长江三峡贯通过程的动态古地貌重建<sup>*</sup>

田子晗, 索艳慧, 李三忠, 丁雪松, 韩续, 宋双双, 付新建. (2024). 长江三峡贯通过程的动态古地貌重建^* [J]. 古地理学报, 26(1): 208-229.
TIAN Zihan, SUO Yanhui, LI Sanzhong, DING Xuesong, HAN Xu, SONG Shuangshuang, FU Xinjian. (2024). Dynamic paleo-landscape reconstruction revealing incision process of Three Gorges of Yangtze River[J]. Journal Of Palaeogeography, 26(1): 208-229. 复制到剪切板

Doi: 10.7605/gdlxb.2023.06.071
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长江三峡贯通过程的动态古地貌重建^*

田子晗^1,², 索艳慧^1,², 李三忠^1,², 丁雪松³, 韩续^1,², 宋双双^1,², 付新建^1,²

1 深海圈层与地球系统教育部前沿科学中心,海底科学与探测技术教育部重点实验室,中国海洋大学海洋地球科学学院,山东青岛 266100

2 青岛海洋科学与技术国家实验室,海洋矿产资源评价与探测技术功能实验室,山东青岛 266237

3 加州大学洛杉矶分校地球行星与空间科学学院,美国加州洛杉矶 CA90095

通讯作者简介 索艳慧,女,1987年生,中国海洋大学教授、博士生导师,从事海洋地质学、洋底动力学研究。E-mail: suoyh@ouc.edu.cn。

第一作者简介 田子晗,男,1998年生,硕士研究生,海洋地质学专业。E-mail: tzh7403@stu.ouc.edu.cn。

收稿日期:2022-10-21 修回日期:2023-02-08

基金资助:*青岛海洋科学与技术国家实验室山东省专项经费(编号: 2022QNLM05032)、国家自然科学基金项目(编号: 42121005,91958214)、山东省自然科学基金项目(编号: ZR2021YQ25)和中央高校基本科研业务费专项(编号: 202172003)联合资助

摘要

长江是亚洲第一大河,其形成和演化是新生代以来中国东西部构造—气候—地貌综合演变的结果。长江三峡的贯通是现代长江形成的标志性事件,但受限于传统沉积学、地球化学等单一方法的制约,对“长江三峡何时贯通”这一关键科学问题一直存在争议。综合考虑了构造运动、古气候及海平面变化等影响河流发展的关键因素,并将这些因素输入 Badlands古地貌模拟软件,动态重建了长江“第一弯”以东地区晚白垩世(80 Ma)以来的长江流域地貌及水系演化过程; 并利用四川盆地和江汉盆地的地震剖面资料验证了模拟结果的可靠性。模拟结果表明,青藏东部及上扬子西南缘晚始新世—渐新世的阶段性隆升迫使四川盆地原有南流水系下切受阻,沉积物在盆内堆积形成冲积河道并促使四川盆地地貌由“东北高西南低”反转为“西南高东北低”;新生代早期,江汉盆地长期受控于中国东部的裂陷环境,持续处于较低基准面。四川盆地的水系反转和江汉盆地的持续低基准面,最终导致位于二者之间的长江三峡在晚渐新世发生贯通。由此,本研究提出一种上扬子地区水系反转并被下游捕获的三峡贯通机制。

关键词: 古地貌重建; 长江三峡贯通; 晚渐新世; 四川盆地; 江汉盆地; 水系反转

中图分类号:P531 文献标志码:A 文章编号:1671-1505(2024)01-0208-22

Dynamic paleo-landscape reconstruction revealing incision process of Three Gorges of Yangtze River

TIAN Zihan^1,², SUO Yanhui^1,², LI Sanzhong^1,², DING Xuesong³, HAN Xu^1,², SONG Shuangshuang^1,², FU Xinjian^1,²

1 Frontiers Science Center for Deep Ocean Multispheres and Earth System,Key Lab of Submarine Geosciences and Prospecting Techniques,MOE and College of Marine Geosciences,Ocean University of China,Shandong Qingdao 266100,China

2 Laboratory for Marine Mineral Resources,National Laboratory for Marine Science and Technology(Qingdao),Shandong Qingdao 266237,China

3 University of California Los Angeles,Department of Earth,Planetary and Space Sciences,Los Angeles,CA90095,USA

About the corresponding author SUO Yanhui,born in 1987,is a professor and a Ph.D. supervisor of Ocean University of China. She mainly focuses on marine geology and marine geodynamics. E-mail: suoyh@ouc.edu.cn.

