活动造山带地区基岩河道宽度控制因素及其对地貌演化指示意义

doi:10.3969/j.issn.0253-4967.20250002

摘要/Abstract

摘要：

活动造山带地貌演化是构造抬升与侵蚀作用竞争的结果, 河流作为关键营力, 其形态调整可反映区域构造活动与气候变化信息。传统研究聚焦于河流坡度对构造扰动的响应, 而河道宽度作为水力系统的另一重要参数, 其控制因素及地貌指示意义尚未充分揭示。基岩河道宽度是揭示构造-侵蚀相互作用与地貌演化过程的关键参数, 近年来逐渐成为地貌学研究的热点。文中系统地综述了水力几何模型、侵蚀动力学理论与全球典型案例研究, 重点讨论了基岩河道宽度的控制因素(河床可蚀性、构造变形、沉积物效应及气候变化等)。综合现有研究可以发现: 1)河床可蚀性是控制宽度的核心内在因素, 岩体强度与节理密度通过影响侵蚀机制(磨蚀或拔蚀)调控河道形态: 高抗侵蚀性基岩区河流收缩变窄, 陡峭度增加; 软弱或破碎岩层则促进侧蚀, 形成宽浅河谷。2)构造变形通过隆升速率变化驱动河道形态调整: 在高隆升速率区, 河流通过收缩宽度集中水流剪切力, 加速下切以平衡抬升; 而在低隆升区则以拓宽河道削弱侵蚀能力。3)沉积物供给的双重效应显著影响宽度响应: 具有充足沉积物覆盖的河床抑制下切但增强侧蚀, 而低沉积物供给则使能量集中于基底侵蚀, 形成窄深河道。4)极端气候事件通过洪水流量剧变和沉积物脉冲输入, 触发河道宽度短期调整, 长期则通过侵蚀基准面变化影响形态演化。由此可见, 当前研究仍存在多因素耦合机制不明、定量模型普适性不足等问题, 未来需结合高分辨率遥感、数值模拟与年代学数据, 深化宽度参数在地貌演化模型中的应用, 为造山带构造-气候相互作用研究提供新视角。

关键词: 河道宽度, 水力侵蚀模型, 瞬态地貌, 河流地貌

Abstract:

Fluvial erosion of bedrock channels plays a crucial role in controlling denudation rates in orogenic belts. Dynamic adjustment of bedrock channels in response to perturbations such as tectonic and climatic events controls the mechanisms and pace of regional geomorphic evolution. Fluvial systems generally evolve toward a steady state, adjusting their channel geometry to maintain a stable erosion rate. However, variations in tectonic activity, channel substrate strength, and sediment cover can cause fluvial systems to deviate from this equilibrium state. In response to those disturbances, fluvial systems modify their stream power by altering their geometry. Thus, channel morphology is vital for revealing the processes of geomorphic evolution and their control mechanisms. Stream power incision model is the base for quantitative studies of how fluvial systems adapt to tectonic, climatic, and lithological changes. Channel slope and channel width are the two most commonly used parameters to determine the state of channel stream power. Channel slope influences the rate of stream power dissipation along the downstream direction, while river width dictates the distribution of stream power across the channel bed. A reduction in channel width can concentrate stream energy, thereby promoting downcutting. Previous studies that have used fluvial geomorphology to infer tectonic and climatic information have largely focused on changes of channel slope, often overlooking the critical role of channel width. And the controlling factors and geomorphic indications of channel width, another important parameter of the hydraulic system, have not been fully revealed. Bedrock channel width is a key parameter for revealing the tectonic-erosional interaction and the geomorphologic evolution process, and has gradually become a hot spot in geomorphologic research in recent years. This paper addresses this gap by exploring how variations in channel width in response to external perturbations contribute to geomorphological evolution. In this paper, we provide a systematic review of hydraulic geometry modelling, erosion dynamics theory and global case studies, focusing on the factors controlling the width of bedrock channels(bed erodibility, tectonic deformation, sediment effects, and climate change, etc.). The synthesis of existing studies reveals that: 1)Bed erodibility is the core intrinsic factor controlling channel width, and rock mass strength and joint density regulate channel morphology by influencing the erosion mechanism(abrasion/abrasion): channel in high erosion-resistant bedrock zones tend to have narrower width, and higher steepness; on the other hand, weak or fractured rock layers promote lateral erosion and the formation of wide, shallow river valleys. 2)Tectonic deformation drives channel morphology through changes in uplift rate: rivers in high uplift rate areas concentrate shear forces by contracting width, accelerating downcutting to balance uplift, while rivers in low uplift areas weaken erosive capacity by widening the channel. 3) The dual effect of sediment supply significantly influences the response to width: adequate sediment cover of the streambed inhibits downcutting but enhances lateral erosion, whereas low sediment supply concentrates the energy on basement erosion, creating narrower and deeper channels. 4)Extreme climatic events trigger short-term adjustments in channel width through drastic changes in flood flow and sediment pulse inputs, and in the long term influence morphological evolution through changes in erosion datum. Thus, the current study still has the problems of an unknown multi-factor coupling mechanism and insufficient universality of the quantitative model. In the future, we need to combine high-resolution remote sensing, numerical simulation and chronological data to deepen the application of the width parameter in the geomorphological evolution model, so as to provide a new perspective for the study of tectonic-climatic interactions in orogenic zones.

