古地理学报

柴西北晚新生代沉积源区分析:来自碎屑锆石U-Pb年龄及Hf同位素的约束^*

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肖梦晗 , 郑绵平 , 张永生 , 侯献华 , 施林峰

古地理学报 | 纪念冯增昭先生百年诞辰专题 2026,28(3): 949-969

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古地理学报 |纪念冯增昭先生百年诞辰专题 2026 , 28 (3) : 949 -969

柴西北晚新生代沉积源区分析:来自碎屑锆石U-Pb年龄及Hf同位素的约束^*

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肖梦晗, 郑绵平, 张永生, 侯献华, 施林峰

作者信息

中国地质科学院矿产资源研究所, 自然资源部盐湖资源与环境重点实验室, 北京 100037

通讯作者:

张永生,男,1963年生,博士,研究员,博士生导师,主要从事盐类矿床地质与“油钾兼探”研究。E-mail: zys_601@126.com。

作者简介:

谨以此文纪念冯增昭先生诞辰100周年。

肖梦晗,女,1999年生,博士研究生,主要从事盐湖学与古地磁学研究。E-mail: xiaomenghan4869@163.com。

Provenance analysis of the Late Cenozoic sediments in Dalangtan area, northwestern Qaidam Basin: evidence from detrital zircon U-Pb ages and Hf isotopes

Menghan XIAO, Mianping ZHENG, Yongsheng ZHANG, Xianhua HOU, Linfeng SHI

Affiliations

MLR Key Laboratory of Saline Lake Resources and Environments, Institute of Mineral Resources,Chinese Academy of Geological Sciences, Beijing 100037, China

Corresponding Author:

ZHANG Yongsheng,born in 1963,Ph.D.,researcher and Ph.D. supervisor,is primarily engaged in researches on the geology of salt deposits and “oil-potash dual exploration”. E-mail: zys_601@126.com.

XIAO Menghan,born in 1999,Ph.D. candidate,is primarily engaged in researches on salinology and paleomagnetism. E-mail: xiaomenghan4869@163.com.

出版时间: 2026-06-01 doi: 10.7605/gdlxb.2026.110

文章导航

摘要

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柴达木盆地位于青藏高原东北缘,其特殊的地层岩性及沉积特征反映了复杂的盆山系统和多种物源区成因。柴达木盆地西北部大浪滩—黑北凹地发育一套巨厚的晚新生代砂砾石沉积层系,为新型“砂砾型”卤水钾盐矿赋存地层。本研究选取大浪滩地区柴钾2井、柴钾3井不同埋深的7个砂岩样品进行了碎屑锆石U-Pb年代学、锆石微量元素特征分析与Lu-Hf同位素研究。结果表明,研究区碎屑锆石以岩浆成因为主,Th/U值为0.02~1.26,稀土元素配分模式呈现重稀土元素相对富集、显著Eu负异常和Ce正异常。碎屑锆石U-Pb年龄总体介于213.9~3307 Ma之间,主要包括4组年龄,分别是: 200~300 Ma,330~510 Ma,740~990 Ma,1.1~3.3 Ga。通过与周缘潜在源区对比发现,柴钾2井七个泉组物源以东昆仑祁漫塔格为主,柴钾3井七个泉组主要受阿尔金山和柴北缘共同影响; 狮子沟组表现出更明显的多源混合特征,其中柴钾2井狮子沟组反映东昆仑祁漫塔格、柴北缘、南祁连山和阿尔金山共同供源,柴钾3井狮子沟组则以东昆仑祁漫塔格物源为主,同时接受阿尔金山和柴北缘的部分输入。总体上,柴钾2井、柴钾3井之间的物源差异反映出山前冲洪积扇相沉积体系的横向分异与晚新生代构造活动增强的共同控制。研究结果可为阿尔金山及青藏高原北缘快速隆升提供可靠的年龄证据,对探索柴达木盆地“砂砾型”含钾卤水资源提供了新的年代制约。