About the first author TIAN Zihan,born in 1998,master degree candidate,majors in marine geology. E-mail: tzh7403@stu.ouc.edu.cn.

Fund:Co-funded by the Marine S & T Fund of Shandong Province for National Laboratory for Marine Science and Technology(Qingdao)(No.2022QNLM05032),the National Natural Science Foundation of China(Nos.42121005,91958214),the Natural Science Foundation of Shandong Province of China(No. ZR2021YQ25)and the Fundamental Research Funds for the Central Universities(No.202172003)

Abstract

The Yangtze River,Asia's largest river,represents a significant geomorphological event within the integrated tectonics-climate-landscape system of the Cenozoic era in China. A key point of debate in understanding its formation is the timing of the incision of the Three Gorges,situated between the Sichuan and Jianghan basins,which marked the emergence of the modern Yangtze River. Despite abundant geological data,there remains controversy over when exactly the Three Gorges were formed or incised. Previous studies usually focused on isolated factor affecting the river development,e.g., tectonic movements,sedimentology,paleo-climate and sea level changes,to resolve this key issue. In contrast,our study utilizes Badlands,a software for simulating paleo-landscape,to integrate these key factors quantitatively. Focusing on the area east of the “first bend”(Shigu Town in Yunnan Province)of the Yangtze River,we used Badlands to reconstruct the paleo-landscape and river system evolution process since the Late Cretaceous(80 Ma). We further validated our model results using seismic data from the Sichuan and Jianghan basins. The results revealed that the river flow direction in the Sichuan Basin was reversed to drain northwards due to the Late Eocene-Oligocene uplift in the eastern Tibet and the southwestern Upper Yangtze Plate. The Jianghan Basin maintained a consistently low base level during the early Paleogene,influenced by the continental rifting environment in eastern China. The reversal of the drainage direction in the Sichuan Basin and the long-lasting low base level in the Jianghan Basin eventually made the Three Gorges to be incised at the latest Oligocene. We propose that the reversal and subsequent capture of the Upper Yangtze River's flow by the middle Yangtze River played a crucial role in the incision mechanism of the Three Gorges.

Key words: paleo-landscape reconstruction; Three Gorges incision; Late Oligocene; Sichuan Basin; Jianghan Basin; drainage inversion

文章图片

1 概述

新生代以来, 太平洋板块俯冲和印度— 欧亚板块碰撞导致东亚地形格局从东高西低转变为西高东低(Ren et al., 2002; Schellart et al., 2019; 张岳桥等, 2019; 李三忠等, 2022), 青藏高原加速隆升产生强烈地势差异并促使东亚季风系统形成及强化, 上述过程深刻影响了长江、黄河、珠江等大型河流系统的形成演化。其中, 长江起源于青藏高原唐古拉山, 向东流入东海, 全长6280 km, 是亚洲第一、世界第三大河; 长江携带的巨量水沙, 在其流域生态环境和中国东部边缘海的海陆相互作用及其物质循环过程中扮演关键角色(汪品先, 1998; 郑洪波和贾军涛, 2009)。长江水系的形成, 是板块构造驱动下的沉积、地貌和气候演化有机结合的结果, 是研究地球深部与地表系统多圈层耦合作用的“ 天然实验室” 。但对于“ 长江东流水系形成于何时” 这一关键科学问题却一直存在重大争议, 尤其是针对长江水系定型的标志性事件— — 长江三峡贯通的时限存在多种观点: 低温热年代学研究揭示45~40 Ma期间四川盆地及黄陵穹隆存在1期快速降温事件, 可能是三峡贯通后地层快速剥蚀所致(Richardson et al., 2008, 2010); 江汉盆地沉积相及“ 长江砾岩” 年代学等研究结果暗示三峡的贯通发生在渐新世— 中新世之交(Zheng et al., 2011; 郑洪波等, 2013); 三峡地区河流阶地沉积物ESR(Electron Spin Rasanance:电子自旋共振)测年则反映了长江三峡可能在早更新世贯通(Li et al., 2001)。以上观点主要是基于沉积学、地球化学等单一方法对三峡贯通过程进行分析, 尚未从新生代以来的构造— 气候— 地貌的统一耦合体系角度出发, 系统推演长江演化过程。

