松花江吉林段河流沉积物碎屑锆石U-Pb年龄特征及地质意义
doi: 10.19762/j.cnki.dizhixuebao.2024433
倪倩1 ， 郭令芬1,2 ， 谢远云1,2 ， 孙磊1 ， 迟云平1,2 ， 刘海金1 ， 魏振宇1 ， 汪烨辉1 ， 吴鹏3
1. 哈尔滨师范大学地理科学学院，黑龙江哈尔滨， 150025
2. 哈尔滨师范大学寒区地理环境监测与空间信息服务黑龙江省重点实验室，黑龙江哈尔滨， 150025
3. 湖南科技大学地球科学与空间信息工程学院，湖南湘潭， 411201
基金项目: 本文为国家自然科学基金项目(编号42171006)和黑龙江省自然科学基金项目(编号ZD2023D003)联合资助的成果
U-Pb age characteristics and geological significance of the detrital zircon in the sediments of the Songhua River, Jilin Province
NI Qian1 ， GUO Lingfen1,2 ， XIE Yuanyun1,2 ， SUN Lei1 ， CHI Yunping1,2 ， LIU Haijin1 ， WEI Zhenyu1 ， WANG Yehui1 ， WU Peng3
1. College of Geographic Science, Harbin Normal University, Harbin, Heilongjiang 150025 , China
2. Heilongjiang Province Key Laboratory of Geographical Environment Monitoring and Spatial Information Service in Cold Regions, Harbin Normal University, Harbin, Heilongjiang 150025 , China
3. College of Earth Science and Space Information Engineering, Hunan University of Science and Technology, Xiangtan, Hunan 411201 , China
摘要
河流在源-汇系统中发挥着重要的纽带作用，其沉积物是源-汇系统物源分析的关键切入点。河流碎屑锆石U-Pb年龄对于水系演化、物源示踪和源-汇研究中得到广泛应用。然而，高纬度地区河流碎屑锆石U-Pb年龄分布的影响因素及其在物源示踪研究中的代表性等还没有得到充分评估，很可能导致结果不一致进一步影响源-汇系统的建立。为此，本文以松花江吉林段为研究对象，通过对6个河流沉积物共780个锆石U-Pb年龄进行分析，利用逆向蒙特卡罗模型进行定量约束。结果表明，样品的锆石U-Pb年龄分布主要有三组峰：2500 Ma、250 Ma、180 Ma，且从上游至下游，锆石年龄分布型式发生明显变化。其中，上中游河段来自华北克拉通东北缘的特征年龄2500 Ma的锆石占比发生明显下降，推测由于丰满水库的拦截作用以及远离源区的河流搬运作用所致。中游至下游河段华北克拉通东北缘贡献占比持续下降，松嫩及张广才岭地块的贡献增大，显示了河流搬运过程中新物源的加入。松花江干流河段，嫩江带来的大量小于250 Ma的锆石颗粒稀释了第二松花江2500 Ma的锆石年龄特征。在源-汇系统研究时，不同河段的物源信号存在差异，甚至上游的物源信号在下游可能缺失，用河流河口的碎屑锆石或单个样品的碎屑锆石年龄数据代表整个集水区的物源信息存在一定的不确定性。此外，松花江吉林段的年龄峰值与中亚造山带东部构造岩浆热事件吻合良好，2500 Ma可能是对华北克拉通微陆块合并的记录，250 Ma、180 Ma分别响应古亚洲洋闭合和古太平洋板块的俯冲过程。本研究对理解松花江吉林段源-汇过程具有重要意义，也为东北地区构造事件提供重要的参考价值。
Abstract
Rivers play an important role in source-to-sink systems, with their sediments serving as key entry points for provenance analysis. U-Pb dating of detrital zircon in river sediments has become a widely used tool for studying drainage evolution, provenance tracing, and source-to-sink relationships. However, the factors influencing the U-Pb age distribution of fluvial-detrital zircons in high-latitude regions and their representation in provenance tracing studies have not been fully evaluated. This can lead to inconsistent results and potentially affect the accurate establishment of source-to-sink systems. This study focuses on the Jilin section of the Songhua River, analyzing a total of 780 zircon U-Pb ages from 6 river sediment samples, and quantitative constraints were applied using an inverse Monte Carlo model. The results reveal three dominant zircon U-Pb age peaks: 2500 Ma, 250 Ma, and 180 Ma. Additionally, the age distribution pattern of zircons shows significant variations from upstream to downstream. Specifically, the proportion of zircons with a characteristic age of 2500 Ma, derived from the northeastern margin of the North China Craton, decreases markedly in the upper and middle reaches. This suggests that the increased contribution of new provenance sources in the middle reaches has diluted the provenance signal from the upper reaches, potentially influenced by the interception effect of the Fengman Reservoir. Furthermore, the contribution from the northeastern margin of the North China Craton continues to decline in the middle to lower reaches, while the contribution from the Songnen and Zhangguangcai Range blocks increases, indicating the addition of new provenance sources during river transport. In the main stream of the Songhua River, a significant influx of zircon particles younger than 250 Ma, carried by the Nenjiang River, dilutes the 2500 Ma age signature characteristic of zircons from the second Songhua River. This study highlights that provenance signals vary significantly across different river reaches, and signals present in the upper reaches may be missing in the lower reaches. Consequently, using detrital zircon age data from river estuaries or a single sample to represent the provenance information of an entire catchment introduces some degree of uncertainty. In addition, the peak ages observed in the Jilin section of the Songhua River align with the tectono-magmatic thermal events of the eastern Central Asian Orogenic Belt. The 2500 Ma peak may represent of the consolidation of the North China Craton microcontinent, while the 250 Ma and 180 Ma peaks correspond to the closure of the Paleo-Asian Ocean and the subduction of the Paleo-Pacific Plate, respectively. This study provides significant insights into the source-to-sink processes in the Jilin section of the Songhua River and offers valuable reference data for understanding tectonic events in Northeast China.