关键词

锆石U-Pb年龄 / Hf同位素 / LA-ICP-MS / 物源分析 / 柴达木盆地

Abstract

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The Qaidam Basin,on the northeastern margin of the Tibetan Plateau,preserves distinctive stratigraphic and sedimentary records of a complex basin-mountain system and multiple provenance sources. In the Dalangtan-Heibei sag of the northwestern basin,a thick Late Cenozoic gravel succession hosts a newly recognized gravel-type potash-bearing brine deposit. In this study,seven sandstone samples from different depths in boreholes CJ-2 and CJ-3 were analyzed for detrital zircon U-Pb geochronology,trace elements,and Lu-Hf isotopes. The detrital zircons are predominantly magmatic in origin,with Th/U ratios of 0.02-1.26 and REE patterns characterized by HREE enrichment,pronounced negative Eu anomalies,and positive Ce anomalies. U-Pb ages range from 213.9 to 3307 Ma and define four main age groups: 200-300 Ma,330-510 Ma,740-990 Ma,and 1.1-3.3 Ga. Provenance comparison shows that the Qigequan Formation in borehole CJ-2 was sourced mainly from the East Kunlun-Qimantagh,whereas that in borehole CJ-3 was influenced chiefly by the Altyn Tagh and the northern Qaidam margin. The Shizigou Formation shows stronger multi-source mixing: in borehole CJ-2 it records contributions from the East Kunlun-Qimantagh,northern Qaidam margin,South Qilian Mountains,and Altyn Tagh,whereas in borehole CJ-3 it was derived mainly from the East Kunlun-Qimantagh,with subordinate input from the Altyn Tagh and northern Qaidam margin. These inter-well provenance differences reflect the combined effects of lateral differentiation within the piedmont alluvial-proluvial fan system and intensified Late Cenozoic tectonic activity. The results can provide reliable age evidence for the rapid uplift of the Altun Mountains and the northern margin of the Tibetan Plateau,and offer new age constraints for exploring the gravel type potassium-bearing brine resources in the Dalangtan-Heibei sag of Qaidam Basin.

Key words

Zircon U-Pb dating / Hf isotopic / LA-ICP-MS / provenance analysis / Qaidam Basin

引用本文

肖梦晗, 郑绵平, 张永生, 侯献华, 施林峰. 柴西北晚新生代沉积源区分析:来自碎屑锆石U-Pb年龄及Hf同位素的约束^*. 古地理学报, 2026 , 28 (3) : 949 -969 . DOI: 10.7605/gdlxb.2026.110

Menghan XIAO, Mianping ZHENG, Yongsheng ZHANG, Xianhua HOU, Linfeng SHI. Provenance analysis of the Late Cenozoic sediments in Dalangtan area, northwestern Qaidam Basin: evidence from detrital zircon U-Pb ages and Hf isotopes[J]. Journal of Palaeogeography (Chinese Edition), 2026 , 28 (3) : 949 -969 . DOI: 10.7605/gdlxb.2026.110

正文

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柴达木盆地是青藏高原东北部最大的高海拔陆相盆地(Hanson et al., 2001;Cao et al., 2008),新生代沉积序列厚度较大,平均厚度达8 km(Xia et al., 2001)。这一沉积序列保存了柴达木盆地及周边地区新生代构造的详细证据,记录了重要的地质事件,如印度板块和欧亚板块的碰撞(Yin and Harrison,2000;Royden et al., 2008)、青藏高原的形成和隆升(Harrison et al., 1992;Clark,2011)、盆地周缘的阿尔金山、南祁连山以及东昆仑山的变形和隆升等(陈宣华等,2011;张涛等,2012;He et al., 2020;王嘉琦等,2023)。自渐新世以来,阿尔金断裂带的活动(Yin et al., 2002;Liu et al., 2003)也与柴达木盆地西北部的数次快速隆升(强挤压)、沉积几乎同时发生(Sun et al., 2010;Gao et al., 2011),这些新生代多期构造隆升事件及其剥蚀过程,极有可能导致柴达木盆地沉积物源区组成或供源格局发生显著变化(Ritts and Biffi,2001;Zhuang et al., 2011)。因此,柴达木盆地晚新生代沉积物的物源分析可为认识青藏高原东北缘造山带的岩石组成提供重要证据。