Badlands古地貌模拟软件, 是一套正演不同时间和空间尺度上地表过程的数值模拟软件, 它综合考虑了地幔对流、构造、古气候、侵蚀和沉积等地球深部和浅表系统多种因素对地貌的影响(Salles, 2016; Salles et al., 2018)。因此, 作者利用Badlands软件, 通过加载中国东部、四川盆地及周边地区山脉隆升剥蚀量、新生代裂陷盆地沉降量、海平面变化、降水量等数据, 耦合了构造— 气候— 地貌系统, 模拟了云南省石鼓镇“ 长江第一弯” 以东区域晚白垩世以来的地貌演变过程, 并分析长江演化及三峡贯通过程。

2 区域地质背景

长江流域面积达180万平方千米, 跨越多个地质单元。金沙江段主要流经昌都地块、松潘— 甘孜地块; 川江段及中下游流经扬子地块, 包括四川盆地、黄陵穹隆、江汉— 洞庭湖盆地、苏北— 南黄海盆地及东海陆架盆地等次级单元; 长江流域北部为秦岭— 大别造山带, 南部为华夏地块(图 1-a, 1-b)。昌都地块地处长江源头(图 1-b), 变质基底由3套前寒武纪地层构成(游再平, 2001)。早古生代造山活动频繁, 加里东运动后进入稳定洋盆阶段并发育弧后盆地, 沉积相主要表现为滨海相及浅海碳酸盐岩相; 中生代以来洋盆逐渐关闭, 由早三叠系滨浅海环境过渡至晚侏罗系陆内环境, 在此期间形成巨厚复理石及磨拉石建造; 新生代以来走滑拉分活动强烈, 盆地沉积广泛发育(杜德勋等, 1997)。

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	图 1 长江流域地貌及水系(a)和主要地质单元(b)Fig.1 Landscape and drainage distribution(a) of Yangtze River basin and its main tectonic units(b)

松潘— 甘孜褶皱带地处扬子地块以西, 涵盖了长江金沙江段(图 1-b)。该褶皱带主体为晚石炭世至晚三叠世期间古特提斯洋向北俯冲过程中形成的弧前构造带(杨宗让, 2002); 晚二叠世, 峨眉山地幔柱活动引发强烈的裂谷作用并形成深水洋盆(Song et al., 2004); 中三叠世以来洋盆逐渐萎缩并发育巨厚复理石建造。晚三叠世松潘— 甘孜褶皱带向扬子地块强烈俯冲形成龙门山冲断带(刘树根等, 1995)。

扬子地块是长江流域主体地区(图 1-b), 其基底由太古宇— 古元古界结晶基底及中— 新元古界变质基底组成, 发生在0.82 Ga左右的晋宁运动使扬子地块与华夏地块完成拼合(葛肖虹和马文璞, 2014)。随后扬子地块长期处于稳定阶段, 南华纪至中三叠世发育广泛的浅海碳酸盐沉积, 印支期后转入陆相沉积; 晚白垩世以来, 扬子板块受到古太平洋板块及太平洋板块俯冲影响, 广泛发育裂陷盆地并形成众多河流湖泊相沉积(王鸿祯, 1985)。

秦岭— 大别造山带地处长江流域北部(图 1-b), 其基底形成于晚太古代— 古元古代; 新元古代至早古生代期间, 秦岭造山带持续处于扩张状态, 裂谷活动强烈并在早古生代形成宽2000~3000 km的洋盆, 在此期间广泛发育深水盆地沉积; 早古生代晚期, 扬子板块开始向华北板块俯冲并于晚中生代发生碰撞作用; 三叠纪, 全面陆陆碰撞造山作用使秦岭— 大别造山带最终成型(张国伟等, 1996)。中生代以来, 秦岭造山带处于持续剥蚀状态; 新生代强烈的伸展作用导致秦岭再次隆升形成高耸山脉并成为长江流域和黄河流域分水岭(孟庆任, 2017)。

华夏地块位于长江流域东南部(图 1-b), 碎屑锆石年代学(Zhang et al., 2006)表明其可能存在太古代基底。元古代以来, 华夏地块发生多期变质作用, 沉积环境主要为深水盆地。晋宁运动后, 华夏地块与扬子板块拼合形成统一的华南板块, 此后加里东期广泛的构造活动使华夏地块褶皱广泛发育; 晚中生代以来强烈的火山活动对其也产生显著影响(葛肖虹和马文璞, 2014)。

3 模拟方法及模型构建

3.1 模拟方法

Badlands是一个描述地球表面活动的景观演化模型(Landscape evolution models)。该模型考虑了构造活动、气候变化、海平面升降、地壳均衡效应、岩石剥蚀及沉积物堆积等过程对地貌演化的影响(Salles and Hardiman, 2016)。