Key words: channel width, stream power erosion, transient geomorphology, fluvial landform

张熠辉, 张会平, 赵旭东. 活动造山带地区基岩河道宽度控制因素及其对地貌演化指示意义[J]. 地震地质, 2026, 48(3): 651-684.

ZHANG Yi-hui, ZHANG Hui-ping, ZHAO Xu-dong. BEDROCK CHANNEL WIDTH IN ACTIVE OROGENIC BELTS: CONTROLLING FACTORS AND IMPLICATIONS FOR LANDSCAPE EVOLUTION[J]. SEISMOLOGY AND GEOLOGY, 2026, 48(3): 651-684.

图/表 13

图1 全球河道宽度研究实例

Fig. 1 Examples of global river channel width studies.

图2 河道几何形态参数 W 河道宽度; D 河道深度; B 河道横断面面积; Wp 湿面周长; Wv 河谷宽度

Fig. 2 River channel geometry parameters.

表1 不同地区河道宽度水力几何系数(部分修改自Wohl et al., 2008)

Table1 Hydraulic Geometry Coefficients of River Channel Width for Different Regions (modified from Wohl et al., 2008)

地区	水力几何表达式	文献
Satsop River, 华盛顿州	W=0.007A^0.47, 基岩河道 W=0.005A^0.49, 冲积河道	Montgomery et al., 2001
Willapa River, 华盛顿州	W=0.054 7A^0.32, 基岩河道 W=0.020A^0.39, 冲积河道
Sullivan and Larson Creek, 俄勒冈州	W=0.015A^0.42, 基岩河道 W=0.034A^0.33, 冲积河道
Knowles Creek, 俄勒冈州	W=0.002A^0.53, 基岩河道 W=0.05A^0.32, 冲积河道
Yuba River, 加尼福尼亚州	W=0.008A^0.37, 基岩河道 W=0.003A^0.45, 冲积河道
门多西诺三联点, 加利福尼亚州北部	W∝A^0.4	Snyder et al., 2003
Clearwater River, 华盛顿州	W=4.20A^0.42	Tomkin et al., 2003
Lachlan River,澳大利亚东南部	W∝0.0004A^0.55, W∝0.001A^0.53, W∝0.012A^0.41	van der Beek et al., 2003
圣伊内斯山脉, 加利福尼亚南部沿海地区	W∝0.08A^0.33(低抬升速率) W∝0.007A^0.42(高抬升速率) W∝A^0.4(全段)	Duvall et al., 2004
加利福尼亚州金山, 俄勒冈州沿海地区, 华盛顿州奥林匹克山脉, 内华达山脉, 弗吉尼亚州马里兰地区, 四川龙门山地区	W=3.3A^0.36	Whipple, 2004
亚平宁山脉中部, 意大利	W∝A^0.35~0.5	Whittaker et al., 2007b
北港溪, 台湾	W=0.002 3A^0.5378	Yanites et al., 2010c
涪江, 四川	W∝A^0.57	Kirby et al., 2011
杂谷脑河, 四川	W∝A^0.39
湔江, 四川	W∝A^0.63
黑水河、岷江, 四川	W∝A^0.36