针对柴达木盆地西北部,前人在沉积学、低温热年代学等方面取得了较大的研究进展,但是晚新生代以来较为可靠的物源供给区及其转换时限还缺少更进一步的数据支撑。沉积岩中的锆石作为一种重要副矿物,随着近年来 LA-ICP-MS 微区分析技术迅速发展,碎屑锆石的 U-Pb 年代学已经广泛应用于沉积地层和物源示踪研究(Cawood et al., 2013)。此外,锆石微量元素,如稀土元素(REEs),被认为是化学成分不变,保留了源岩的特征(Taylor and McLennan,1985;McLennan,2018)。这些微量元素不仅可用于沉积物来源和沉积盆地构造背景的判别(Bhatia and Crook,1986),还能识别源区岩石类型(Hoskin and Ireland,2000;Grimes et al., 2007),有效区分2个或2个以上具相似形成年龄、不同形成背景的物源类型等。

柴达木盆地西北部大浪滩地区发育一套巨厚的新生代砂砾石沉积层系,为新型“砂砾型”卤水钾盐矿赋存地层,是柴达木盆地第四纪以来重要的盐类沉积中心。本研究对大浪滩地区柴钾2井100.93 m、199.97 m、401.51 m、501.65 m、1215.47 m和柴钾3井301.52 m、789.92 m埋深的7个砂岩样品进行了碎屑锆石U-Pb年代学、锆石微量元素特征分析与Lu-Hf同位素研究,结合潜在物源区碎屑锆石U-Pb年代学资料,对柴西北大浪滩地区晚新生代沉积物进行综合物源分析。本研究的目的是推断砂砾石层系的物源和沉积过程,为阿尔金山及青藏高原北缘快速隆升提供可靠的年龄证据,对探索大浪滩—黑北凹地“砂砾型”含钾卤水资源提供新的年代制约。

1 区域地质背景

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柴达木盆地位于青藏高原东北缘(图1),是新生代期间发育起来的大型陆相沉积盆地,四周被阿尔金山、东昆仑祁漫塔格和祁连山所环绕。在印度板块与欧亚板块持续汇聚的构造背景下,盆地内部形成了一系列北西—东西走向的逆冲褶皱带,同时在南、北边缘发育了大规模的逆冲断层。从大地构造单元来看,柴达木盆地与周缘山脉经历了新元古代早期、早古生代和晚古生代—早中生代多期构造-岩浆活动,而非一个刚性克拉通(Yin and Harrison,2000;Cheng et al., 2017)。这一复杂的地质演化过程,使周缘的阿尔金山、东昆仑祁漫塔格和祁连山成为盆地沉积物的主要物源区(Zhuang et al., 2011;Jian et al., 2013)。