源-汇系统是剥蚀地貌（源）和沉积地貌（汇）两个宏观的地貌单元空间上相互依存、时间上持续进行物质迁移与交换的过程。该系统具有整体性和定量性特征（陈星渝等，2024），并且是地球系统科学领域的重要研究热点（Romans et al.，2016；Li Chao et al.，2016；Pan Baotian et al.，2016；Ji Hongyu et al.，2022）。在源-汇系统中，河流扮演着关键的纽带角色，是物源分析的核心切入点（林旭等，2020; 刘海金等，2021）。现代河流沉积物作为主要水系流域的代表样本，由于其地质、地貌和气候条件相对透明，因此成为源-汇系统研究中最为直接且便捷的研究对象（梁文栋和胡修棉，2023）。
锆石（ZrSiO4）是现代河流碎屑物质中常见的副矿物，其物理化学性质极为稳定且封闭温度较高，因此能够有效地捕获河流系统地质历史中的重要信息（Barham et al.，2019）。河流沉积物的碎屑锆石U-Pb年代学被广泛用于定量物源分析（如Alizai et al.，2011；Krippner and Bahlburg，2013；Lin Xu et al.，2024）以及古水系演化的重建（如Nie Junsheng et al.，2015；Blum，2019；Wang Licheng et al.，2022；He Jie et al.，2023；林旭等，2024）。此外，由于锆石保存了地质时间尺度上的主要年龄和地球化学数据，也常被用于重建区域构造历史（Yang Jie et al.，2009; Pepper et al.，2016; 李兆等，2016; Malaviarachchi et al.，2019）。近年来，对我国的河流沉积物碎屑锆石U-Pb年代学的研究主要集中于长江、黄河、珠江等大型河流（Wang Wei et al.，2019；He Jie et al.，2020；Guo Rujun et al.，2021；林旭等，2022；Lin Xu et al.，2024），对高纬度东北地区松花江吉林段研究相对较少。值得注意的是，很多研究选择用河口样本来代表次级河流的集水区（Alizai et al.，2011；Yang Shouye et al.，2012；Choi，et al.，2016；Zhu Ziyi et al.，2023），但也有研究对河口沉积物的代表性表示质疑（Castillo et al.，2022）。次级河流的河口样品是否能作为集水区代表、河流过程中的潜在影响是否存在，又如何影响沿线沉积物的组成和锆石年龄还有待商榷（郭佩等，2017；Chew et al.，2020；王亚东等，2022；王平等，2022；Gregory et al.，2022）。
松花江吉林段作为松花江主要支流之一，是研究构造-气候-地表过程的天然实验室（Wu Peng et al.，2020）。先前对该地区的研究主要基于重矿物和元素地球化学等方法，旨在重建松花江水系的反转演化历史（Xie Yuanyun et al.，2020; 魏振宇等，2020; 李思琪等，2022; 徐园园等，2022）。然而，基于碎屑锆石U-Pb年代学的河流沉积物研究尚显不足。尽管李明（2010）和 Sun Lei et al.（2023）的研究揭示了吉林段松花江碎屑锆石年龄的变化，但具体原因尚未得到深入探讨。
因此，本文以松花江吉林段中下游的现代河流沉积物为研究对象，进行碎屑锆石U-Pb年龄分析，结合已报道的其他河段数据，讨论河流碎屑锆石U-Pb年龄中物源信号的空间变化及其影响因素。此外，通过与河流流经地层的锆石U-Pb年龄数据进行对比，进行物源正演分析，以揭示松花江吉林段的源-汇过程，为东北地区构造环境演化提供约束。本研究对了解中国东北现代河流的源-汇过程及水系形成演化具有重要意义。
1 研究区域概况
松花江吉林段（42°1′N~45°25′N；124°39′E~128°E）是松花江的南缘（正源）支流，流域面积73400 km2，全长795 km，河网密度低，受到支流的影响有限。该段发源于长白山天池西北侧，由南向北分为上游段（源头—丰满水库）、中游段（丰满水库—沐石河口）以及下游段（沐石河口—三岔口）三个河段。在三岔口处，松花江吉林段和嫩江汇合，形成干流段（郭付友，2017）。上游地区基岩裸露，落差大，属于山区型河道。丰满水库（又名松花湖）是位于上游下段的大型人工河谷水库，建于1937年，总库容103.77亿m3，该水库对沉积物的输送以及大坝上游和下游河流的水动力的影响不容忽略（Zhang Jinyue et al.，2012）。
松花江吉林段流域在构造上位于中亚造山带（CAOB）的东部（图1a），其源头位于华北克拉通的东北缘，流经松嫩地块单元（董玉等，2022）。松嫩地块可进一步划分为东北地区中部的松辽盆地、东北部的小兴安岭以及东部的张广才岭。松辽盆地形成于中生代晚期，是典型的大型中生代—新生代陆相沉积盆地（图1b），基底由弱变质的古生代花岗岩、沉积岩和中生代花岗岩构成（Gao Fuhong et al.，2007; Pei Fuping et al.，2007）。南部的古元古代变质花岗岩和变质辉长岩通常被认为是华北克拉通推覆至此的构造岩片（张艳斌等，2004）。张广才岭和小兴安岭主要以大量显生宙花岗岩为主，罕见新元古代片麻花岗岩出露，其中显生宙花岗岩可细分为三个阶段：早古生代、二叠纪和早中生代（Wang Feng et al.，2014; Luan Jinpeng et al.，2022）。张广才岭的地质体主要为二叠纪至侏罗纪花岗岩（权京玉，2013）。东北地区丰富的地质多样性为该区河流源-汇过程的研究提供重要的背景支持。