San Gabriel Mountains, 加利福尼亚州	W=3.18A^0.27(低起伏度区域) W=4.06A^0.22(高起伏度区域)	DiBiase et al., 2011
上西瓦利克山, 喜马拉雅山脉	W∝A^0.36	Allen et al., 2013
中西瓦利克山, 喜马拉雅山脉	W∝A^0.72
苏格兰高地地区	W=4.54A^0.3, 基岩河道 W=4.61A^0.41, 冲积河道	Whitbread et al., 2015
Ontario and Québec, 加拿大	W=6.62A^0.4	Ferguson et al., 2017

表1 不同地区河道宽度水力几何系数(部分修改自Wohl et al., 2008)

Table1 Hydraulic Geometry Coefficients of River Channel Width for Different Regions (modified from Wohl et al., 2008)

地区	水力几何表达式	文献
Satsop River, 华盛顿州	W=0.007A^0.47, 基岩河道 W=0.005A^0.49, 冲积河道	Montgomery et al., 2001
Willapa River, 华盛顿州	W=0.054 7A^0.32, 基岩河道 W=0.020A^0.39, 冲积河道
Sullivan and Larson Creek, 俄勒冈州	W=0.015A^0.42, 基岩河道 W=0.034A^0.33, 冲积河道
Knowles Creek, 俄勒冈州	W=0.002A^0.53, 基岩河道 W=0.05A^0.32, 冲积河道
Yuba River, 加尼福尼亚州	W=0.008A^0.37, 基岩河道 W=0.003A^0.45, 冲积河道
门多西诺三联点, 加利福尼亚州北部	W∝A^0.4	Snyder et al., 2003
Clearwater River, 华盛顿州	W=4.20A^0.42	Tomkin et al., 2003
Lachlan River,澳大利亚东南部	W∝0.0004A^0.55, W∝0.001A^0.53, W∝0.012A^0.41	van der Beek et al., 2003
圣伊内斯山脉, 加利福尼亚南部沿海地区	W∝0.08A^0.33(低抬升速率) W∝0.007A^0.42(高抬升速率) W∝A^0.4(全段)	Duvall et al., 2004
加利福尼亚州金山, 俄勒冈州沿海地区, 华盛顿州奥林匹克山脉, 内华达山脉, 弗吉尼亚州马里兰地区, 四川龙门山地区	W=3.3A^0.36	Whipple, 2004
亚平宁山脉中部, 意大利	W∝A^0.35~0.5	Whittaker et al., 2007b
北港溪, 台湾	W=0.002 3A^0.5378	Yanites et al., 2010c
涪江, 四川	W∝A^0.57	Kirby et al., 2011
杂谷脑河, 四川	W∝A^0.39
湔江, 四川	W∝A^0.63
黑水河、岷江, 四川	W∝A^0.36
San Gabriel Mountains, 加利福尼亚州	W=3.18A^0.27(低起伏度区域) W=4.06A^0.22(高起伏度区域)	DiBiase et al., 2011
上西瓦利克山, 喜马拉雅山脉	W∝A^0.36	Allen et al., 2013
中西瓦利克山, 喜马拉雅山脉	W∝A^0.72
苏格兰高地地区	W=4.54A^0.3, 基岩河道 W=4.61A^0.41, 冲积河道	Whitbread et al., 2015
Ontario and Québec, 加拿大	W=6.62A^0.4	Ferguson et al., 2017