柴达木盆地周缘的三大山脉构成了一个完整的物源供给系统。西北侧的阿尔金山在走滑断裂活动和分段隆升过程中不断向盆地提供碎屑物质。阿尔金山基岩组成复杂,发育前寒武纪结晶基底及多期古生代岩浆岩,古元古代(1.6—2.0 Ga)、新元古代(922—928 Ma)、早古生代(517—385 Ma)和二叠纪(260—280 Ma)锆石U-Pb年龄在阿尔金山的火成岩和变质基底中普遍存在(Gehrels et al., 2003a, 2003b;刘良等,2015),其年龄组成以954—939 Ma、~517 Ma、501—496 Ma、469—435 Ma、424—406 Ma及265 Ma为主(刘良等,2015;Chen et al., 2018;Wu et al., 2018;曾旭等,2024)。贯穿该山的阿尔金走滑断裂带,其约1600 km的延伸长度和350~400 km的左旋位移量,显著控制了柴达木盆地西北部古近纪沉积物的分散路径(Tapponnier and Molnar,1977;Yue et al., 2004)。盆地北部的南祁连山以发育古元古界基底上覆中元古界—新元古界盖层为特征,同时大面积出露古生代火山—沉积岩系。其南侧的柴北缘构造带主要指北柴达木早古生代俯冲—碰撞带,以发育早古生代高压—超高压变质岩、蛇绿混杂岩和侵入岩为特征(Yin and Harrison,2000;Xiao et al., 2009)。欧龙布鲁克地块虽属独立微陆块,但因位于柴达木盆地北缘方向并发育古老结晶基底,本研究将其作为柴北缘方向上的古老基底源区一并讨论。东昆仑祁漫塔格保存了700~1000 Ma基底信息,并广泛发育490—390 Ma和250—240 Ma的岩浆活动,是柴达木盆地南缘重要的供源区(Li et al., 2013;Jian et al., 2020;Song et al., 2020)。裂变径迹热年代学数据揭示,这些山脉的主要隆升—剥露期发生在新生代(Jolivet et al., 2001;Duvall et al., 2013;Wang et al., 2015;He et al., 2017, 2018;Wu et al., 2021)。这种构造隆升—剥蚀—沉积的耦合过程,最终塑造了柴达木盆地的新生代沉积格架。

大浪滩地区位于阿尔金山前缘的柴达木盆地西北部次级凹陷带,受阿尔金走滑断裂与基底断裂控制,形成NWW向展布的洼陷—褶皱分区并使沉积中心呈条带化分割。钻遇地层狮子沟组(磁性地层年龄约8.1—2.5 Ma)以陆相碎屑充填为主(Fang et al., 2007),表现为泥岩—砂质泥岩夹砂岩至砾岩,含盐类沉积夹层,代表相对较低能的湖相—滨湖相沉积; 上覆地层七个泉组(磁性地层底界年龄约2.5 Ma)(Fang et al., 2007),在盆地边缘以巨厚砾石—砂砾石沉积为特征,代表近源高能粗碎屑沉积,向盆地内部逐渐过渡为河流—滨浅湖相的较细粒沉积组合。山前冲洪积扇与河道砂砾层构成高孔渗储卤介质,与断裂带共同约束卤水补给、运移与封存,含钾卤水总体被认为属于溶滤—沉积型(郑绵平等,2015)。

柴钾2井、柴钾3井位于大浪滩西北部靠近阿尔金山前位置,地层序列发育于冲洪积扇沉积环境。柴钾2井深1216.65 m,整体为一大套砂砾石层,岩性为砾质中粗砂及中粗砂质砾石(图2-a),分选性较差,磨圆度一般,次棱角状—次圆状; 砾石呈杂色,主要成分为石英、长石、辉石、角闪石和花岗岩等; 含水性、透水性极好,为“砂砾型”含钾卤水储集层段,于1215 m出现1 m厚的泥岩隔水层。柴钾3井深791.98 m,其中0~370.75 m为砂砾石层,分选性较差,磨圆度一般,次棱角状—次圆状,砾石主要成分为石英、长石、辉石、花岗岩等,砾石成层排布(图2-b至2-e),含水性、透水性极好; 自370.75 m后出现胶结致密的粉砂岩、泥岩隔水层与砂砾石层互层,呈现出泥岩—粉砂岩—泥岩、泥岩—粉细砂岩—中粗砂层—粉砂层—泥岩等规律的沉积韵律,指示远端扇、扇中亚相及泥坪微相。

2 样品采集与测试

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本研究共选取大浪滩地区柴钾2井100.93 m、199.97 m、401.51 m、501.65 m、1215.47 m和柴钾3井301.52 m、789.92 m埋深7个砂岩样品(图2),用于碎屑锆石年代学分析。样品岩性以黄褐色砾质中粗砂为主,经破碎和筛分后,采用重液和磁法将重矿物分离,并在双目显微镜下人工挑选较完整的锆石颗粒,每个样品挑选250颗用环氧树脂固定制靶,打磨抛光后,通过反射光及透射光观察,筛除缺陷锆石颗粒,拍摄锆石的阴极发光(CL)图像,确定锆石的内部结构特征。随机选择没有裂缝和包裹体的纯净锆石颗粒进行锆石U-Pb年龄测试。

