2012 John Wiley & Sons, Ltd.
[78]Xu J X.The influence of dilution on downstream channel sedimentation in large rivers: The Yellow River, China
. Earth Surface Processes and Landforms, 2013, 39(4): 450-462.
[本文引用: 1]
[79]Xu J X.Hyperconcentrated flows in the slope-channel systems in gullied hilly areas on the Loess Plateau, China
. Geografisca Annaler, 2004, 86A(4): 349-366.
URL [本文引用: 1]摘要
Based on the data from Zizhou and Wangjiagou Experimental stations in the coarse sediment-producing area of the middle Yellow River drainage basin, this study deals with characteristics of hyperconcentrated flows in slope-channel systems in the gullied hilly areas. The results show that there exists a sediment storing-releasing mechanism in the systems, which is related to the different behaviors of sediment transport by non-hyperconcentrated and hyperconcentrated flows. For the non-hyperconcentrated flows, the relatively coarse fractions of sediment from the slopes are deposited in the channel,and for the hyperconcentrated flows, the previously deposited coarse sediment may be eroded and released from the channel. There is a close relationship between rainfall and the formation of hyperconcentrated flows. Two thresholds are observed from the plot of event maximum suspended sediment concentration versus rainfall intensity. When the first threshold is exceeded, the sediment concentration increases sharply and when the second is exceeded, there is a extreme concentration, i.e., the sediment concentration remain unchanged with the increase in rainfall intensity.
[80]Xu J X.Double thresholds in scour-fill processes and some implications in channel adjustment
. Geomorphology, 2004, 57: 321-330.
https://doi.org/10.1016/S0169-555X(03)00163-6URL [本文引用: 1]摘要
Through an analysis of data collected from the Yellow River and its tributaries on the Loess Plateau of China, the phenomenon of double-thresholds in scour-fill processes of wide-range water-sediment two-phase flows has been shown. Thresholds located in non-hyperconcentrated flows may be called the lower threshold, and that in hyperconcentrated flows the upper threshold. This double-threshold phenomenon leads to complicated sediment transport behavior of heavily sediment-laden rivers. With an increase in suspended sediment concentration, the channel sediment delivery ratio increases initially and becomes higher than 1, followed by a decrease and finally becomes lower than 1 again. Controlled by the double-thresholds in the scour-fill processes, channel adjustment of the lower Yellow River is non-linear and complex. When the suspended concentrations were lower than the lower threshold or higher than the upper threshold, scour or bed downcutting was the dominant channel-forming process. Channel shape tends to be narrower and deeper, and the channel thalweg became more sinuous. When the suspended concentrations lay between the lower and upper thresholds, deposition of sediment was the dominant channel-forming process; channel shape tended to be shallower and wider, and channel thalweg became less sinuous.
[81]Liao Jianhua, Xu Jiongxin, Yang Yonghong.Study of the spatial differentiation of hyperconcentrated flows frequency in the Loess Plateau
. Advances in Water Science, 2008, 19(2): 160-170.
Magsci [本文引用: 1]摘要
以1964-1989年黄土高原区284个水文站的泥沙观测资料为基础,结合相应区域内自然条件与人类活动相关资料,运用空间分析及数理统计方法,研究了黄土高原区高含沙水流发生频率的空间分布规律,并分析了高含沙水流发生频率及其与各影响因素之间的关系。研究结果表明,黄土高原区高含沙水流发生频率高值区为带状分布,呈东北-西南向,且存在3个高值中心区,分别位于111&#176;E、40&#176;N,107&#176;E、36&#176;N和104&#176;E、34&#176;N附近;在分析各影响因素与高含沙水流发生频率关系基础上,进一步研究了多因素对高含沙水流发生频率的综合影响,结果表明,灌木林、丘陵旱地、有林地、黄土厚度、年平均降水量等主要影响因素对高含沙水流发生频率的相对贡献率依次为17%、4%、7%、30%、42%。
[廖建华, 许炯心, 杨永红. 黄土高原区高含沙水流发生频率空间分异及其影响因素
. 水科学进展, 2008, 19(2): 160-170.]
Magsci [本文引用: 1]摘要
以1964-1989年黄土高原区284个水文站的泥沙观测资料为基础,结合相应区域内自然条件与人类活动相关资料,运用空间分析及数理统计方法,研究了黄土高原区高含沙水流发生频率的空间分布规律,并分析了高含沙水流发生频率及其与各影响因素之间的关系。研究结果表明,黄土高原区高含沙水流发生频率高值区为带状分布,呈东北-西南向,且存在3个高值中心区,分别位于111&#176;E、40&#176;N,107&#176;E、36&#176;N和104&#176;E、34&#176;N附近;在分析各影响因素与高含沙水流发生频率关系基础上,进一步研究了多因素对高含沙水流发生频率的综合影响,结果表明,灌木林、丘陵旱地、有林地、黄土厚度、年平均降水量等主要影响因素对高含沙水流发生频率的相对贡献率依次为17%、4%、7%、30%、42%。
[82]Xu J X, Yang J S, Yan Y X.Erosion and sediment yield as influenced by coupled eolian and fluvial processes: The Yellow River, China
. Geomorphology, 2006, 73(1): 1-15.
https://doi.org/10.1016/j.geomorph.2005.03.012URL [本文引用: 1]摘要
Based on data from the middle Yellow River, a model of erosion and sediment yield is proposed to describe coupled eolian and fluvial processes in a transitional zone from arid to sub-humid climates, and to explain rapid erosion and a high sediment yield in the zone. In the study area, wind action predominates from March to June, which erodes weathered bedrock and transports eolian sand to gullies, river channels and floodplains. In the following summer, especially from July to September, rainstorm runoff in gullies and river channels transports large quantities of fine loessic material, in the form of hyperconcentrated flow. As a result, most of the previously stored eolian sand and material supplied by mass-wasting of loess can be transported to the major tributaries and the main stream of the Yellow River, resulting in the high specific sediment yield. There exists an optimal grain size composition which maximizes suspended sediment concentration in the study area, resulted from the combined wind-water processes.
[83]Xu J X.Influences of coupled wind-water processes on suspended sediment grain size: An example from tributaries of the Yellow River
. Hydrological Science Journal, 2005, 50(5): 881-896.
https://doi.org/10.1623/hysj.2005.50.5.881URL摘要
Catchments; Flow of fluids; Grain size and shape; Precipitation (meteorology); Regression analysis; Sediments; Water; Wind
[84]Xu J X.Hyperconcentrated flows as influenced by coupled wind-water processes
. Science in China Series D: Earth Sciences, 2005, 48(11): 1990-2000.
https://doi.org/10.1360/04yd0307URL摘要
Using data from more than 40 rivers in the middle Yellow River basin, a study has been made of the influence of coupled wind-water processes on hyperconcentrated flows. A simple ehicle model has been proposed to describe hyperconcentrated flows. The liquid phase of two-phase flows is a ehicle , in which coarse sediment particles are carried as solid-phase The formation and characteristics of hyperconcentrated flows are closely related with the formation and characteristics of this liquid-phase and solid-phase. Surface materials and geomorphic agents of the middle Yellow River basin form some patterns of combination, which have deep influence on the formation and characteristics of liquid- and solid-phases of hyperconcentrated flows. The combination of high percentages of relatively coarse material with low percentages of fine material appears in the area predominated by the wind process, where the supply of relatively coarse sediment is sufficient, but the supply of relatively coarse sediment is not. The combination of low percentages of relatively coarse material with high percentages of fine material appears in the area predominated by the water process, where the supply of fine sediment is sufficient, but the supply of fine sediment is not. In the area predominated by coupled wind-water processes appears the combination of medium percentages of coarse and fine materials, and thus both coarse and fine sediments are in relatively sufficient supply. The manner in which the mean annual sediment concentrations of liquid- and solid-phases vary with total suspended sediment concentration is different. With the increased total suspended sediment concentration, mean annual sediment concentration of liquid-phase increased to a limit and then remained constant; however, mean annual sediment concentrations of solid-phase increased continuously. Thus, the magnitude of total suspended sediment concentration depends on the supply conditions of relatively coarse sediment and the ability of the flow to carry these relatively coarse sediment particles. In the area predominated by wind process, both the liquid- and the solid-phases cannot develop well, and their concentrations are low. In the area predominated by the water process, the mean annual sediment concentrations of liquid- and solid-phases are also low. Only in the area predominated by coupled wind-water processes, can the conditions most favor the development of both the liquid- and solid-phases, and then the peaks of mean annual sediment concentrations of liquid- and solid-phases appear. Low values of suspended sediment concentrations appear in the areas predominated by the wind process or by the water process, a fact indicating that the predominating wind process or water process does not favor the development of hyperconcentrated flows. Peak values.appear in the area where the coupled wind-water processes are predominated, indicating that the coupled wind-water processes most favor the development of hyperconcentrated flows.