2 样品采集与实验方法
2.1 样品采集
本文在吉林段松花江干流采集6个现代河流沉积物样品（AB-71、AB-64、AB-80、AB-81、AB-82、AB-83），为避免样品污染，采样地点选择远离人类活动的区域（图1c）。此外，还收集已发表的松花江流域碎屑锆石年龄数据集，包括SHJ1、SHJ2、SHJ3、SHJ4、JL1和SN1（李明，2010; Sun Lei et al.，2020）。本研究中采集的所有样品均经过干筛处理，以获得63~250 μm的组分，用于碎屑锆石年龄分析。这种筛分方法有助于减少由于流体动力分选和粒度依赖引起的粒度效应偏差（Morton et al.，1994）。
图1中亚造山带大地构造简图（a，据Zhou Jianbo et al.，2010修改）、中国东北地区地质简图（b，据梁乾坤等，2023修改）及松花江吉林段流域地势地貌及样品位置分布图（c）
Fig.1Schematic tectonic map of the Central Asian Orogenic Belt (a, after Zhou Jianbo et al., 2010) , simplified geological map of NE China (b, after Liang Qiankun et al., 2023) and the landscape of the Songhua River basin in Jilin section and the sample location (c)
2.2 碎屑锆石U-Pb年代学
锆石的制靶、阴极发光图像拍摄及锆石U-Pb同位素测试分析均在河北廊坊市诚信地质服务有限公司完成。首先采用传统的重液法和磁性分离技术从子样品中分离出碎屑锆石。在双目显微镜下手工挑选进一步纯化，每个样品随机选择300个锆石颗粒粘贴在无色透明的环氧树脂上，通过磨砂抛光使内部纹理完全暴露。然后通过扫描电子显微镜拍摄阴极发光（cathodoluminescence，CL）图像，结合反射光和透射光下的图像，分析其内部结构。
使用德国Analytik Jena AG公司PlasmaQuant MS elite四级杆质谱仪和美国NewWave公司193 nm激光剥蚀系统（NWR193）对这些颗粒进行U-Pb年代测定分析。仪器采用人工合成硅酸盐玻璃参考标准NIST SRM 610进行校准，激光光斑直径为25 μm，频率为12 Hz，采用单点剥蚀模式，氦气作为载气。每个年龄数据的误差在1σ范围内。对于年龄小于1000 Ma和大于1000 Ma的锆石，分别使用206Pb/238U年龄和207Pb/206Pb年龄进行测定。谐和度超出90%至110%的锆石颗粒被排除。使用基于R语言的IsoplotR程序绘制核密度估计图（Kernel Density Estimates，KDE）进行可视化分析，并通过多维尺度分析（MDS）量化锆石年龄的相似性与差异性。主要通过基于K-S检验的D值的结果，将高维度数据以点的形式在二维空间中投射，通过欧几里得距离量化数据的相似性或差异性，实现样本的相似性的高水平可视化的空间表达。谢帕德图（Shepard plot）和应力值stress是用于评估 MDS 转换结果的拟合度的两种方式，谢帕德图（Shepard plot）中点位越接近 1∶1线或应力值越接近零说明MDS结果拟合越好（张凌等，2020）。
2.3 碎屑锆石混合模型
Amidon et al.（2005）首次建立了河流沉积物正演混合模型，用于分析、模拟和重构河流流域内的沉积物来源及物源，从而推断沉积过程和物源贡献机制。本文采用DZmix碎屑地质年代数据定量混合模型，该模型在Matlab Runtime环境中运行，带宽值设置为30，通过连续迭代10000次确定最佳拟合曲线，并通过相关系数R2与目标样本进行定量比较，为最佳拟合结果提供平均值和不确定性（Sundell and Saylor，2017）。在吉林段松花江中，潜在物源包括华北克拉通北缘东段、张广才岭、松辽盆地南部以及嫩江。将吉林段松花江河流沉积物样品划分为上游段、中游段、下游段以及松花江干流段，分别作为建模目标样本，输出源样本的模拟贡献率，其总和为1（Shang Yuan et al.，2021）。
3 研究结果
通过阴极发光（CL）图像分析，大部分锆石颗粒呈次圆形，自形程度较差，且大多数锆石发育有清晰的振荡环带或条形分带结构（图2），属于典型的岩浆成因锆石特征。锆石的Th/U比值总体范围为0.01~5.29，如图3所示，97%的大碎屑锆石的Th/U比值大于0.1，综合判断松花江吉林段河流沉积物中的锆石主要为岩浆成因锆石，可以指示源区相应的岩浆热力事件。通过对本研究采集的6件松花江吉林段沉积物样品中碎屑锆石进行LA-MC-ICP-MS U-Pb年龄测定，获得780个谐和度在90%至110%范围之内的数据（附表1，附表2）。分析结果以核密度估计图（Kernel Density Estimate，KDE）的形式展示（图4）。位于中游的AB-71、AB-64、AB-80、AB-81主要峰值为2542 Ma、2536 Ma、2477 Ma、2454 Ma、182 Ma、176 Ma，次要峰值为252 Ma、246 Ma；位于下游的AB-82、AB-83主要峰值为2501 Ma、2519 Ma、182 Ma，次要峰值为252 Ma、246 Ma。综合来看，来自不同河流沉积物样品的年龄谱具有共同特征，年龄谱分布具有显著多峰态特征，主要峰值为180 Ma（侏罗纪）、250 Ma（三叠纪）和2500 Ma（太古宙）。年龄数据主要集中在以下三段范围： 2880~2030 Ma、364~207 Ma和205~101 Ma。