碎屑锆石 LA-ICP-MS U-Pb 年龄测试工作在中国地质科学院自然资源部成矿作用与资源评价重点实验室完成,实验采用激光剥蚀电感耦合等离子质谱法(LA-ICP-MS),使用德国Analytik Jena公司生产的PlasmaQuant MS Elite 四级杆质谱进行,配套Resolution S-155 193 nm 激光系统对样品进行消融,信号强度由Bruker M90 ICP-MS 采集分析。实验中采用氦气和氩气分别作为剥蚀物质的载气和分析过程中的补充气,激光器工作频率为4 Hz,激光束斑直径为30 μm,能量密度约4.0 J/cm²。每个碎屑锆石样品测试80颗锆石左右。在U-Pb同位素定年和微量元素含量处理中,采用锆石标准91500和玻璃标准物质NIST610作外标,分别进行同位素和微量元素分馏校正。实验数据处理采用ICPMS DataCal程序(Liu et al., 2010),锆石样品的U-Pb年龄谐和图和加权平均计算采用Isoplot程序(Ludwig,2003)。采用Andersen(2002)提出的普通Pb校正方法对所有的年龄数据进行了校正。经普通Pb校正后,对年龄小于1 Ga的颗粒,由于其内部Pb含量较低、测定误差相对较大,采用 ²⁰⁶Pb/²³⁸U年龄作为最终年龄; 而对于年龄大于1 Ga的颗粒,因放射性成因Pb更为富集,则选用 ²⁰⁷Pb/²⁰⁶Pb 年龄作为最终年龄(Gehrels et al., 2008)。

对锆石开展原位Lu-Hf同位素测试,所用仪器为配备Newwave UP 213 nm激光剥蚀系统的Neptune多接受电感耦合等离子体质谱仪(MC-ICPMS)。在激光剥蚀过程中,设定斑束尺寸为55 μm,激光频率控制在8 Hz。实验选取国际锆石标准GJ-1作为参考物质,实测获得的¹⁷⁶Hf/¹⁷⁷Hf加权平均值为0.282007±0.000007(2σ,n=36),该数值与Morel等(2008)的参考标准值在误差允许范围内,验证了本次实验数据的可靠性。在(¹⁷⁶Hf/¹⁷⁷Hf)i与ε_Hf值的计算过程中,¹⁷⁶Lu衰变常数选用Scherer等(2001)提出的1.865×10^-11 a^-1;ε_Hf值计算所采用的球粒陨石Hf同位素参数则参考Bouvier等(2008)的推荐值,具体参数为¹⁷⁶Lu/¹⁷⁷Hf=0.0336、¹⁷⁶Hf/¹⁷⁷Hf=0.282785。Hf模式年龄计算过程中,亏损地幔当前的¹⁷⁶Hf/¹⁷⁷Hf值设定为0.28325,¹⁷⁶Lu/¹⁷⁷Hf值取0.0384;两阶段模式年龄的计算,则采用Griffin等(2000)提出的平均地壳参数(¹⁷⁶Lu/¹⁷⁷Hf)C=0.015完成,确保计算结果的科学性与规范性。

3 数据分析

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3.1 锆石年龄分布

从柴钾2井、柴钾3井碎屑锆石的代表性样品阴极发光图像(图3)可看出,样品中碎屑锆石多呈自形—半自形短柱状和长柱状,部分颗粒边缘可见一定程度的磨蚀,粒度整体较为均一,内部结构多发育清晰的振荡环带,仅少数锆石颗粒不具明显生长环带。锆石颗粒的长度为60~220 μm,宽度为50~150 μm。Th/U值为0.02~1.26,且大多数锆石颗粒的Th/U值大于0.4,呈现出岩浆成因特征(图4),与CL图像显示的锆石表面结构一致。全部样品中有7.03%的锆石颗粒Th/U值小于0.1,鉴于低Th/U值并非变质锆石的唯一判据,且该部分颗粒在CL图像中总体仍保留振荡环带,因此本研究保留其年龄信息,并在后续解释中结合微量元素特征讨论其成因意义。