1)构造活动是某点一段时间内在三维空间上的位移积累量, 包括垂直方向上的隆升沉降量以及水平方向上的运动距离(文中称之为构造地形); 此外还可以将反演得到的动力地形作为构造活动参数(Ding et al., 2019)。

2)气候变化参数在Badlands代码中以降水量的形式表现, 可以在模型中某段时间内设置恒定值或导入地形降水线性模型(Smith and Barstad, 2004)加以实现。

3)海平面升降是影响地表作用的重要因素, 其变化受到气候、洋陆相互作用等因素控制, Badlands代码中可通过导入全球海平面变化曲线数据加以实现。

4)地貌演化中伴随着剥蚀及沉积过程, 这会导致地球弹性外壳上的区域质量再分配并进一步影响地壳形变, Badlands代码中可通过挠曲均衡模块对进行相应校正。

在代码运行过程中主要遵循以下质量连续性方程:

$\frac{\partial z}{\partial t}$ =-Ñ · q_s+u (1)

该方程描述了构造驱动的地貌效应(Chen et al., 2014)。公式(1)左侧表示某点地表高程(z)在单位时间上的变化量; 右侧u表示构造活动引发的地表隆升/沉降量, 单位m/yr; q_s表示深度上为整体、单位宽度上的沉积物通量, 单位m²/yr。

下述方程描述了沉积物的输运及水流侵蚀过程(Salles, 2016):

-Ñ · q_r=-eA^m(Ñ z)ⁿ (2)

-Ñ · q_d=-κ $^{2}$ z (3)

公式(2)描述了沉积物以地表径流方式输运的状态, 左侧q_r表示单位宽度上流水输运沉积物的速率; 右侧€ 为无量纲侵蚀常数, 其受到气候、岩性及泥沙载荷多因素控制(Whipple and Tucker, 1999), A为排水面积, Ñ z为地形梯度, m和n表示沉积物通量及输运能力恒定的情况下河流下切速率与河床剪应力之间的关系, 它们没有恒定取值但m/n的值通常为0.5(Tucker and Hancock, 2010)。公式(3)描述了沉积物以蠕移扩散方式输运的状态, 其中κ 表示扩散系数, 其取值不固定, 往往受到岩性、降水及其他因素影响, 可通过现场考察获取较为精确的数值(Dietrich et al., 1995; Whipple and Tucker, 1999; Tucker and Hancock, 2010)。

3.2 模型构建

构建的地貌演化模型需输入初始地形、构造地形、古降水、古海平面、侵蚀系数等。

3.2.1 初始古地形构建

文中研究区为长江第一弯以东地区, 纬度范围24° N~35° N、经度范围100° E~122° E(图 2)。长江流域的地貌演化和贯通主要发生在新生代。为了较为完整地体现一系列晚白垩世— 早新生代构造活动对地形产生的影响, 需要对新生代的模拟时间进行合理外延。80 Ma前后(± 5 Ma)的古地貌研究成果较为丰富, 更易用于限定古地形, 故设定初始古地形时间为80 Ma。研究区包含多个构造单元, 各单元初始古高程数据来源见表 1。

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	图 2 长江流域晚白垩世(80 Ma)初始古地貌Fig.2 Paleo-landscape reconstruction at the Late Cretaceous(80 Ma) in Yangtze River basin

表 1 各构造单元晚白垩世古高程数据 Table1 Paleo-elevation of each tectonic unit at the Late Cretaceous

3.2.2 构造地形构建

新生代以来, 受到太平洋及特提斯构造体系相互作用的强烈影响, 中国东部地区普遍遭受弧后伸展导致的古高原垮塌及克拉通破坏作用, 而西部、西南部则由于印度— 欧亚板块碰撞发生强烈横向缩短及纵向隆升作用, 中国整体地貌产生西低东高到西高东低的巨变(李三忠等, 2022; 张岳桥等, 2019; Ren et al., 2002; Schellart et al., 2019)。此外, 中国大陆内部存在多个相互作用复杂的构造单元, 无法通过粗糙且变化量较小的动力地形模拟数据准确约束构造地形。因此, 作者收集了造山带低温热年代学及裂陷盆地沉降数据(图 3), 构建各构造单元不同演化阶段的构造地形。不同构造单元的数据详情见表 2。

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	图 3 长江流域晚白垩世(80 Ma)以来构造数据分布(具体数据及来源见表 2)Fig.3 Distribution of tectonic data since the Late Cretaceous(80 Ma)in Yangtze River basin(see details in Table 2)

表2 长江流域晚白垩世以来造山带区域隆升剥露数据 Table 2 Uplift and exfoliation data of orogenic belt region since the Late Cretaceous in Yangtze River basin