图2松花江吉林段河流沉积物碎屑锆石CL图像
Fig.2CL image of river sediment detrital zircon in the Jilin section of the Songhua River
图3松花江吉林段河流沉积物碎屑锆石U-Pb年龄与Th/U比值分布图
Fig.3U-Pb ages and Th/U ratios of analyzed detrital zircons in the sediments of the Jilin section of the Songhua River
4 讨论
4.1 松花江吉林段碎屑锆石U-Pb年龄的空间变化
本研究在松花江吉林段中下游采集的河流沉积物样品的碎屑锆石年龄谱分布差异不明显，显示出相似的年龄峰值，反映流域内碎屑沉积物的总体成分，表明了河漫滩沉积物的混合和平均效应（Yang Shouye et al.，2012）。图5展示了本研究及其他研究的河流沉积物样品碎屑锆石年龄比例变化的折线图与百分比柱状图。在松花江吉林段上游段（样品AB-SHJ4），中生代和新生代锆石占比为15.75%，古生代和元古宙锆石占比为3.15%，太古宙锆石占比为81.10%；中游段（样品AB-71、AB-64、AB-80、AB-81和JL1）中生代和新生代锆石占比上升至47.57%，古生代和元古宙锆石占比为12.01%，太古宙锆石下降至40.42%；下游段（样品SHJ1、AB-82、AB-83）中生代和新生代锆石占比达到52.80%，古生代和元古宙锆石占比为12.32%，太古宙锆石下降至34.88%；松花江干流段中生代和新生代锆石占比上升至72.40%，古生代和元古宙锆石占比为19.14%，太古宙锆石减少至8.45%。总体趋势表明，从上游段到松花江干流段，中生代和新生代（＜250 Ma）锆石的比例在下游显著增加；古生代和元古宙锆石的比例缓慢增加；太古宙锆石（＞2500 Ma）的比例则显著下降。添加报道过的流域内其他河段的锆石年龄数据后（李明，2010; Sun Lei et al.，2020），虽然碎屑锆石年龄分布相似，但年龄组合比例在下游表现出显著的变异性（图5），进一步揭示下游信号传播的复杂性，反映河流系统处于不断的动态变化中。
图4松花江吉林段河流沉积物碎屑锆石U-Pb年龄KDE图解
Fig.4KDE plots of detrital zircons in the sediments of the Jilin section of the Songhua River
图5松花江吉林段河流沉积物碎屑锆石U-Pb 年龄百分比变化
Fig.5Change in percentage age of detrital zircon U-Pb in the Jilin section of the Songhua River
4.2 松花江吉林段碎屑锆石U-Pb年龄物源分析的影响因素
源-汇系统研究的核心在于揭示沉积物所记录的物源信息与地质信号在时空维度上的传递与耦合机制（Armitage et al.，2011）。基于碎屑锆石年代学的验证与机理研究表明，在利用碎屑锆石U-Pb年代学进行物源分析时，锆石年龄分布特征不仅受控于源区属性，还可能受到多种潜在因素的影响，这些因素往往容易被忽视，从而导致河流沉积物物源判别结果的偏差。（Malusà et al.，2013；Condie et al.，2017；Ahmadet al.，2019；Caracciolo，2020；Markwitz et al.，2020），甚至可能导致上游的物源信息在下游缺失（Jackson et al.，2019；Thomson et al.，2022）。人为偏差主要体现在采样分析方法上的差异，随着科学技术的革新已经得到完善和统一（Spencer et al.，2016；张凌等，2020；陈玺贇，2022），其次就是人类社会活动对河流过程的改造（Shang Yuan et al.，2021；Gregory et al.，2022）。自然偏差主要来源于锆石丰度（Moecher and Samson，2006；Chew et al.，2020）、水动力分选（Lawrence et al.，2011）以及锆石再循环（Dröllner al.，2023；宋仁龙等，2024）等，本文采用了63~250 μm级宽窗口策略有效的减弱水动力分选导致的粒度效应的影响（Morton et al.，1994）；已有研究利用元素地球化学方法证明松花江吉林段的沉积物再循环程度较低，因此也可以排除锆石再循环的影响（Qi Haodong et al.，2025）; 由于流域源岩类型差异不大，中下游地势相对平坦，本文假设侵蚀均匀，源岩锆石丰度相近（He Mengying et al.，2014）。为便于分析松花江吉林段锆石年龄变化的内在机制并估计潜在源区对吉林段的贡献，本研究以样品SHJ4碎屑锆石年代数据代表吉林段松花江上游段的组成；样品AB-71、AB-64、AB-80、AB-81和JL1的碎屑锆石年代数据代表吉林段松花江中游段的组成；样品SHJ1、AB-82和AB-83组合代表吉林段松花江下游段的组成；SN1、SHJ2、SHJ3组合代表松花江干流段的组成。运用多维尺度分析（MDS）图谱分别显示样本与潜在物源之间的关系（图7a），应力值sterss等于0.012，小于0.025，并且谢帕德图（Shepard plot）中点位与1∶1线较接近，说明匹配度良好（图7b）。