从7个样品的U-Pb谐和图(图5;图6)可以看出,绝大多数数据点都落在谐和线上或者附近位置。样品的锆石年龄整体介于213.9~3307.8 Ma之间,大致可划分为4个年龄区间,分别为200~300 Ma、330~510 Ma、740~990 Ma、1.1~3.3 Ga。

柴钾2井共测试5件样品,其中七个泉组4件、狮子沟组1件。七个泉组样品(GCJ-2-1、GCJ-2-2、GCJ-2-4和GCJ-2-5)有效数据点为187个,碎屑锆石年龄集中于239.8~1580.6 Ma之间,主峰较为稳定,主要分布在250.8±3.9~262.9±3.4 Ma,反映出明显的印支期年龄组分; 次峰范围为300.0±3.2~401.2±2.3 Ma,显示晚古生代年龄组分亦较为发育。相比之下,狮子沟组样品GCJ-2-12有效数据点为47个,年龄分布范围明显扩大(213.9~2387.3 Ma),主峰和次峰分别为267.0±3.5 Ma和452.4±5.4 Ma,表明其年龄组成较七个泉组更为复杂,并具有较明显的早古生代特征。

柴钾3井共测试2件样品,分别来自七个泉组和狮子沟组。七个泉组样品GCJ-3-3获得33个有效数据点,年龄范围为390.3~3307.8 Ma,主峰和次峰分别为409.3±2.9 Ma和465.6±3.7 Ma,均以早古生代年龄组分为主。狮子沟组样品GCJ-3-8获得61个有效数据点,年龄范围为371.1~1912.2 Ma,主峰为386.6±5.1 Ma,次峰为942.9±7.7 Ma,显示除古生代年龄组分外,还发育明显的中元古代年龄信息。

总体来看,柴钾2井七个泉组样品以250~263 Ma峰值为主,而柴钾3井样品则以386~466 Ma峰值更为突出,反映出不同钻孔及层位之间的碎屑锆石年龄组成存在一定差异。

3.2 Hf同位素特征

每个样品选取目标年龄的锆石颗粒各30个左右进行Hf同位素测试(图7),且每个碎屑锆石颗粒的Hf分析点圈定基本与U-Pb分析点重合,但由于部分点位已被激光打穿,因此稍稍偏移U-Pb分析中心点来保证实验数据的完整性。

锆石Hf同位素特征变化较大,绝大多数样品在亏损地幔和0.2 Ga地壳演化线之间,锆石¹⁷⁶Lu/¹⁷⁷Hf值介于0.000104~0.003772之间,其中约92.3%的分析点小于0.002,显示放射性成因的Hf同位素富集程度较低(钟海仁等,2020);¹⁷⁶Hf/¹⁷⁷Hf值为0.282005~0.282946,均值为0.282612。所有分析点ε_Hf(t)值变化范围为-9.60~12.26(图7),整体均值为2.97,其中正ε_Hf(t)值占75.7%,负ε_Hf(t)值占24.3%,显示研究区碎屑锆石总体以新生地壳物质贡献为主,但同时混有一定比例的古老地壳再循环组分。锆石两阶段Hf模式年龄T_DMc为0.53~2.04 Ga,主要集中于0.80~1.50 Ga,并在1.0~1.1 Ga附近形成明显峰值,指示物源区所记录的地壳增生事件主要集中于中元古代晚期—新元古代早期,局部保留有更古老基底的信息。