山脉、高原等隆升区数据绝大多数来自低温热年代学方法获得的研究资料(表 2; 表 3)。低温热年代学研究最常见的对象是磷灰石或锆石裂变径迹, 该方法往往用以揭示岩石的剥露(exhumation)过程(Peter and Mark, 2006), 即岩石相对的地表位移, 其往往是侵蚀(erosion)或构造活动(tectonic progress)引发负载岩石的清除(removal)作用(England Molnar, 1990)。通常情况下, 磷灰石快速冷却是构造剥露的重要特征, 而正断层活动、陆内造山增厚及大陆边缘地壳横向减薄等构造因素控制了构造剥露速度(Ring et al., 1999; Stü we and Terence, 1998), 因此可以通过低温热年代学数据对构造地形加以约束。地壳均衡补偿了相当一部分剥露作用效果(Tsuboi, 1983), 因此低温热年代学数据包含了均衡效应的影响。此外, 地壳挠曲均衡量恢复严重依赖准确的有效弹性厚度(Te), 该数值受到板块演化的显著影响。因研究区构造单元众多且模拟时间跨度大, 难以获得合适的Te参数, 故建立模型时没有进行挠曲均衡校正。

表 3 长江流域晚白垩世以来盆地沉降速率数据 Table3 Data of basin subsidence rates since the Late Cretaceous in Yangtze River basin

3.2.3 古降水重建

在Badlands代码中, 古降水量是影响地表岩石侵蚀、河流下切及沉积物搬运的重要参数(Salles and Hardiman, 2018)。研究区不同时间段古降水量数据及来源见表 4。

表 4 长江流域晚白垩世以来古降水量数据汇总 Table4 Paleo-precipitation data since the Late Cretaceous in Yangtze River basin

3.2.4 古海平面重建

海平面升降会改变河流侵蚀基准面以及沉积物容纳空间, 从而影响流域地貌的演变(Watts and Thorne, 1984; Schumm, 1993; Jacob et al., 2011; Ken et al., 2015), 因此是模型的重要参数。本研究采用了Haq等(1987)海平面重建方案。

3.2.5 侵蚀系数

侵蚀系数(erodibility coefficient)是在Badlands代码中构建地貌演化模型重要参数, 它受到岩性、河道宽度、洪水频率及河道水流动力等因素的控制(Salles and Hardiman, 2016)。模拟结果表明, 侵蚀系数对地貌演化模型影响强烈, 通过现今研究区真实地貌、地表岩石侵蚀量恢复以及盆地地震剖面等资料约束, 设定该系数为5× 10^-6较为贴合实际情况。

4 模拟结果

4.1 古地貌演化过程

晚白垩世, 中国整体地形呈现出“ 东高西低” 的特征。锆石年代学研究(王瑞和姜宝玉, 2021)表明, 这一时期四川盆地可能存在流向西南的水系, 四川盆地被造山带围限仅西南侧海拔较低是水系向该方向发育的原因(图 4-a, 4-b)。受古太平洋板块俯冲后撤影响, 中国东部裂陷活动强烈(Li et al., 2014; Suo et al., 2019), 山间盆地及边缘海盆地的发育可能促进了东部水系的建立(图 4-b), 而扬子地区东西两侧水系被海拔超过2000 m的湘鄂西褶皱带阻隔。

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	图 4 晚白垩世(80 Ma)以来古地貌演化模型Fig.4 Paleo-landscape evolution model since the Late Cretaceous

古新世至早始新世, 中国整体地貌格局没有发生明显变化(图 4-b, 4-c)。但东部的持续裂陷活动(Li et al., 2014; Suo et al., 2019), 导致盆地规模扩大、古高原萎缩。中下扬子东部河流系统继续向西扩展, 而四川盆地水系格局没有显著变化(图 4-c)。

古近纪晚期, 青藏东南缘及大凉山地区的快速隆升, 导致四川盆地排水严重受阻, 沉积物大量堆积抬升地表并迫使西南向水系开始衰亡(图 4-c, 4-d)。湘鄂西褶皱带长期构造稳定, 持续剥蚀降低。

中国东部持续强烈伸展作用则导致江汉盆地处于较低基准面。研究区东西两侧构造环境的共同作用, 最终导致长江三峡在晚渐新世(约26 Ma)发生贯通(图 4-e)。新近纪以来, 研究区气候湿润化, 中国东部山脉侵蚀强烈, 长江流域现今水系形态逐步建立(图 4-f)。晚新生代以来, 云贵高原快速隆升, 促使金沙江向北进入四川盆地形成现代长江流域(图 4-g, 4-h)。