图6本研究及前人研究中松花江吉林段的河流沉积物碎屑锆石年龄KDE图解（a~f；i~n）及潜在源区的碎屑锆石U-Pb年龄KDE图解（g、h、o、p）
Fig.6KDE diagrams of detrital zircon ages from river sediments in the Jilin section of the Songhua River from this and previous studies (a~f; i~n) and KDE plots for potential source areas (g, h, o, p)
张广才岭火成岩锆石年龄数据引自敖光，2016；句高等，2018；李翱鹏等，2019；赵越等，2021；Xue Yiting et al.，2024; 刘昊等，2024；华北克拉通东北缘火成岩锆石年龄数据引自Wang Ying et al.，2006；秦亚等，2014；张宏涛，2017；Wang Yini et al.，2018；张笑鸣，2021；玄雨菲等，2022；邢恺晨，2023；李忠水，2023；松嫩地块南部火成岩锆石年龄数据引自Pei Fuping et al.，2011；Wang Zijin et al.，2015；张海洪等，2016；宋健等，2017；Wang Hongyan et al.，2022；邢恺晨，2023；嫩江河流沉积物锆石年龄数据引自李明，2010
Igneous zircons age data in Zhangguangcai Range from Ao Guang, 2016; Ju Gao et al., 2018; Li Aopeng et al., 2019; Zhao Yue et al., 2021; Xue Yiting et al., 2024; Liu Hao et al., 2024; igneous zircons age data in northeastern NCC from Wang Ying et al., 2006; Qin Ya et al., 2014; Zhang Hongtao, 2017; Wang Yini et al., 2018; Zhang Xiaoming, 2021; Xuan Yufei et al., 2022; Xing Kaichen, 2023; Li Zhongshui, 2023; zircon age data of igneous rocks in the southern part of the Songnen massif are cited from Pei Fuping et al., 2011; Wang Zijin et al., 2015; Zhang Haihong et al., 2016; Song Jian et al., 2017; Wang Hongyan et al., 2022; Xing Kaichen, 2023; the age data of zircon sand in the Nenjiang River are quoted from Li Ming, 2010
4.2.1 上游段—中游段
目视判别结果表明，除华北克拉通外，前寒武纪年龄锆石在其他潜在物源的年龄谱中明显缺乏（图6）。逆向蒙特卡罗模型的定量结果（表1）显示，在上游段（源头—丰满水库），华北克拉通的贡献最大，达到98%。松花江吉林段自源头至两江口，穿过长白山山地，流速较大，裸露的河床提供丰富的沙物质来源。MDS图也显示，上游段样品与华北克拉通之间存在较强的亲缘性（图7）。2500 Ma年龄峰值常作为华北克拉通来源的示踪指标，在松花江吉林段源头广泛存在。然而，在中游段，华北克拉通的贡献占比下降至67.7%，张广才岭的贡献占比则增加至30.7%。碎屑锆石年龄谱的最明显变化是太古宙锆石的U-Pb年龄组分逐步下降，特别是在丰满水库上游的样品SHJ4和丰满水库下游的样品AB-71中，太古宙锆石的比例显著下降（图5）。推测这种变化主要方面由于中游新来源锆石的稀释作用所致，太古宙锆石主要在上游源头华北克拉通东北缘大量富集，中游流经的松嫩地块主要为大型中生代—新生代陆相沉积，与源区相比张广才岭与松辽盆地的太古宙基底特征年龄缺乏，经过第二松花江的搬运作用，与华北克拉通东北缘距离越来越远，源区贡献能力有限，张广才岭的贡献上升，随着二叠纪至侏罗纪年龄锆石不断输入，稀释了太古宙锆石的贡献占比；次要方面很可能与丰满水库有关，水库可能改变松花江吉林段流域的侵蚀格局，破坏沉积物的连续性，从而影响现代河流泥沙的碎屑锆石年龄分布（Moore et al.，2021; Thomson et al.，2022）。河流经过水库后，粗泥沙率先沉积，悬浮物被进一步输送并沉降到水库底部，从根本上改变上游和下游河流的泥沙输送和水动力。当水库开闸放水时，沉积物含量相对较低且的水流从大坝出水口排出，导致下游河流阶地或河道被切割和侵蚀，使河道变宽变硬，碎屑锆石年龄特征有所改变。部分河道沉积物可能会再次出现，但由于缺乏来自华北克拉通的物源供给，2500 Ma年龄峰值相比水库前依然显著下降。最终，河流剖面根据大坝的存在进行调整，并在大坝下游建立了一个新的剖面（图8）。