[85]Xu J X.The behavior of specific sediment yield in different grain size fractions in the tributaries of the middle Yellow River as influenced by eolian and fluvial processes. Earth Surface Processes and
Landforms. 2008, 33: 1157-1173.
https://doi.org/10.1002/esp.1603URL [本文引用: 1]摘要
Based on data from 35 stations on the tributaries of the Yellow River, annual specific sediment yield (Ys) in eight grain size fractions has been related to basin-averaged annual sand-dust storm days (Dss) and annual precipitation (Pm) to reveal the influence of eolian and fluvial processes on specific sediment yield in different grain size fractions. The results show that Ys in fine grain size fractions has the highest values in the areas dominated by the coupled wind-water process. From these areas to those dominated by the eolian process or to those dominated by the fluvial process, Ys tends to decrease. For relatively coarse grain size fractions, Ys has monotonic variation, i.e. with the increase in Dss or the decrease in Pm, Ys increases. This indicates that the sediment producing behavior for fine sediments is different from that for relatively coarse sediments. The results all show that Ys for relatively coarse sediments depends on the eolian process more than on the fluvial process, and the coarser the sediment fractions the stronger the dependence of the Ys on the eolian process. The Ys-Dss and Ys-Pm curves for fine grain size fractions show some peaks and the fitted straight lines for Y-Dss and Ys-Pm relationships for relatively coarse grain size fractions show some breaks. Almost all these break points may be regarded as thresholds. These thresholds are all located in the areas dominated by the coupled wind-water process, indicating that these areas are sensitive for erosion and sediment production, to which more attention should be given for the purpose of erosion and sediment control. A number of regression equations were established, based which the effect of rainfall, sand-dust storms and surface material grain size on specific sediment yield can be assessed. Copyright 2007 John Wiley & Sons, Ltd.
[86]Xu J X, Yan Y X.Effect of reservoir construction on suspended sediment load in a large river system: Thresholds and complex response
. Earth Surface Processes and Landforms, 2010, 35: 1666-1673.
https://doi.org/10.1002/esp.2006URL [本文引用: 1]摘要
Dam construction greatly alters the channel boundary of rivers, making the dammed river system a human-controlled system. Based on hydrometric data in the upper Changjiang River basin, the change in behaviour of sediment transport of some dammed rivers was studied. As a result, some phenomena of threshold and complex response were found. When the coefficient (C(r,a)) of actual runoff regulation by reservoirs, defined as the ratio of total capacity of reservoirs to annual runoff input, is smaller than 10%, suspended sediment load at Yichang station, the control station of the Changjiang River, shows a mild decreasing trend. When this coefficient becomes larger than 10%, suspended sediment load decreases sharply. The coefficient of 10% can be regarded as a threshold. The C(r,a) of 10% is also a threshold, when the variation of suspended sediment concentration (SSC) with C(r,a) at Yichang station is considered. The impacts of reservoir construction can be divided into several stages, including road construction, dam building and closure, water storage and sediment trapping. During these stages, some complex response was identified. At the station below the dam, SSC increases and reaches a maximum, and then declines sharply. This phenomenon was found on the main-stem and several major tributaries of the upper Changjiang River. In the Minjiang River, where a series of dams were built successively, the response of SSC is more complicated. Copyright (C) 2010 John Wiley & Sons, Ltd.
[87]Xu J X.Complex response of channel fill-scour behavior to reservoir construction: An example of the upper Yellow River, China
. River Research and Applications, 2013, 29: 593-607.
https://doi.org/10.1002/rra.2558URLMagsci [本文引用: 1]摘要
<p>The influence of a reservoir on downstream hydrological regime and channel adjustment depends on the operational mode of the reservoir. The Liujiaxia and Longyangxia Reservoirs were completed in 1968 and 1985, respectively, both above Lanzhou. The former controls most suspended sediment supply from the drainage area above Lanzhou station, and the latter controls most runoff generated from the same area; the former has relatively small storage capacity and is used for interseasonal regulation of river flow, and the latter has much larger storage capacity and is used for multiannual regulation of river flow. Thus, the former changes sediment regime greatly, whereas the latter changes flow regime significantly. Of the runoff of the upper Yellow River, more than 95% comes from the drainage area above Lanzhou and less than 5% from below Lanzhou; of the sediment supply, 46% comes from the drainage area above Lanzhou and 56% from below Lanzhou, which cannot be regulated by the two reservoirs. Influenced by these factors, channel fill&ndash;scour behaviour after the reservoir construction exhibited a complex response, which can be separated as two stages. The response at the first stage was dominated by the Liujiaxia Reservoir and at the second by the Longyangxia Reservoir. The first stage of response can be generalized as follows: completion of the Liujiaxia Reservoir&thinsp;<img src="http://onlinelibrarystatic.wiley.com/undisplayable_characters/002192.gif" alt="[RIGHTWARDS ARROW]" />&thinsp;large quantity of sediment trapped&thinsp;<img src="http://onlinelibrarystatic.wiley.com/undisplayable_characters/002192.gif" alt="[RIGHTWARDS ARROW]" />&thinsp;downstream channel scour&thinsp;<img src="http://onlinelibrarystatic.wiley.com/undisplayable_characters/002192.gif" alt="[RIGHTWARDS ARROW]" />&thinsp;sediment trapping attenuating due to the decrease of storage capacity&thinsp;<img src="http://onlinelibrarystatic.wiley.com/undisplayable_characters/002192.gif" alt="[RIGHTWARDS ARROW]" />&thinsp;channel scour declining. The second stage of response can be generalized as follows: completion of the Longyangxia Reservoir&thinsp;<img src="http://onlinelibrarystatic.wiley.com/undisplayable_characters/002192.gif" alt="[RIGHTWARDS ARROW]" />&thinsp;significant reduction of high-flow season flow&thinsp;<img src="http://onlinelibrarystatic.wiley.com/undisplayable_characters/002192.gif" alt="[RIGHTWARDS ARROW]" />&thinsp;downstream river flow incapable of carrying sediment supplied below the dam&thinsp;<img src="http://onlinelibrarystatic.wiley.com/undisplayable_characters/002192.gif" alt="[RIGHTWARDS ARROW]" />&thinsp;downstream channel sedimentation enhanced. The changes induced by the two reservoirs occurred successively, and a cycle of complex response occurred during the river channel adjustment. Copyright &copy; 2012 John Wiley &amp; Sons, Ltd.</p>
[88]Shi Changxing, Fan Xiaoli, Shao Wenwei, et al.Channel change of the Inner Mongolian reach of the Yellow River and its causes
. Geographical Research, 2013, 32(5): 787-796.