4.2 模拟结果对比

为验证模拟结果的可靠性, 选择长江三峡东西两侧的江汉盆地和四川盆地作为参考对象, 对比了晚白垩世以来四川盆地的剥蚀量(图 5)及江汉盆地沉积厚度(图 6)。模拟结果表明, 四川盆地的剥蚀主要集中在川东、川北及川西南等边缘区域, 而川中、川南的剥蚀明显较弱(图 5-a), 这与低温热年代学恢复的剥蚀量(图 5-b)反映的趋势相同。但需要注意文中模拟的起始时间为80 Ma, 故模拟结果相对于热年代学揭示的晚白垩世以来的剥蚀恢复量偏小。地震资料揭示, 江汉盆地晚白垩世以来的沉积中心主要位于江陵凹陷、潜江凹陷, 其沉积厚度超过10 000 m; 其他区域, 如陈沱口凹陷、小板凹陷、沔阳凹陷部分区域沉积厚度达5000 m(江汉油田石油地质志编写组, 1991)。本研究模拟结果呈现的盆地各次级单元沉积厚度和沉积中心位置与地震资料揭示的结果吻合较好(图 6)。此外, 模拟结果中显示的部分地层剖面结构, 也与地震剖面解译的地层结构呈现出明显的相似性(图 7)。

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	图 5 四川盆地晚白垩世以来地层剥蚀量 a— 低温热年代学揭示剥蚀量(据邓宾等, 2009); b— 本研究模拟的80 Ma以来剥蚀量Fig.5 Strata denudation since the Late Cretaceous in Sichuan Basin

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	图 6 江汉盆地晚白垩世以来地层沉积厚度 a— 地震资料揭示的沉积厚度(据Wu et al., 2020); b— 本研究模拟的沉积厚度Fig.6 Sedimentary thickness since the Late Cretaceous in Jianghan Basin

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图 7 江汉盆地地震剖面与模拟剖面结果对比(剖面位置见图 6-a。地震剖面来源: AA’ 据赵长煜, 2009; BB’ 和CC’ 据卢林, 2005; DD’ 据王德良等, 2018)Fig.7 Comparison between seismic profiles and simulated profiles in Jianghan Basin(Profile location is shown in Fig.6-a. Seismic profile AA’ was from Zhao, 2009; BB’ and CC’ were from Lu, 2005; DD’ was from Wang et al., 2018)

5 讨论

5.1 长江三峡的贯通时限

利用锆石年龄特征进行物源追踪是分析河流演化的重要方法(Clift et al., 2012)。同位素年代学研究表明, 扬子板块、华夏板块、松潘— 甘孜地块、江南造山带及秦岭大别造山带中, 现代长江流域大部分区域碎屑锆石的年龄大于65 Ma, 年龄小于65 Ma的碎屑锆石记录主要出现在金沙江地区。青藏高原始新世以来的隆升过程伴随着广泛的岩浆活动, 是长江流域新生代锆石的主要物源(He et al., 2013, 2014)。长江上游北羌塘地块出露诸多年龄为40~24 Ma的花岗岩(朱丽等, 2006; Xu et al., 2019), 其东部金沙江— 红河构造带则存在年龄为40~30 Ma的花岗岩(Liu et al., 2022); 此外, 松潘— 甘孜褶皱带东南部鲜水河断裂带出露始新世— 渐新世花岗岩(李海龙等, 2016; 唐渊等, 2022)。因此, 在长江中下游地区沉积地层中识别新生代锆石信号, 是分析三峡贯通时限的重要依据。

江汉盆地位于长江三峡东侧出口, 必然留存其贯通事件的地质记录(Zheng, 2015)。Yang等(2019)在江汉盆地中新统广化寺组下部, 首次识别出同位素年龄32 Ma的碎屑锆石, 该地层底界年代约为26~24.6 Ma(王必金等, 2006)。江汉盆地内部存在最新年龄不超过36.5 Ma新生代玄武岩(徐论勋等, 1995)。可见, 长江三峡在渐新世末期已经贯通, 才会导致上述可能来源于青藏东部新生代花岗岩的碎屑锆石进入江汉盆地。

另有研究表明, 长江下游南京、六安地区出露的“ 长江砾岩” 形成年代不晚于早中新世, 其碎屑锆石年龄谱特征与长江三角洲全新世沉积物锆石年龄谱特征(Jia et al., 2010)基本相当, 由此推测长江三峡贯通导致一条含有与现代长江无法区分物源的河流在中新世之前形成(Zheng et al., 2013)。