图3 印度Siwaliks山前河道形态研究结果(修改自Allen et al., 2013) a—c 莫汉德山脉的区域图、平衡剖面图及研究河流, 图b中, 蓝色虚线代表河道高程; d 莫汉山脉地层岩性及岩体强度测量值; e 河道陡峭系数分布图; f 河道宽度系数分布图; g 河流剪应力分布图

Fig. 3 Results of the study of river channel morphology in Siwaliks, India(modified from Allen et al., 2013).

图4 雅鲁藏布江南迦巴瓦峡谷区河道宽度与流域面积幂率图(修改自Montgomery,2004) 灰色虚线表示W∝A0.5

Fig. 4 Plot of river channel width versus drainage area in the Namcha Barwa Canyon, Yarlung Tsangpo(modified from Montgomery, 2004).

图5 不同隆升速率下河道宽度与流域面积关系图(修改自Turowski et al., 2007b)

Fig. 5 Plot of river channel width versus drainage area under different uplift rates (modified from Turowski et al., 2007b).

图6 加利福尼亚州南部沿岸的圣伊内斯山脉的河道宽度研究结果(修改自Duvall et al., 2004) a 研究区位置; b 宽度-流域面积幂率图。以位于低隆升速率区的38号河道和位于高隆升速率区的50号河道为例, 对其河道宽度和流域面积进行幂率回归以计算其宽度系数, 图中虚线表示以相同的幂指数进行回归计算; c 河道陡峭系数图, 低隆升速率区的平均陡峭系数为13.8, 高隆升速率区的平均陡峭系数为26.1

Fig. 6 Results of river channel width analysis in the Santa Ynez Mountains along the south coast of California(modified from Duvall et al., 2004).

图7 河道宽度对于活动褶皱的响应概念图(修改自Amos et al., 2007) a 隆升幅度较小时河道宽度缩小而坡度可以保持不变; b 隆升量增大到一定程度河道宽度收缩幅度达到最大值, 河道坡度开始变化

Fig. 7 Conceptual diagram of river channel width response to active folding(modified from Amos et al., 2007).

图8 中国台湾地区北港溪(Peikang River)河道坡度与河道宽度顺流变化趋势(修改自Yanites et al., 2010c) 虚线表示断层, 灰色实线代表计算值, 叉号代表实测值

Fig. 8 Downstream trends of channel gradient and width in the Peikang River, Taiwan, China(modified from Yanites et al., 2010c).

图9 不同沉积物通量(QS)下河道宽度和坡度随侵蚀速率变化模式图(修改自Yanites et al., 2010a)

Fig. 9 Plot of river channel width and slope variation patterns against erosion rate under different sediment fluxes(modified from Yanites et al., 2010a).

图10 Rio Torto河流满岸河道宽度顺流变化趋势(a);Rio Torto河河道宽度与河谷宽度比值顺流变化趋势(b)(修改自Whittaker et al., 2007a)

Fig. 10 Downstream trends of bankfull width in the Rio Torto(a); Downstream trend of the channel-to-valley width ratio(b)(modified from Whittaker et al., 2007a).

图11 具有不同Selby岩体强度的河道对应的水力几何系数回归(修改自Wohl et al., 2008)

Fig. 11 Regression of hydraulic geometry coefficients for river channels categorized by Selby rock mass strength(modified from Wohl et al., 2008).

图12 中国台湾地区2009年莫拉克台风前后河道形态变化(修改自Yanites et al., 2018) a、c 台湾中央山脉以西流域; b、d 中央山脉以东流域

Fig. 12 Changes in channel morphology in Taiwan, China induced by Typhoon Morakot(modified from Yanites et al., 2018).

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