https://doi.org/10.11821/yj2013050002URLMagsci [本文引用: 1]摘要
利用黄河内蒙段1962-2000年间4期大断面观测资料,计算了各期河床冲淤和河槽形态指标。发现从1962-2000年间前20年、中间9年及后9年,内蒙河段河槽500m<sup>2</sup>过水面积下河底高程发生了降低&mdash;升高&mdash;再升高的过程;河槽漫滩过水面积经历了升高&mdash;降低&mdash;再降低的过程,2000年只有1982年的大约一半;滩地经历了持续淤积过程,平均抬升0.25m;河槽宽深比值经历了变化不显著&mdash;增加&mdash;减小的过程。分析结果表明:气候变化、引水、水库拦沙和重点产沙支流来沙变化在河床冲淤和河床形态调整中作用较大;水库对径流的年内调节对1982年后河槽淤积贡献较大;来水来沙变化下河流多要素自动调整是造成河槽形态变化过程复杂的原因。
[师长兴, 范小黎, 邵文伟, . 黄河内蒙河段河床冲淤演变特征及原因
. 地理研究, 2013, 32(5): 787-796.]
https://doi.org/10.11821/yj2013050002URLMagsci [本文引用: 1]摘要
利用黄河内蒙段1962-2000年间4期大断面观测资料,计算了各期河床冲淤和河槽形态指标。发现从1962-2000年间前20年、中间9年及后9年,内蒙河段河槽500m<sup>2</sup>过水面积下河底高程发生了降低&mdash;升高&mdash;再升高的过程;河槽漫滩过水面积经历了升高&mdash;降低&mdash;再降低的过程,2000年只有1982年的大约一半;滩地经历了持续淤积过程,平均抬升0.25m;河槽宽深比值经历了变化不显著&mdash;增加&mdash;减小的过程。分析结果表明:气候变化、引水、水库拦沙和重点产沙支流来沙变化在河床冲淤和河床形态调整中作用较大;水库对径流的年内调节对1982年后河槽淤积贡献较大;来水来沙变化下河流多要素自动调整是造成河槽形态变化过程复杂的原因。
[89]Shi C X.Decadal trends and causes of sedimentation in the Inner Mongolia reach of the upper Yellow River, China
. Hydrological Processes, 2016, 30: 232-244.
[本文引用: 1]
[90]Xu J X.Response of land accretion of the Yellow River Delta to global climate change and human activity
. Quaternary International, 2008, 186: 4-11.
https://doi.org/10.1016/j.quaint.2007.08.032URL [本文引用: 1]摘要
In the past 50 years, influenced by global climate change, the Eastern Asian summer monsoon intensity (SMI) changed significantly, and that has led to some response in the water cycle system of the Yellow River basin and in the land accretion process of the delta. The variation in annual precipitation is synchronic with that in SMI. From 1950 to 1970, annual air temperature showed a slight decrease with large fluctuations. Since 1970, a significant increasing trend can be seen. Climate change may result in a change in sediment flux into the sea, and therefore in a change in the rate of land accretion of delta (R
[91]Xu Jiongin.Sediment transferring function of the lower reaches of the Yellow River influenced by drainage basin factors and human activities
. Science in China Series D: Earth Sciences, 2004, 34(8): 775-781.
[本文引用: 1]

[许炯心. 流域因素与人类活动对黄河下游河道输沙功能的影响
. 中国科学D辑: 地球科学, 2004, 34(8): 775-781.]
[本文引用: 1]
[92]Xu J X.Decreasing trend of sediment transfer function of the Upper Yellow River, China, in response to human activity and climate change
. Hydrological Sciences Journal, 2015, 60(2): 311-325.
https://doi.org/10.1080/02626667.2014.885655URL [本文引用: 1]摘要
An index (F-s) for sediment transfer function is introduced, based on the sediment budget at the channel scale. The purpose of this study is two-fold: to gain a deeper insight into how F-s is influenced by natural and human factors, and to provide some new knowledge for decision making in the management of the Upper Yellow River, China. Since 1960, the F-s of the Lanzhou to Toudaoguai reach of the Upper Yellow River shows a decreasing trend. At the drainage basin level, the decreased F-s can be explained by changes in precipitation and air temperature, as well as by a number of variables describing human activity, such as reservoir regulation, water diversion, and soil and water conservation. The higher temperature reduces the transfer function, while the larger runoff coefficient increases it. At the channel level, the decreased F-s can be explained by a number of variables of flow and sediment input. Three countermeasures for restoration of the F-s are suggested. [GRAPHICS] Editor Z.W. Kundzewicz
[93]Shi C X, Zhang D, You L Y.Changes in sediment yield of the Yellow River basin of China during the Holocene
. Geomorphology, 2002, 46: 267-283.
https://doi.org/10.1016/S0169-555X(02)00080-6URL [本文引用: 1]摘要
This research reconstructs the changes in sediment yield of the Yellow River based mainly on a large number of 14C dates collected from the literature. The total volume of sediment yield of the basin during the Holocene is estimated to be 8.0 10 12 tons. The annual sediment yield had an increasing trend over the Holocene from 0.68, 0.72, 0.79 to 1.01 10 9 tons over each 2500-year period from the early Holocene to the present. The changes in sediment yield are ascribed to both natural and anthropogenic reasons, in which the latter became important in the late Holocene. The mean rate of increase in natural sediment yield throughout the Holocene is estimated to be about 0.027 10 6 ton/year, and the natural annual sediment yield is projected to be 0.95 10 9 tons at the present. The increasing trend of natural sediment yield is reasoned to be the consequence of evolution of landforms, enhanced by tectonic movement and climatic change in the Loess Plateau, the principal sediment source of the river, towards a condition favorable to soil erosion. Comparing the estimated annual natural sediment yield with the current annual sediment load of 1.6 10 9 tons of the river, it is clear that human activities have augmented natural soil erosion by about 41% in the Yellow River basin. Furthermore, an estimate of the overall pattern of anthropogenic sediment yield shows an accelerated increasing trend, which is approximately correspondent with that of population in the Loess Plateau area. 2002 Elsevier Science B.V. All rights reserved.
[94]Shi Changxing. Sediment budget of the Yellow River over the period 1855-1968
. Journal of Sediment Research, 2003(2): 1-6.
URLMagsci摘要
通过对黄河上中游来沙量以及对下游和河口泥沙沉积量的估算,建立了1855年至1968年间黄河的泥沙平衡.结果显示,这期间上中游来沙为1 878×108t,其中淤积在下游的泥沙占62%,三角洲淤积占32%;下游淤积量随着大堤修建、大堤防洪能力提高、以及近期修建水库及引水引沙等人类活动的变化相应发生变化;三角洲淤积约有609×108 t,占河口来沙的比例为84%.
[师长兴. 1855年以来黄河泥沙输移系统的泥沙淤积分布分析
. 泥沙研究, 2003(2): 1-6.]
URLMagsci摘要
通过对黄河上中游来沙量以及对下游和河口泥沙沉积量的估算,建立了1855年至1968年间黄河的泥沙平衡.结果显示,这期间上中游来沙为1 878×108t,其中淤积在下游的泥沙占62%,三角洲淤积占32%;下游淤积量随着大堤修建、大堤防洪能力提高、以及近期修建水库及引水引沙等人类活动的变化相应发生变化;三角洲淤积约有609×108 t,占河口来沙的比例为84%.