结合U-Pb年龄及对应的Hf同位素特征,研究区碎屑锆石可划分为4个年龄区间。214~304 Ma年龄段锆石共77颗,为一套典型的年轻组分,其ε_Hf(t)值介于-0.92~11.91之间,平均值为5.57,其中76颗为正值,正值比例高达98.7%,T_DMc年龄为0.53~1.35 Ga,表明该年龄段锆石主要反映了明显的幔源或年轻壳源物质加入,是研究区新生地壳物质贡献最为显著的年龄组。335~514 Ma年龄段锆石共137颗,为全部测试点中最主要的年龄组分,ε_Hf(t)值变化范围最大,为-9.60~12.26,平均值为1.72,其中正值89颗、负值48颗,正值占比65.0%,对应T_DMc年龄为0.57~2.04 Ga,显示这一时期锆石来源最为复杂,既包含一定比例的新生地壳输入,也混入了较多古老地壳重熔或再循环物质。911~964 Ma年龄段锆石共18颗,ε_Hf(t)值为-3.60~6.47,平均值为1.40,正值比例为61.1%,T_DMc年龄为1.41~2.01 Ga,表明该组锆石记录了新元古代地壳增生与古老基底改造并存的特征。1146~1447 Ma年龄段锆石仅3颗,ε_Hf(t)值介于-1.00~4.34之间,T_DMc年龄为1.87~2.02 Ga,数量虽少,但说明研究区物源体系中仍存在少量中元古代基底物质的输入。

3.3 碎屑锆石微量元素特征

本研究选取谐和度较高的锆石颗粒进行微量元素分析,所有样品的锆石颗粒均呈现重稀土元素相对于轻稀土元素富集的特征,在稀土元素球粒陨石标准化的图解(图8;图9)上显示出左低右高的图谱特点,重稀土元素从Gd开始向右逐步增长,所有锆石颗粒均显示出明显的Eu负异常和Ce正异常,具备岩浆成因锆石特征(Hoskin and Ireland,2000;Hoskin and Schaltegger,2003)。需要指出的是,少量低Th/U值锆石颗粒虽可能具有特殊成因意义,但其CL图像仍以振荡环带为主,稀土元素配分模式也未显示典型变质锆石特征。因此,本研究保留其年龄信息参与总体年龄谱分析,但不将其单独作为特定变质源区的判别依据。碎屑锆石Y-U、ΔCe-δEu、Y-Yb/Sm、Y-Nb/Ta、Y-δCe、Nb-Ta等微量元素岩性判别图解(图10)显示,多数数据点集中分布于花岗岩类区域,部分位于基性岩与花岗岩的过渡范围,另有少量点落入伟晶岩区,因此可以推断出研究区碎屑锆石母岩主要为基性和酸性岩浆岩。碎屑锆石U/Yb-Hf、Th/Yb-Hf、U/Yb-Y和Th/Yb-Y判别图解(图11)显示,绝大多数锆石颗粒投点于陆壳成因锆石区域,显示其来源于陆壳花岗质岩石。Nb/Hf-Th/U和Hf/Th-Th/Nb双变量图解(图12)表明,大部分锆石颗粒形成于岩浆弧/造山带环境。

4 讨论

收起

沉积物从源区风化剥蚀开始,经历了不同地表动力机制的搬运、沉积、水动力改造以及后期成岩作用等影响。而锆石作为一种抗物理风化和化学风化能力较强的矿物,可以在不同的风化和水动力搬运条件下仍然保持着最初的物源信息,因此广泛应用于物源分析(钟海仁等,2020)。在分析碎屑锆石物源时,可以根据各个样品年龄峰值的分布情况、Hf同位素及微量元素特征的综合对比寻找相应的潜在物源区,并结合其他区域地质资料来判断碎屑物质的潜在源区和搬运路径。少量低Th/U值锆石颗粒虽然在成因上值得关注,但由于其未显示典型变质锆石的CL结构特征,且未形成独立年龄峰,本研究暂不将其单独作为特定变质源区的判别标志,而主要将其视为总体年龄谱中的辅助信息。

4.1 潜在物源区特征

研究区位于大浪滩地区西北部靠近阿尔金山前位置,周缘存在4个潜在物源区,分别是阿尔金山、东昆仑祁漫塔格、南祁连山及柴北缘构造带,均可能为大浪滩地区提供物源(Zhao et al., 2020a,2020b)。