不同的沉积相反映了水动力环境的变化, 是分析水系类型及演化的重要依据(Andrew, 2006)。Wang等(2014)指出江汉盆地西缘宜昌至松滋地区出露的古近系主要为砂岩— 粉砂岩, 代表低能量边缘湖相环境, 而在中新世地层中则出现大量低成熟度砾石并发育辫状河沉积, 古水流呈东南走向。在晚渐新世, 江汉盆地主体也由深水湖盆沉积向大型河流沉积转变。此外, 长江下游多地出露早中新世辫状河及泛滥平原相沉积(Zheng et al., 2013; 徐亚东等, 2014; Wang et al., 2022)。上述区域沉积环境的显著变化, 可能反映了中下扬子地区在早中新世之前可能出现了东西向大型贯通性河流。

以上资料均表明长江下游地区在早中新世沉积物源及沉积动力条件已经发生显著转变, 这种转变可能受到了长江三峡贯通的影响。本研究模拟结果揭示的长江三峡在晚渐新世— 早中新世贯通, 这一结果与上述地质资料吻合。

5.2 古长江水系演化及三峡贯通机制

大型河流系统的形成发展受到板块构造、气候演变、海平面升降等要素的控制(郑洪波和贾军涛, 2009)。新生代以来, 青藏高原隆升、中国东部裂陷盆地发育以及东亚季风建立等因素(汪品先, 1998)均对长江水系的形成和演化产生了重要影响。因此, 对三峡贯通事件的研究, 需要综合考虑各种因素效应并对各因素的重要性加以评估。Badlands软件定量化考虑了上述多种环境因素, 基于这种构造— 气候— 地貌综合演变的模拟结果, 可以探讨古长江水系演化及三峡贯通机制。

沉积资料表明, 晚白垩世原四川盆地呈现出“ 东北高西南低” 的地貌格局, 大凉山等现今高海拔地区处于湖盆沉积环境(Li et al., 2016); 扬子西南缘沿南北方向分布一系列盆地, 如西昌盆地、会理盆地、楚雄盆地、思茅盆地等, 这些盆地在晚白垩世至古新世普遍发育湖泊及河流相沉积(江卓斐等, 2014; 杨庆道, 2014; 冯盈, 2016; 赵杰等, 2020)。最新的锆石年代学数据表明, 晚白垩世至早古近纪青藏高原东缘存在一个物源区(包括松潘— 甘孜及上扬子地区), 发育流经上述盆地群的古河流(Zhao et al., 2021)。这得到了本研究模拟结果的验证, 模拟结果显示, 这一时期四川盆地由西南缘向外排水, 这些水系构成了古长江川江段(图 4-a, 4-b)。

古地磁、沉积相及古生物研究表明, 印度— 欧亚板块于55~50 Ma开始碰撞并进入“ 软碰撞” 阶段(Lee and Lawver, 1995; Suo et al., 2020), 新特提斯洋盆逐渐关闭(Klootwijk et al., 1992; Beck et al., 1995; Najman et al., 2010)。古氧同位素研究认为, 青藏东南缘在晚始新世(约40 Ma)已经存在与现今海拔相当的高原(Hoke et al., 2014; Li et al., 2015a), 但大气及海洋性质变化会显著影响传统氧同位素古地貌重建结果, 故该结果受到质疑。最新的古气候重建结果表明, 青藏地区晚始新世低海拔边界条件设定得到的氧同位素分布模型, 与实地样品分布拟合效果更好(Botsyun et al., 2019)。本研究的古地貌模拟结果表明, 青藏东南部及扬子西南缘的低地貌可能更有利于四川盆地周围山脉剥蚀物质向外排泄, 仅在现今大凉山地区出现较薄沉积地层(图 8-b), 原有水系的地貌梯度得以维持。另外锆石年代学研究表明, 至少40 Ma思茅盆地存在上扬子地区的物质输入(冯盈, 2016), 南流水系尚未中断。

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	图 8 四川盆地AB剖面模拟结果(剖面位置见图 1)Fig.8 Model results along Profile AB in Sichuan Basin(Profile location is shown in Fig.1)