[95]Shi C X, Zhang D D, You L Y.Sediment budget of the Yellow River Delta, China: The importance of dry bulk density and implications to understanding of sediment dispersal
. Marine Geology, 2003, 199(1/2): 13-25.
https://doi.org/10.1016/S0025-3227(03)00159-2URL摘要
This study constructs sediment budgets for the delta of the Yellow River, one of the world's largest muddy rivers, and, based on these budgets, discusses the characteristics and related mechanisms of sediment dispersal atthe river mouth. The sediment budgets are derived from quantifying deposits in the deltaic lobe formed at the Diaokouhe mouth of the river. A detailed investigation of the dry bulk density of deposits in the delta, which yields models of dry bulk density of deposits in the main depositional settings of the delta, guarantees the reliability of the sediment budgets. Results shore that deposits behind the delta front of the Diaokouhe lobe over the period of 1965 to 1974 account for 73.5% of the incoming sediment. The constructed sediment budgets reveal that the proportions of the deposits accumulated behind the delta front vary considerably over time. The main factor responsible for the variations is the change in sediment discharge of the river There is no evidence for the anticipated positive relationships between the proportion of sediment escaping from the delta and water discharge, clay content of incoming sediment, or mouth channel efficiency. The characteristics of sediment dispersal on the delta are related to the rapid extinction of sediment-charged hyperpycnal underflows, which are dominant in the plumes off the Yellow River mouth, and sediment deposition in the overbank flow on the delta plain because both of these processes trap a higher proportion of sediment at a higher sediment discharge.
[96]Shi Changxing, Xu Jiaqiang, Guo Lipeng, et al.Sedimentation in the lower reaches and sediment yield in the upper and middle reaches of the Yellow River in the past 2600 years
. Quaternary Sciences, 2009, 29(1): 116-125.
Magsci [本文引用: 1]摘要
<p>主要基于华北平原上93个钻孔中沉积物详细观测和分析数据,结合182组<sup>14</sup>C测年和埋深数据、参考前人黄河下游河道历史变迁及其他相关研究成果,估算出2600年以来黄河下游在602BC~11A.D.,11~1034A.D.,1034~1128A.D.,1128~1855A.D.和1855~1997A.D.等5个历史时期的年平均沉积量分别是3.89&times;10<sup>8t</sup>/a,2.24&times;10<sup>8t</sup>/a,6.63&times;10<sup>8t</sup>/a,6.78&times;10<sup>8t</sup>/a和8.47&times;10<sup>8t</sup>/a。通过建立黄河下游有无堤防和决溢频率与泥沙输移比的关系,计算出5个时期黄河上中游的平均年输沙量分别是6.2&times;10<sup>8t</sup>/a,6.8&times;10<sup>8t</sup>/a,8.3&times;10<sup>8t</sup>/a,11.5&times;10<sup>8t</sup>/a和15.3&times;10<sup>8t</sup>/a。进而探讨了黄河输沙量变化的主要原因,以及历史上王景治河后出现的600年安流时期的原因。</p>
[师长兴, 徐加强, 郭立鹏, . 近2600年来黄河下游沉积量和上中游产沙量变化过程
. 第四纪研究, 2009, 29(1): 116-125.]
Magsci [本文引用: 1]摘要
<p>主要基于华北平原上93个钻孔中沉积物详细观测和分析数据,结合182组<sup>14</sup>C测年和埋深数据、参考前人黄河下游河道历史变迁及其他相关研究成果,估算出2600年以来黄河下游在602BC~11A.D.,11~1034A.D.,1034~1128A.D.,1128~1855A.D.和1855~1997A.D.等5个历史时期的年平均沉积量分别是3.89&times;10<sup>8t</sup>/a,2.24&times;10<sup>8t</sup>/a,6.63&times;10<sup>8t</sup>/a,6.78&times;10<sup>8t</sup>/a和8.47&times;10<sup>8t</sup>/a。通过建立黄河下游有无堤防和决溢频率与泥沙输移比的关系,计算出5个时期黄河上中游的平均年输沙量分别是6.2&times;10<sup>8t</sup>/a,6.8&times;10<sup>8t</sup>/a,8.3&times;10<sup>8t</sup>/a,11.5&times;10<sup>8t</sup>/a和15.3&times;10<sup>8t</sup>/a。进而探讨了黄河输沙量变化的主要原因,以及历史上王景治河后出现的600年安流时期的原因。</p>
[97]Xu J X.Sedimentation rates in the lower Yellow River over the past 2300 years as influenced by human activities and climate change
. Hydrological Processes, 2003, 17(16): 3359-3371.
https://doi.org/10.1002/hyp.1392URL [本文引用: 1]摘要
Analysis of the sedimentary record has been used to determine the historical sedimentation rate in the lower Yellow River and the historical literature has been studied to obtain information on climate change and human activities. Based on the data obtained, the temporal variation in the sedimentation rate in the lower Yellow River over the past 2300 years has been studied in relation to climate change and the impact of human activities. The results indicate that the response of the sedimentation zone of Yellow River system to changes in the erosion zone are consistent with existing understanding. Changes in vegetation and land use, both related to climate change and human activities, are two major controls responsible for the increase in sedimentation rates. Additionally, the changing strategies for harnessing of the lower Yellow River are also responsible for such acceleration. With the trend of accelerated sedimentation in the past 2300 years, the period from the 7th to 10th centuries and the period since the mid-19th century have been identified as two periods in which abrupt changes occurred. Copyright
[98]Jin Desheng, Shi Changxing, Chen Hao, et al.Sediment disasters, their types and classification principles in drainage system
. Acta Geographica Sinica, 2002, 57(2) : 238-248.
Magsci [本文引用: 1]摘要
<p>泥沙灾害按驱动力、灾害发生的地貌学系统、灾害的表现形式及具体灾害系统,分层次逐级划分成自然动力与人为动力泥沙灾害2个灾列;流域水系,沟道坡面、河道及平原河口海岸4个泥沙灾害类;侵蚀型、输移(搬运)型、堆积型、复杂型及关联型5种泥沙灾害型;最后分别列出2系列的49个及54个灾种。这是一种比较综合、系统的分类原则和类型划分。从流水地貌、泥沙运动及灾害学相结合来看,泥沙灾害具有自然地理地带性、垂直分带性、群发性、继发性和周期性、渐发性和突发性,以及复杂性和非线性等特征。</p>
[金德生, 师长兴, 陈浩, . 流域系统的泥沙灾害类型及其划分原则
. 地理学报, 2002, 57(2): 238-248.]
Magsci [本文引用: 1]摘要
<p>泥沙灾害按驱动力、灾害发生的地貌学系统、灾害的表现形式及具体灾害系统,分层次逐级划分成自然动力与人为动力泥沙灾害2个灾列;流域水系,沟道坡面、河道及平原河口海岸4个泥沙灾害类;侵蚀型、输移(搬运)型、堆积型、复杂型及关联型5种泥沙灾害型;最后分别列出2系列的49个及54个灾种。这是一种比较综合、系统的分类原则和类型划分。从流水地貌、泥沙运动及灾害学相结合来看,泥沙灾害具有自然地理地带性、垂直分带性、群发性、继发性和周期性、渐发性和突发性,以及复杂性和非线性等特征。</p>
[99]Ni Jinren, Li Xiuxia, Xue An, et al.Sediment disaster chain and its applications to interpretation of disaster process characteristics related to sediment transport
. Journal of Natural Disasers, 2004, 13(5): 1-9.
https://doi.org/10.3969/j.issn.1004-4574.2004.05.001URL [本文引用: 1]摘要
泥沙灾害是地球表层的主要灾害 之一。泥沙灾害具有链锁式反应机制,在一定条件下构成泥沙灾害链。阐述了泥沙灾害链的概念、特点及类型,并以黄河与长江流域的泥沙灾害为例,对其链式特征 进行了深入分析。研究表明,泥沙灾害链是泥沙灾害过程的主要表现形式之一,反映了泥沙灾害中隐含的渐发特征和强次生灾害特征,泥沙灾害链是研究泥沙灾害过 程规律和特征的重要基础。
[倪晋仁, 李秀霞, 薛安, . 泥沙灾害链及其在灾害过程规律研究中的应用
. 自然灾害学报, 2004, 13(5): 1-9.]
https://doi.org/10.3969/j.issn.1004-4574.2004.05.001URL [本文引用: 1]摘要
泥沙灾害是地球表层的主要灾害 之一。泥沙灾害具有链锁式反应机制,在一定条件下构成泥沙灾害链。阐述了泥沙灾害链的概念、特点及类型,并以黄河与长江流域的泥沙灾害为例,对其链式特征 进行了深入分析。研究表明,泥沙灾害链是泥沙灾害过程的主要表现形式之一,反映了泥沙灾害中隐含的渐发特征和强次生灾害特征,泥沙灾害链是研究泥沙灾害过 程规律和特征的重要基础。
[100]Ni Jinren, Qian Zhenghan.On the functional blocking the flow of the Yellow River
. Science in China (Series E), 2002, 32(4): 496-502.