图7松花江吉林段及其潜在源区的 MDS判别结果（a）及谢帕德图（b）
Fig.7Multidimensional scaling (MDS) (a) and Shepard plot (b) plots for the Jilin section of the Songhua River sediments and potential source areas
SN—松嫩地块；ZGCL—张广才岭；NCC—华北克拉通东北缘；NJ—嫩江
SN—Songnen block; ZGCL—Zhang Guangcai Range; NCC—northeast margin of North China craton; NJ—Nenjiang River
4.2.2 中游段—下游段
中游段地貌类型属于低山丘陵，下游段地貌类型为低洼平原，相较于上游段，河道较弯曲且坡度相对平缓，意味着稳定的沉积物运输占主导（曹小磊，2017）。华北克拉通的贡献持续下降，而松嫩地块和张广才岭的贡献上升，至下游段，华北克拉通的贡献下降至60.7%，松嫩地块和张广才岭的贡献分别上升至1.8%和37.4%（表1）。下游样品中的二叠纪至侏罗纪U-Pb年龄分布与流域中暴露的火成岩单元的年龄相匹配，包括松嫩地块南部和张广才岭（图6）。这表明，随着河流搬运距离的增大及物源混合作用，来自松花江吉林段上游的物源信号随着集水区暴露地层变化而变化。MDS图也显示下游样品与松嫩地块的亲缘关系逐渐加近，体现了松嫩地块物源的贡献（图7a）。特别是靠近第二松花江河口的样品AB-83与上游段样品SHJ4的碎屑锆石年龄比例变化显著，揭示物源的空间异质性。
表1松花江吉林段河流沉积物定量物源混合贡献比例重建结果
Table1Results of quantitative reconstruction of provenance in the Jilin Songhua river sediments based on inverse Monte Carlo modeling
4.2.3 下游段—干流段
下游段在三江口与嫩江汇合为干流段，在干流段的逆向蒙特卡罗模型的定量分析中，将嫩江作为潜在物源之一纳入模型，结果显示嫩江、华北克拉通、张广才岭和松嫩地块南部的物源贡献分别为53.9%、15.9%、18.6%和11.0%（表1）。MDS分析结果显示，此时干流段与华北克拉通的亲缘性较弱，与嫩江、松嫩地块南、张广才岭亲缘关系较近（图7a）。下游段的样品AB-83大于250 Ma比例为64.23%，嫩江汇入后，干流段第一个样品SN1的锆石年龄大于250 Ma比例达到了83.90%（图5）。前人研究收集的嫩江下游样品的年龄谱主要集中于100~200 Ma（李明，2010），推测下游段至干流段物源信号的变化主要由于第二松花江与嫩江在两江口的汇合，新来源的锆石不断输入，从而迅速掩盖和稀释了源头碎屑锆石的年龄特征（图8）。
4.3 碎屑锆石年龄U-Pb年代学物源分析的启示
在理想条件下，源区的碎屑应完全输送到汇区。实际上，由于老沉积物的改造和新沉积物的加入，河流沉积物的成分在沿河流下游会发生变化。松花江吉林段河流沉积物碎屑锆石U-Pb年龄分布比例的变化揭示了下游信号传播的复杂性。上游中华北克拉通特有的2500 Ma信号在中游腹地被显著削弱。河流沉积物是非静态的，在河流搬运过程中受到物理和化学风化/侵蚀、水动力分选、额外支流的稀释、局部侵蚀及人为活动的影响，其成分组成会向下游不断变化，某些成分含量可能会增多某些成分也可能会减少。这些因素导致碎屑锆石年龄谱的解释和物源判别存在一系列的偏差（Amidon et al.，2005；Ahmad et al.，2019）。
本文研究结果提供了物源分析的三点有意义的启示。首先，河流沉积物的贡献不仅包括源区的岩石，还包括集水区暴露地层的贡献，暴露地层的非均质分布会导致局部地层对某些年龄的局部贡献（Cawood et al.，2003；Zhang Jinyu et al.，2012；He Mengying et al.，2014）。其次，人类活动如大坝建设会减少沉积通量，从而削弱物源信号，但农业活动或采矿等活动则可能增加沉积物通量。最后，支流的汇入可能会稀释物源信号。综上，松花江吉林段作为大河流域的重要河段，其物源信号从上游至河口发生了显著变化。在源-汇系统研究时，用河流河口的碎屑锆石或单个样品的碎屑锆石年龄数据代表整个集水区的物源信息存在一定不确定性，需谨慎使用。
4.4 碎屑锆石揭示的区域构造岩浆事件
地壳生长的时期往往伴随着与深部地幔相关的岩浆活动，锆石的U-Pb年龄反映了锆石在750℃左右结晶的时间，一些古老的岩石由于风化作用很难获取地壳信息，幸运的是，现代河流沉积物碎屑锆石能够为大陆地壳中保存的岩浆和地壳形成事件提供了可靠的记录（Condie et al.，2009；Hawkesworth et al.，2010；Cawood et al.，2012；陈岳龙等，2014）。本研究中CL图像和锆石Th/U比值（图2和图3）表明，吉林段松花江采集的河流沉积物样品的碎屑锆石绝大多数为岩浆成因，这些数据有效地反映了中亚造山带东部地区的一些岩浆事件。研究区域主要分布在吉林省南部，其构造演化历史较为复杂。该区域构造上归属于中亚造山带的东段，东侧与太平洋板块相接，北侧则通过鄂霍茨克缝合带与西伯利亚板块相邻，南面则以索伦克尔-西拉木伦-长春-吉缝合带为界，与华北克拉通相毗连。在古亚洲洋构造域、蒙古-鄂霍茨克洋及环太平洋构造体系的影响下，以及在扬子克拉通与华北克拉通的叠加和改造作用的共同作用下（Yang Jihu et al.，2007；唐杰等，2018；Wang Feng et al.，2019a，2019b），几个具有不同构造属性的微陆块进行了拼接，并经历了一系列的岩浆活动和变质过程（刘永江等，2022；董玉等，2022）。