岩浆记录及热年代学研究表明, 晚始新世(约40 Ma)青藏东部及四川盆地西南缘龙门山南部开始快速隆升(Chung et al., 1998, 2005; Richardson et al., 2008; Zhang et al., 2016), 这可能与45 Ma以来印度— 欧亚板块进入“ 硬碰撞” 阶段(Lee and Lawver, 1995)有关。与此同时, 印支地块快速顺时针旋转, 扬子西南缘受到强烈挤压(刘俊来等, 2007), 楚雄盆地群快速隆升(杨庆道, 2014)。本研究模拟结果显示, 青藏东南缘快速隆升导致剥蚀通量迅速增加, 而扬子西南部隆升则迫使沉积物在四川盆地南部堆积并形成平衡冲积河流系统(图 4-c, 4-d; 图 8-c, 8-d)。相较于深切河谷, 地形梯度较低的冲积河道更有利于河道反转使得古长江连续向西袭夺更易进行(Clark et al., 2004)。

晚古近纪, 四川盆地西南缘受到强烈挤压并广泛发育褶皱(Burchfiel et al., 1995; 王二七和尹纪云, 2009), 盆地向南排水进一步受阻。平衡冲积河流系统在下游隆升会显著阻碍河流下切, 导致沉积物在上游堆积并降低地貌梯度(Humphrey and Konrad, 2000), 当隆升速度高于河流下切速度则会迫使河道转向或消亡(Burbank et al., 1996)。本研究模拟结果表明, 约30 Ma盆地西南部大凉山地区的快速隆升破坏了南向外流水系, 30~25 Ma龙门山地区的强烈挤压(Wang et al., 2012)则进一步缩小盆地容积, 沉积物快速堆积并导致盆内冲积地貌逐渐反转(图 8-c至8-e)。此外, 川东— 湘鄂西褶皱带北部古近纪构造稳定持续剥蚀降低(王平等, 2012; 石红才和施小斌, 2014), 而江汉盆地长期裂陷沉降维持较低基准面则为河流改道提供大坡度潜在导流路径。上述因素综合作用, 导致晚渐新世四川盆地东北边缘产生新的河流切口引发长江三峡贯通(图 4-e, 4-f)。同位素研究表明, 24 Ma之后红河流域与上扬子地区失去联系, 这很可能与晚渐新世古长江中上游被下游袭夺有关(Clift et al., 2006, 2008)。

早中新世, 东亚季风体系逐步确立(Sun and Wang, 2005; Yao et al., 2011), 湿润化的气候加剧了侵蚀作用, 四川盆地剥蚀强烈(图 8-g, 8-h), 中国东部地形持续降低, 长江中下游流域进一步扩张(图 4-f, 4-g)。晚中新世青藏高原快速隆升, 下地壳管道流向东部川滇地块强烈挤出(Clark and Royden, 2000; Schoenbohm et al., 2006), 导致云贵高原快速抬升(王国芝等, 2004), 长江进一步向上游扩展并在不早于中新世进入云贵高原(图 4-h)。沉积学研究表明江汉盆地新沟、周老钻孔中第四纪地层沉积物磁化率大幅提高, 这是大量铁磁性物质的输入的结果(Zhang et al., 2008)。现代长江水系碎屑矿物研究表明长江流域仅金沙江段沉积物重矿物含量超过5%, 且绝大多数为铁磁性矿物, 而长江其他支流沉积物重矿物含量显著低于金沙江段(王中波等, 2006), 而江汉盆地第四纪地层磁化率大幅提升可能与长江进入云贵高原有关。

由此, 作者推测, 长江三峡的贯通方式具体表现为: 四川盆地西南向水系消亡、新生东向水系进入江汉盆地并被中国东部原有水系捕获形成统一流域。

6 结论

本研究利用Badlands古地貌模拟软件, 动态重建了长江“ 第一弯” 以东地区、晚白垩世(80 Ma)以来的长江流域地貌及水系演化过程。基于模型结果, 探讨了长江长江水系的演化过程和三峡贯通机制, 主要结论如下:

1)新生代以来, 扬子板块东西部各自独立发育河流系统, 它们是构成现代长江的重要组成部分。晚渐新世(约26 Ma), 东、西河流系统在湘鄂西褶皱带北部三峡地区发生贯通, 成为现代长江形成的标志性事件。

2)长江三峡的贯通是四川盆地水系反转和江汉盆地持续低基准面的共同作用。印度— 欧亚板块碰撞导致的青藏东南缘及上扬子西南部的快速隆升, 迫使原四川盆地南向排水系统消亡, 同时沉积物排泄受阻在盆内堆积形成冲积河流系统并引发地貌变为“ 西南高东北低” ; 中国东部裂陷活动持续进一步破坏原有高原地貌, 并大幅降低区域(包括江汉盆地在内)基准面。上述作用共同导致长江三峡在晚渐新世贯通。

(责任编辑李新坡; 英文审校徐杰)

参考文献

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