[本文引用: 1]

[倪晋仁, 钱征寒. 论黄河功能性断流
. 中国科学: E辑, 2002, 32(4): 496-502.]
[本文引用: 1]
[101]Numerical simulation of flows in dam breach development of the Tangjiashan Lake formed by Wenchuan Earthquake in China. Chinese Science Bulletin, 2008, 53(24): 3127-3133.URL [本文引用: 1]摘要
"5.12"汶川特大地震造成了重大人员伤亡和财产损失,而山体滑坡形成的堰塞湖不稳定而易于发生溃决,造成洪水灾害,是震后急需防御的次生灾害重点和难点.除了大量的现场勘测外,对泄流及堰塞体冲刷过程的研究,是制定下游避险、抢险方案的关键.清华大学水沙科学与水利水电工程国家重点实验室曾为规模最大、威胁最严重的唐家山堰塞湖抢险提供了及时的技术支持,本文是部分工作的总结.针对唐家山堰塞湖特定的泄流动力学过程,开发了平面二维水沙数学模型,扩展了基本方程,考虑了堰塞体形成的河床变形对水流运动的影响,提出了高精度且高效率的边界跟踪算法,分析了堰塞湖泄流过程以及堰塞体冲刷发展的机制.结果表明,河床变形对泄流影响较大,堰塞体以溯源冲刷为主,计算得到的泄流流量、堰塞湖水位与实际观测值吻合较好,这些结果已经很好地服务于唐家山堰塞湖下游应对方案的确定.
[王光谦, 钟德钰, 张红武, . 汶川地震唐家山堰塞湖泄流过程的数值模拟
. 科学通报, 2008, 53(24): 3127-3133.
URL [本文引用: 1]摘要
"5.12"汶川特大地震造成了重大人员伤亡和财产损失,而山体滑坡形成的堰塞湖不稳定而易于发生溃决,造成洪水灾害,是震后急需防御的次生灾害重点和难点.除了大量的现场勘测外,对泄流及堰塞体冲刷过程的研究,是制定下游避险、抢险方案的关键.清华大学水沙科学与水利水电工程国家重点实验室曾为规模最大、威胁最严重的唐家山堰塞湖抢险提供了及时的技术支持,本文是部分工作的总结.针对唐家山堰塞湖特定的泄流动力学过程,开发了平面二维水沙数学模型,扩展了基本方程,考虑了堰塞体形成的河床变形对水流运动的影响,提出了高精度且高效率的边界跟踪算法,分析了堰塞湖泄流过程以及堰塞体冲刷发展的机制.结果表明,河床变形对泄流影响较大,堰塞体以溯源冲刷为主,计算得到的泄流流量、堰塞湖水位与实际观测值吻合较好,这些结果已经很好地服务于唐家山堰塞湖下游应对方案的确定.
[102]Xu J X.Sediment jamming of a trunk stream by hyperconcentrated floods from small tributaries: Case of the Upper Yellow River, China
. Hydrological Sciences Journal, 2015, 61(10). doi: 10.1080/02626667.2015.1055272.
URL [本文引用: 1]摘要
AbstractThe tributary–trunk stream relationship is investigated with respect to hyperconcentrated flows and coupled wind–water processes in the Yellow River, China. Ten small tributaries that drain only 3% of the total drainage area of the trunk stream transport large amounts of relatively coarse sediment from the desert to the trunk stream during hyperconcentrated floods. The resultant strong sedimentation often jams the trunk stream, leading to serious disasters. This study reveals the cause of this interesting phenomenon and proposes countermeasures for disaster reduction. A typical sediment-jamming event in July 1989 was thoroughly analysed based on the observational data, including the beginning, development, and final stages of the event. An index of the geomorphorphogic effectiveness of the tributary on the trunk stream and a number of indices describing SJEs and the influencing factors are adopted, based on which a discrimination relationship for the occurrence of SJEs is established and some stat...
[103]Wu Jishan, Wang Chenghua.The development trend of the mountain hazards research and the task
. Journal of Mountain Science, 2006, 4(5): 518-524.
https://doi.org/10.3969/j.issn.1008-2786.2006.05.002URL [本文引用: 1]摘要
泥石流、滑坡等山地灾害已成为世界各国十分关注的自然灾害问题。据最近几年的国际学术会议。泥石流、滑坡研究的前沿领域是:泥石流、滑坡活动的地带性与全球气候变化的规律;泥石流、滑坡起动机理、动力学模型;泥石流、滑坡等山地灾害风险分析、发生时间预报;成灾机理与减灾防灾关键技术。国内研究较晚,但发展很快。经过近50a的研究,涉及上述诸多研究领域。但研究不深,还存在不少差距。据国内外研究态势,针对山地所实际,提出了在泥石流、滑坡理论创新和防治关键技术等研究方面12条任务。
[吴积善, 王成华. 山地灾害研究的发展态势与任务
. 山地学报, 2006, 4(5): 518-524.]
https://doi.org/10.3969/j.issn.1008-2786.2006.05.002URL [本文引用: 1]摘要
泥石流、滑坡等山地灾害已成为世界各国十分关注的自然灾害问题。据最近几年的国际学术会议。泥石流、滑坡研究的前沿领域是:泥石流、滑坡活动的地带性与全球气候变化的规律;泥石流、滑坡起动机理、动力学模型;泥石流、滑坡等山地灾害风险分析、发生时间预报;成灾机理与减灾防灾关键技术。国内研究较晚,但发展很快。经过近50a的研究,涉及上述诸多研究领域。但研究不深,还存在不少差距。据国内外研究态势,针对山地所实际,提出了在泥石流、滑坡理论创新和防治关键技术等研究方面12条任务。
[104]Wu Jishan, Cheng Zunlan, Geng Xueyong.Investigation on the yield mechanism of viscous debris flows
. Journal of Sediment Research, 2007(2): 17-23.
URLMagsci [本文引用: 1]摘要
粘性泥石流产流是斜坡或沟床中粘粒含量较高的松散土体与入渗为主的水体结合,产生容重和起始静力分别大于1.8~1.9t/m3和30Pa的土水混合流.产流包括两个紧密相连的过程:含水量饱和或局部饱和土体的起动过程;动起后的流体化过程.本文首先阐述粘性泥石流产流的4种理想化情况及其相应的公式和4类流体化方式;然后结合泥石流活动的实际状况,提出粘性泥石流产流的4种常见类型,从而综合探讨粘性泥石流的产流机理.
[吴积善, 程尊兰, 耿学勇. 粘性泥石流产流机理探讨
. 泥沙研究, 2007(2): 17-23.]
URLMagsci [本文引用: 1]摘要
粘性泥石流产流是斜坡或沟床中粘粒含量较高的松散土体与入渗为主的水体结合,产生容重和起始静力分别大于1.8~1.9t/m3和30Pa的土水混合流.产流包括两个紧密相连的过程:含水量饱和或局部饱和土体的起动过程;动起后的流体化过程.本文首先阐述粘性泥石流产流的4种理想化情况及其相应的公式和4类流体化方式;然后结合泥石流活动的实际状况,提出粘性泥石流产流的4种常见类型,从而综合探讨粘性泥石流的产流机理.