图8丰满水库坝对下游碎屑锆石 U-Pb 年龄谱可能产生的影响示意图（据王平等， 2022修改）
Fig.8Effect of dams on the downstream detrital zircon age signals (after Wang Ping et al., 2022)
2880~2030 Ma：吉林段河流沉积物中的太古宙年龄峰值与华北克拉通微块体合并形成克拉通的主要时期高度吻合。第二松花江发源于吉林省南部的长白山山地，位于华北克拉通北缘东段的龙岗陆块。作为主要古老克拉通之一，华北克拉通的形成及构造演化被广泛研究（Wang Yini et al.，2018；李鹏川，2019；高天宇，2019；邢恺晨，2023；李忠水，2023）。现有研究表明，华北克拉通的前寒武纪基底中，有超过80%的部分由新太古代（约2600~2500 Ma）形成的岩石构成。这一时期被认为是华北克拉通地壳发育的主要阶段。（Liu Xiaoming，2008；Yang Jie et al.，2009；Gao Shan，2009；耿显雷等，2011；Zhao Guochun and Zhai Mingguo，2013），华北克拉通最早的地壳吸积发生在约2700 Ma，由七个微陆块构成（Zhai Mingguo et al.，2000）。在2500 Ma，所有微陆块可能由新太古代绿岩带拼合成一体，此时发生了广泛的变质作用和岩浆岩的侵入，标志着华北克拉通基本构造框架建立。前人研究报道的锆石数据中显示的各区块发生的花岗岩岩体侵入作用和新太古代变质作用也支持这一论点（翟明国，2004；Zhai Mingguo et al.，2010；Wan Yusheng et al.，2012）。
364~207 Ma：该年龄段河流沉积物碎屑锆石的峰值主要集中在约250 Ma，二叠纪—三叠纪岩浆活动在松嫩地块南部广泛发育，这一岩浆活动可能与中国东北地区古亚洲洋的闭合有关。晚二叠世至早三叠世，古亚洲洋从西到东呈剪刀状闭合，西伯利亚克拉通发生顺时针旋转，与华北克拉通沿索伦—西拉木伦—长春一线碰撞拼贴（Wu Fuyuan et al.，2007，2011；Guan Qingbin et al.，2018；李韶凯等，2020）。在这一过程中，西伯利亚克拉通边缘的复合块体下部岩石圈地幔物质熔融，开始出现伸展性质的A型花岗岩（Wu Fuyuan et al.，2003；李梦琪，2023）。中三叠世，吉林省东部的古亚洲洋的闭合完成（Chen Bin et al.，2000；Wang Zijin et al.，2015；Du Qingxiang et al.，2019）。伸展作用将持续到晚三叠世，造成的垮塌事件也影响到了张广才岭和小兴安岭地区（Tang Jie et al.，2018），现今东北内部各区域分布的280~210 Ma的岩浆事件多与造山后的伸展环境有关。
205~101 Ma：河流沉积物碎屑锆石所记录的年龄主要峰值在180 Ma（早侏罗世）。中亚造山带东部在中生代的构造演化特征包括造山运动后的伸展以及古太平洋构造体系与蒙古-鄂霍次克构造体系的叠加（Liang Yong et al.，2022）。在中亚造山带的花岗岩中，侏罗纪和白垩纪的花岗岩数量最多、分布最广（Wu Fuyuan et al.，2003；Wilde，2015；龙欣雨，2023）。前人对松嫩地块早侏罗世的侵入岩进行了大量报道（Wu Fuyuan et al.，2002；彭玉鲸等，2007；Wu Fuyuan et al.，2007；葛文春等，2007；Yu Jiejiang et al.，2012；Guo Feng et al.，2015），这些花岗岩主要为I型花岗岩，通常来源于地壳火成岩的部分熔融伴有幔源物质的加入，指示了与大陆边缘洋壳俯冲相关的挤压环境（Wu Fuyuan et al.，2011）。此外，松嫩地块广泛分布的碳酸盐岩（浅水）与碎屑沉积物（深水）共存的现象，进一步支持了该地区可能已演化为具有岛弧性质的俯冲-吸积复合体。小兴安岭—张广才岭的东北-西南走向与古太平洋板块与欧亚板块俯冲方向近乎垂直，这一几何关系符合板块俯冲前缘应力场控制的构造相应模式，也为西北-东南向的俯冲运动提供了有力证据。综上所述，本研究中河流沉积物锆石的180 Ma年龄峰值与古太平洋板块向欧亚板块俯冲的时代一致，反映了该时期显著的构造-岩浆活动。
5 结论
本研究通过对松花江吉林段6个河流沉积物共780个锆石U-Pb年龄进行分析，利用逆向蒙特卡罗模型进行定量约束并结合MDS验证，取得结果如下：
（1）碎屑锆石年龄特征：松花江吉林段江河流沉积物样品的碎屑锆石大部分为岩浆成因，且U-Pb年龄呈多峰态分布的特征，主要集中在三段：2880~2030 Ma、364~207 Ma、205~101 Ma，峰值分别为2500 Ma（太古宙）、250 Ma（三叠纪）和180 Ma（侏罗纪）。