[105]Xie Hong, Zhong Dunlun, Wei Fangqiang, et al.Debris flow hazards and their formation causes in mountain urban area of China
. Journal of Mountain Science, 2006, 24(1): 79-87.
[本文引用: 1]

[谢洪, 钟敦伦, 韦方强, . 我国山区城镇泥石流灾害及其成因
. 山地学报, 2006, 24(1): 79-87.]
[本文引用: 1]
[106]Wu Jishan, Zhang Jun, Cheng Zunlan, et al.Relation and its determination of residual layer and depth of viscous debris flows
. Journal of Sediment Research, 2003(6): 7-12.
URLMagsci [本文引用: 1]摘要
粘性泥石流泥深是否包括残留层,一直存在着是与否二种观点和相应的二种观测值,其中大多数观测值不包括残留层.通过观测和试验,尤其原型观测表明,在后继粘性泥石流作用下,除底部很薄的一层不动外,残留层是运动的,泥深应该包含残留层厚度,对过去不包括残留层的泥深观测值应予更正,但各泥石流观测站过去均没有残留层及其不动层厚度的观测值.为此作者提出了用当时均有观测值的泥石流容重和沟床比降等计算残留层厚度的方法,以及不动层的处理意见,以确定当时泥深,使宝贵的观测值可继续应用.
[吴积善, 张军, 程尊兰, . 粘性泥石流的泥深与残留层关系及其确定
. 泥沙研究, 2003(6): 7-12.]
URLMagsci [本文引用: 1]摘要
粘性泥石流泥深是否包括残留层,一直存在着是与否二种观点和相应的二种观测值,其中大多数观测值不包括残留层.通过观测和试验,尤其原型观测表明,在后继粘性泥石流作用下,除底部很薄的一层不动外,残留层是运动的,泥深应该包含残留层厚度,对过去不包括残留层的泥深观测值应予更正,但各泥石流观测站过去均没有残留层及其不动层厚度的观测值.为此作者提出了用当时均有观测值的泥石流容重和沟床比降等计算残留层厚度的方法,以及不动层的处理意见,以确定当时泥深,使宝贵的观测值可继续应用.
[107]Wu Jishan, Cheng Zunlan.Formation of dam from debris flow in the Southeast Tibet
. Journal of Sediment Research, 2005, 23(4): 399-405.
https://doi.org/10.3969/j.issn.1008-2786.2005.04.003URL [本文引用: 1]摘要
西藏东南部山高谷深,冰川发育,冰碛等松散堆积物厚度大,经常发生大型或特大型泥石流堵断主河,形成堵塞坝.本文针对西藏东南部4条典型泥流沟所发生的7次大型或特大型泥石流中,有5次形成堵塞坝,来剖析泥石流堵塞坝形成的机理和主要因素.提出由于冰雪崩、冰湖溃决或大规模滑坡活动,所激发的首阵或前几阵大流量、高速度、多巨砾,并与主河正交的粘性泥石流,最容易形成堵塞坝.
[吴积善, 程尊兰. 西藏东南部泥石流堵塞坝的形成机理
.山地学报, 2005, 23(4): 399-405.]
https://doi.org/10.3969/j.issn.1008-2786.2005.04.003URL [本文引用: 1]摘要
西藏东南部山高谷深,冰川发育,冰碛等松散堆积物厚度大,经常发生大型或特大型泥石流堵断主河,形成堵塞坝.本文针对西藏东南部4条典型泥流沟所发生的7次大型或特大型泥石流中,有5次形成堵塞坝,来剖析泥石流堵塞坝形成的机理和主要因素.提出由于冰雪崩、冰湖溃决或大规模滑坡活动,所激发的首阵或前几阵大流量、高速度、多巨砾,并与主河正交的粘性泥石流,最容易形成堵塞坝.
[108]Jin Desheng.A study on fluvial dynamic geomorphology and its experiments and simulations
. The Journal of Chinese Geography, 1995, 5(3): 55-68.
URL [本文引用: 1]
[109]Jin Desheng.On several issues of research on the experiment and simulation for geomorphic processes//Geomorphology and Quaternary Professional Committee, Geographical Society of China. Processes and Environment in Geomophology. Beijing: Seismological Press, 1995: 289-295. [本文引用: 1]

[金德生. 地貌过程实验模拟研究若干问题//中国地理学会地貌与第四纪专业委员会. 地貌过程与环境文集. 北京: 地震出版社, 1995: 289-295.] [本文引用: 1]
[110]Jin Desheng, Chen Hao, Guo Qingwu.A preliminary experimental study on non-linear relation of sediment yield to drainage network development
. International Journal of Sediment Research, 1999, 14(2): 9-18.
https://doi.org/10.1109/GCIS.2009.31URL [本文引用: 1]
[111]Jin Desheng, Chen Hao, Guo Qingwu.A preliminary experimental study on non-linear relation of sediment yield to drainage network development
. Acta Geographica Sinica, 2000, 55(4): 439-448.
https://doi.org/10.3321/j.issn:0375-5444.2000.04.006URL摘要
在 35.56mm/ h·cm2定雨强的人工降雨条件下 ,组成物质中径分别为 0 .0 2 1 mm、 0 .0 66mm及 0 .0 76mm的流域发育对比实验表明 ,产沙过程具有波动振荡衰减特征 ;水系发育以增加河道 (沟道 )数目及弯曲拉伸长度两种方式进行最小消能。水系分形维数正是这种消能的量度。水系分数维值随时间呈不对称上凹型曲线。对比分析表明 :产沙过程的振荡性、衰减率 ,随物质变粗而加强 ,水系河道数目随物质变细而增多 ,河道随物质变细拉长 ,分数维值与产沙间是不对称双曲线的非线性关系。曲线的递变率绝对值随时间推移和物质变细而变小 ,体现状况代替时间特征。
[金德生, 陈浩, 郭庆伍. 流域物质组成对水系发育与产沙间非线性关系影响的实验研究,
地理学报, 2000, 55(4): 439-448.]
https://doi.org/10.3321/j.issn:0375-5444.2000.04.006URL摘要
在 35.56mm/ h·cm2定雨强的人工降雨条件下 ,组成物质中径分别为 0 .0 2 1 mm、 0 .0 66mm及 0 .0 76mm的流域发育对比实验表明 ,产沙过程具有波动振荡衰减特征 ;水系发育以增加河道 (沟道 )数目及弯曲拉伸长度两种方式进行最小消能。水系分形维数正是这种消能的量度。水系分数维值随时间呈不对称上凹型曲线。对比分析表明 :产沙过程的振荡性、衰减率 ,随物质变粗而加强 ,水系河道数目随物质变细而增多 ,河道随物质变细拉长 ,分数维值与产沙间是不对称双曲线的非线性关系。曲线的递变率绝对值随时间推移和物质变细而变小 ,体现状况代替时间特征。
[112]Jin Desheng, Guo Qingwu.Experiment on processes of landform evolution of watersheds with homogeneous materials //Geomorphic Experiment and Simulation. Beijing: Seismological Press, 1995.URL [本文引用: 1]

[金德生, 郭庆伍. 均质流域地貌发育过程实验研究//地貌实验与模拟. 北京: 地震出版社, 1995.]URL [本文引用: 1]
[113]Jin Desheng, Chen Hao, Zhang Ouyang, et al.Base level lowering to non-linear relationship between sediment yield and drainage network development:an experimental analysis
. Geographical Research, 2003, 25(2): 560-570.
https://doi.org/10.3321/j.issn:1000-0585.2003.05.004URL [本文引用: 1]摘要
在35.56mm/hr*cm2定雨强的人工降雨条件下,组成物 质中径为0.021mm,侵蚀基准面两次下降的流域发育对比实验表明,水系发育以增加河道(沟道)数目及流域出口段河道下切、溯源侵蚀延伸长度两种方式进 行最小消能,产沙过程具有明显的复杂响应特征.流域侵蚀产沙与水系分形维数间存在显著的非线性特征,分数维值与产沙量间呈不对称双曲线的关系.侵蚀基面下 降导致流域势能的相对增大,在消能过程中,第一次基面下降带来的影响比第二次基面下降带来的影响要显著,在空间上,其影响随远离流域出口而减弱.
[金德生, 陈浩, 张欧阳, . 侵蚀基准面下降对水系发育与产沙间非线性关系影响的实验分析
. 地理研究, 2003, 25(2): 560-570.]
https://doi.org/10.3321/j.issn:1000-0585.2003.05.004URL [本文引用: 1]摘要
在35.56mm/hr*cm2定雨强的人工降雨条件下,组成物 质中径为0.021mm,侵蚀基准面两次下降的流域发育对比实验表明,水系发育以增加河道(沟道)数目及流域出口段河道下切、溯源侵蚀延伸长度两种方式进 行最小消能,产沙过程具有明显的复杂响应特征.流域侵蚀产沙与水系分形维数间存在显著的非线性特征,分数维值与产沙量间呈不对称双曲线的关系.侵蚀基面下 降导致流域势能的相对增大,在消能过程中,第一次基面下降带来的影响比第二次基面下降带来的影响要显著,在空间上,其影响随远离流域出口而减弱.
[114]Xu Weiqun, Ni Jinren, Xu Haipeng, et al.Experimental study on erosion process over loess slopes (I): Surface flow and sediment transport
. Journal of Soil and Water Conservation, 1995, 9(4): 9-28.
URL [本文引用: 1]摘要
黄土坡地坡面侵蚀过程包括降雨过程中的产流产沙过程以及相应的坡面形态变化过程,该文主要研究产流产沙过程。在对国内外已有同类成果分析的基础上,为了弥补现有成果的一些不足之处,设计了室内黄土坡面侵蚀模拟实验。实验分10个组次对产流、渗流、产沙、沟道发育、沟与坡的侵蚀过程及其坡蚀量、沟蚀量、侵蚀过程中的微地貌现象直至坡形变化进行了详细测量与观察,获得了大量实测数据。关于坡面形态变化的讨论将在后文②展开。本文及后文 ̄[1]中论述的实验结果不仅初步揭示了黄土坡面侵蚀过程中上述要素的变化机理,而且也为今后在这方面进行定量化研究提供了精度较高的实测资料。
[徐为群, 倪晋仁, 徐海鹏, . 黄土面坡侵蚀过程实验研究: 产流产沙过程
. 水土保持学报, 1995, 9(4): 9-28.]
URL [本文引用: 1]摘要
黄土坡地坡面侵蚀过程包括降雨过程中的产流产沙过程以及相应的坡面形态变化过程,该文主要研究产流产沙过程。在对国内外已有同类成果分析的基础上,为了弥补现有成果的一些不足之处,设计了室内黄土坡面侵蚀模拟实验。实验分10个组次对产流、渗流、产沙、沟道发育、沟与坡的侵蚀过程及其坡蚀量、沟蚀量、侵蚀过程中的微地貌现象直至坡形变化进行了详细测量与观察,获得了大量实测数据。关于坡面形态变化的讨论将在后文②展开。本文及后文 ̄[1]中论述的实验结果不仅初步揭示了黄土坡面侵蚀过程中上述要素的变化机理,而且也为今后在这方面进行定量化研究提供了精度较高的实测资料。
[115]Zhang Ouyang, Jin Desheng, Chao Hao.An experimental study on spatial and temporal processes and complex response of river channel evolution
. Geographical Research, 2000, 19(2): 180-188.
Magsci [本文引用: 1]摘要
运用过程响应模型实验方法,在游荡型模型小河塑造过程中,分析了游荡河型发育过程中出现的时间和空间演变过程,发现其时、空演替过程可以相互替代,从而在实验室内证实了空代时假说的存在性,为空代时假说提供了新的证据。并据此把复杂响应过程分为时间复杂响应过程和空间复杂响应过程,分析了游荡河型发育过程中出现的时空复杂响应现象。
[张欧阳, 金德生, 陈浩. 游荡河型造床实验过程中河型的时空演替和复杂响应现象
. 地理研究, 2000, 19(2): 180-188.]
Magsci [本文引用: 1]摘要
运用过程响应模型实验方法,在游荡型模型小河塑造过程中,分析了游荡河型发育过程中出现的时间和空间演变过程,发现其时、空演替过程可以相互替代,从而在实验室内证实了空代时假说的存在性,为空代时假说提供了新的证据。并据此把复杂响应过程分为时间复杂响应过程和空间复杂响应过程,分析了游荡河型发育过程中出现的时空复杂响应现象。
[116]Wang Suiji, Bo Junli.Experimental simulation of anastomosing multiple channel formation
. Progress in Geography, 2004, 23(3): 34-42.
https://doi.org/10.11820/dlkxjz.2004.03.005Magsci [本文引用: 1]摘要
<p>网状河流是受到人们关注的新型冲积河流,其水文特征、地貌特征和沉积特征已经不同程度地被揭示。然而,网状河流的水槽实验迄今仍是空白,而水槽模拟实验是在时间和空间都大大缩小之后的自然界河流演变过程的再现。本文报道的是在实验水槽中通过原河道决口后网状河流的发生和演变过程。实验初始条件为:水槽辅助区的待决口河道,目标区为轴部略微下凹的长方形泛滥平原(4.5 m&times;16.5 m),其上下层分别为1.5 cm厚、中值粒径为0.0132 mm的高岭土层和0.5 m厚、中值粒径为0.188mm的天然细砂层,从5.5 m~17 m区段的平均纵比降为0.0058,17m ~22 m区段的平均纵比降为0.0077。采用的定常流量为3 L/s,悬移质输沙量在前3小时为4.5g/min,其后为1.2 g/s。实验总历时50小时。实验初期,目标区的上游段以垂向加积作用为主,中游以随机侵蚀为主,下游以溯源侵蚀为主,在13.5小时左右,相互连通的多重河道的网状河流体系的雏形基本展现。此后至25.5小时,网状河道的演变以下蚀为主演变为以适度的侧蚀,但河岸的后退幅度很小,标志网状河道逐步过渡到成熟期。从25.5小时至50小时,个别河道的局部废弃和决口是该成熟期网状河道演变的新特点。实验成功地模拟了天然网状河流的形成、发展和演变过程,同时也证明了它是不同于分汊河流的河型。这不但是网状河流形成和演变过程的水槽模拟的有益尝试,而且有助于人们进一步认识网状河流的河性。</p>
[王随继, 薄俊丽. 网状河流多重河道形成过程的实验模拟
. 地理科学进展, 2004, 23(3): 34-42.]