（2）从上游至下游，锆石年龄分布型式发生明显变化。上中游河段2500 Ma锆石占比发生明显下降，此年龄主要来自华北克拉通东北缘，推测主要由于远离源头的河流搬运作用及中游局部新物源贡献增大导致的稀释作用，其次很可能与丰满水库的拦截作用有关。中游及下游河段华北克拉通东北缘贡献占比持续下降，松嫩及张广才岭地块的贡献增大，显示了河流搬运过程中新物源的加入。松花江干流河段，嫩江带来的大量小于250 Ma的锆石颗粒稀释了第二松花江2500 Ma的锆石年龄特征。在源-汇系统研究时，不同河段的物源信号存在差异，甚至上游的物源信号在下游可能缺失，用河流河口的碎屑锆石或单个样品的碎屑锆石年龄数据代表整个集水区的物源信息存在一定风险。
（3）构造演化记录：松花江吉林段碎屑锆石U-Pb年龄对中亚造山带东段的构造演化事件有可靠的记录。2500 Ma年龄峰值对应了新太古代华北克拉通微陆块合并过程；250 Ma岩浆活动响应了古亚洲洋的剪刀状闭合以及造山后的伸展作用；180 Ma的年龄峰值与古太平洋板块对欧亚板块的俯冲事件相吻合。这些构造演化记录为东北地区构造事件提供重要的参考价值。
致谢：诚挚感谢责任编委和匿名审稿专家提出的宝贵意见和建议。碎屑锆石年龄和扫描电镜分析得到了廊坊市诚信地质服务有限公司李鹏、张云丹以及张佩萱老师的大力支持。硕士研究生赵薇、刘晓萌、孙宇佳、周莹、崔鑫诣、陶林郦、赵雅茹、张良辰、龙艺丹和孙博妍参与实验样品处理工作，在此一并表示感谢！
附件：本文附件（附表1、2）详见http://www.geojournals.cn/dzxb/dzxb/article/abstract/202509091?st=article_issue
图1中亚造山带大地构造简图（a，据Zhou Jianbo et al.，2010修改）、中国东北地区地质简图（b，据梁乾坤等，2023修改）及松花江吉林段流域地势地貌及样品位置分布图（c）
Fig.1Schematic tectonic map of the Central Asian Orogenic Belt (a, after Zhou Jianbo et al., 2010) , simplified geological map of NE China (b, after Liang Qiankun et al., 2023) and the landscape of the Songhua River basin in Jilin section and the sample location (c)
图2松花江吉林段河流沉积物碎屑锆石CL图像
Fig.2CL image of river sediment detrital zircon in the Jilin section of the Songhua River
图3松花江吉林段河流沉积物碎屑锆石U-Pb年龄与Th/U比值分布图
Fig.3U-Pb ages and Th/U ratios of analyzed detrital zircons in the sediments of the Jilin section of the Songhua River
图4松花江吉林段河流沉积物碎屑锆石U-Pb年龄KDE图解
Fig.4KDE plots of detrital zircons in the sediments of the Jilin section of the Songhua River
图5松花江吉林段河流沉积物碎屑锆石U-Pb 年龄百分比变化
Fig.5Change in percentage age of detrital zircon U-Pb in the Jilin section of the Songhua River
图6本研究及前人研究中松花江吉林段的河流沉积物碎屑锆石年龄KDE图解（a~f；i~n）及潜在源区的碎屑锆石U-Pb年龄KDE图解（g、h、o、p）
Fig.6KDE diagrams of detrital zircon ages from river sediments in the Jilin section of the Songhua River from this and previous studies (a~f; i~n) and KDE plots for potential source areas (g, h, o, p)
图7松花江吉林段及其潜在源区的 MDS判别结果（a）及谢帕德图（b）
Fig.7Multidimensional scaling (MDS) (a) and Shepard plot (b) plots for the Jilin section of the Songhua River sediments and potential source areas
图8丰满水库坝对下游碎屑锆石 U-Pb 年龄谱可能产生的影响示意图（据王平等， 2022修改）
Fig.8Effect of dams on the downstream detrital zircon age signals (after Wang Ping et al., 2022)
表1松花江吉林段河流沉积物定量物源混合贡献比例重建结果
Table1Results of quantitative reconstruction of provenance in the Jilin Songhua river sediments based on inverse Monte Carlo modeling
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