https://doi.org/10.11820/dlkxjz.2004.03.005Magsci [本文引用: 1]摘要
<p>网状河流是受到人们关注的新型冲积河流,其水文特征、地貌特征和沉积特征已经不同程度地被揭示。然而,网状河流的水槽实验迄今仍是空白,而水槽模拟实验是在时间和空间都大大缩小之后的自然界河流演变过程的再现。本文报道的是在实验水槽中通过原河道决口后网状河流的发生和演变过程。实验初始条件为:水槽辅助区的待决口河道,目标区为轴部略微下凹的长方形泛滥平原(4.5 m&times;16.5 m),其上下层分别为1.5 cm厚、中值粒径为0.0132 mm的高岭土层和0.5 m厚、中值粒径为0.188mm的天然细砂层,从5.5 m~17 m区段的平均纵比降为0.0058,17m ~22 m区段的平均纵比降为0.0077。采用的定常流量为3 L/s,悬移质输沙量在前3小时为4.5g/min,其后为1.2 g/s。实验总历时50小时。实验初期,目标区的上游段以垂向加积作用为主,中游以随机侵蚀为主,下游以溯源侵蚀为主,在13.5小时左右,相互连通的多重河道的网状河流体系的雏形基本展现。此后至25.5小时,网状河道的演变以下蚀为主演变为以适度的侧蚀,但河岸的后退幅度很小,标志网状河道逐步过渡到成熟期。从25.5小时至50小时,个别河道的局部废弃和决口是该成熟期网状河道演变的新特点。实验成功地模拟了天然网状河流的形成、发展和演变过程,同时也证明了它是不同于分汊河流的河型。这不但是网状河流形成和演变过程的水槽模拟的有益尝试,而且有助于人们进一步认识网状河流的河性。</p>
[117]Jin D S, Chao H, Zhang O Y.An experimental study on bed-making and catastrophic processes in island braided channel
. International Journal of Sediment Research, 1997, 12(3): 225-239.
URL [本文引用: 1]摘要
LINTRODUCTIONAstudyonevolutionandpredictionofthefluvialgeomorphicsystemhasdevelopedinthe1970's(Scheideggef,1975),andisstillapplied.Fromthemiddleofthe1980'son,researchofcatastrophicprocessesinthefluvialgeomorphicSystem(catatrophism,hazards)hasbeenfocusedo
[118]Zhang O Y, Jin D S, Chao H.An experimental study on temporal and spatial processes of wandering-braided river channel evolution,
International Journal of Sediment Research, 1999, 14(2): 31-38.
URL
[119]Jin Desheng, Zhang Ouyang, Chao Hao, et al.Analysis of thalweg evolution tendency of the wandering reach in the Lower Yellow River after Xiaolangdi Reservoir executing
. Journal of Sediment Research, 2000(6): 52-62.
https://doi.org/10.1007/BF02948846URL [本文引用: 1]摘要
本文借助地貌类比方法及时空复杂响应 ,采用深泓指数及河床起伏度 ,分析了三门峡水库运用后 (196 0~ 196 4年 )黄河下游游荡段的深泓演变情况。预测了小浪底水库修建后 ,清水下泄运用阶段时 ,下游游荡性河段将 :(1)沿程深泓基本保持居中偏右趋势 ,(2 )深泓位移具有时空复杂响应过程 ,(3)游荡程度降低 ,局部河段暂时向微弯发展。因此 ,必须采取“控导主溜 ,稳定险工” ,才能维护良性微弯河势 ,遏制回返向恶性游荡发展。
[金德生, 张欧阳, 陈浩, . 小浪底水库运用后黄河下游游荡性河段深泓演变趋势分析
. 泥沙研究, 2000(6): 52-62.]
https://doi.org/10.1007/BF02948846URL [本文引用: 1]摘要
本文借助地貌类比方法及时空复杂响应 ,采用深泓指数及河床起伏度 ,分析了三门峡水库运用后 (196 0~ 196 4年 )黄河下游游荡段的深泓演变情况。预测了小浪底水库修建后 ,清水下泄运用阶段时 ,下游游荡性河段将 :(1)沿程深泓基本保持居中偏右趋势 ,(2 )深泓位移具有时空复杂响应过程 ,(3)游荡程度降低 ,局部河段暂时向微弯发展。因此 ,必须采取“控导主溜 ,稳定险工” ,才能维护良性微弯河势 ,遏制回返向恶性游荡发展。
[120]Jin Desheng, Chao Hao, Guo Qingwu.An experimental study on non-linear longitudinal profiles
. Acta Geographica Sinica, 1997, 52(2): 154-162.
https://doi.org/10.11821/xb199702008URL [本文引用: 1]摘要
混沌-分形研究是非线性地貌发育理论,尤其是非线性流水地貌学研究的前沿问题,是当代地貌学深层次研究的一个重要界面,在国内外刚刚起步。本文在概述国内外研究进展基础上,以黄河下游及长江中下游为例,运用粗视化方法,对不同河段、不同河型的河床深泓纵剖面进行了分维量计和检验。初步分析表明,冲积河流的河道纵剖面具有分维特征,可用来刻划河流纵剖面发育的复杂程度,结合河床起伏度的统计对比分析,可将其作为河流纵向消能的另一种量度。河流纵剖面的分维具有时空变化,其微小变化可以体现河型在时空上的分异和偏离。分维数值与某些环境因素及水力条件有关,如分维数值D与河床纵坡降J呈负相关。因此,可作为河型演变分析依据的佐证,预测河流纵剖面的发育趋势。
[金德生, 陈浩, 郭庆伍. 河道纵剖面分形—非线性形态特征
. 地理学报, 1997, 52(2): 154-162.]
https://doi.org/10.11821/xb199702008URL [本文引用: 1]摘要
混沌-分形研究是非线性地貌发育理论,尤其是非线性流水地貌学研究的前沿问题,是当代地貌学深层次研究的一个重要界面,在国内外刚刚起步。本文在概述国内外研究进展基础上,以黄河下游及长江中下游为例,运用粗视化方法,对不同河段、不同河型的河床深泓纵剖面进行了分维量计和检验。初步分析表明,冲积河流的河道纵剖面具有分维特征,可用来刻划河流纵剖面发育的复杂程度,结合河床起伏度的统计对比分析,可将其作为河流纵向消能的另一种量度。河流纵剖面的分维具有时空变化,其微小变化可以体现河型在时空上的分异和偏离。分维数值与某些环境因素及水力条件有关,如分维数值D与河床纵坡降J呈负相关。因此,可作为河型演变分析依据的佐证,预测河流纵剖面的发育趋势。
[121]Qiao Yunfeng, Jin Desheng, Yang Lihu, et al. An experimental study on the response of alluvial braided-meandering river to uplift and subsidence with non-uniform movement
. Progress in Geography, 2016, to be published.
[本文引用: 1]

[乔云峰, 金德生, 杨丽虎, . 游荡—弯曲过渡性冲积河流对隆起与坳陷非均匀沉降响应的实验研究
. 地理科学进展, 2016, 待刊.]
[本文引用: 1]
[122]Church M, Ferguson R I.Morphodynamics: Rivers beyond steady state
. Water Resources Research, 2015, 51: 1883-1897. doi: 10.1002/2014WR016862.
URL [本文引用: 1]摘要
The morphology of an alluvial river channel affects the movement of water and sediment along it, but in the longer run is shaped by those processes. This interplay has mostly been investigated empirically within the paradigm of Newtonian mechanics. In rivers, this has created an emphasis on equilibrium configurations with simple morphology and uniform steady flow. But transient adjustment, whether between equilibrium states or indefinitely, is to be expected in a world in which hydrology, sediment supply, and base level are not fixed. More fundamentally, water flows and all the phenomena that accompany them are inherently unsteady, and flows in natural channels are characteristically nonuniform. The morphodynamics of alluvial river channels is the striking consequence. In this paper, we develop the essential connection between the episodic nature of bed material transport and the production of river morphology, emphasizing the fundamental problems of sediment transport, the role of bar evolution in determining channel form, the role of riparian vegetation, and the wide range of time scales for change. As the key integrative exercise, we emphasize the importance of physics-based modeling of morphodynamics. We note consequences that can be of benefit to society if properly understood. These include the possibility to better be able to model how varying flows drive morphodynamic change, to understand the influence of the sediments themselves on morphodynamics, and to recognize the inherent necessity for rivers that transport bed material to deform laterally. We acknowledge pioneering contributions in WRR and elsewhere that have introduced some of these themes.
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