4.1.1 阿尔金山

阿尔金山位于研究区西北侧,是柴达木盆地西北部重要的近邻源区之一。其构造-岩浆演化具有明显的阶段性,古生代花岗质岩浆活动可划分为503—497 Ma、483—458 Ma、456—432 Ma、424—385 Ma、352—338 Ma和265—264 Ma共6期,其中469 Ma、462 Ma、448—444 Ma、444—435 Ma、406 Ma和265 Ma等年龄最具代表性,分别对应俯冲、碰撞后部分熔融、伸展调整及晚期再活动等过程(Cowgill et al., 2003;陈正乐等,2006;吴才来等, 2014a;Wu et al., 2018)。此外,阿尔金山内部还保存954 Ma和939 Ma的新元古代花岗质岩浆活动,并可提供1.8~2.5 Ga的古老锆石组分(Chen et al., 2018;曾旭等,2024)。

Hf同位素和岩石地球化学资料显示,阿尔金山源区中较年轻地壳物质和古老陆壳物质均有参与。南阿尔金不同时期花岗岩锆石ε_Hf(t)以正值为主,但局部可出现负值,说明其源区以较年轻地壳物质为主,同时存在古老陆壳成分(Wu et al., 2018);花岗岩锆石ε_Hf(t)为-8.64~+5.30,两阶段模式年龄为1.59~2.35 Ga,表明新元古代花岗岩主要与古老地壳重熔有关(Chen et al., 2018)。地球化学方面,阿尔金山相关花岗质岩石普遍表现为轻稀土元素富集、Nb-Ta-Ti亏损和不同程度的Eu负异常(Chen et al., 2018;Wu et al., 2018)。总体上,阿尔金山锆石年龄特征可以概括为: 以430~470 Ma为主、同时存在265 Ma和939~954 Ma,Hf同位素以正值占优势但负值亦可出现。

4.1.2 东昆仑祁漫塔格

东昆仑祁漫塔格位于柴达木盆地南缘,是研究区重要的南侧潜在源区。该区保存了较明显的新元古代基底年龄信息,并广泛发育早古生代和三叠纪岩浆活动,年龄主要集中于700~1000 Ma、390~490 Ma和240~250 Ma。其中,700~1000 Ma年龄反映新元古代基底演化,峰值多集中于约800 Ma和920 Ma;390~490 Ma年龄对应早古生代俯冲、增生和碰撞过程; 244~246 Ma左右的花岗岩和石英闪长岩则代表古特提斯北向俯冲背景下的三叠纪岩浆活动(陈国超等,2013;赵菲菲等,2017;Jian et al., 2020;Song et al., 2020)。

东昆仑祁漫塔格不同年龄组的Hf同位素和微量元素特征较为清楚。700~1000 Ma年龄段碎屑锆石ε_Hf(t)为-10~+5,说明新元古代基底既记录了新生地壳加入,也保存了古老地壳再造过程(Jian et al., 2020);洪水河244~246 Ma岩体锆石ε_Hf(t)为-4.0~+1.7,表明其主要来自中元古代基性下地壳熔融,并伴有一定幔源物质加入(Song et al., 2020)。地球化学方面,东昆仑祁漫塔格花岗质岩石普遍表现为轻稀土富集、Nb-Ta-Ti亏损和Eu负异常,反映活动大陆边缘环境下的花岗质岩浆作用(Song et al., 2020)。总体上,东昆仑祁漫塔格物源区特征可概括为: 锆石年龄以240~250 Ma、390~490 Ma和700~1000 Ma为主,Hf同位素多为弱负值至正值。

4.1.3 南祁连山

南祁连山位于柴达木盆地北缘,是研究区另一重要邻近源区。该区以早古生代岩浆活动最为突出,同时保存新元古代和古元古代基底年龄。祁连山地区在517—359 Ma期间形成了大量侵入岩,其中南祁连在452—444 Ma和431 Ma广泛发育碰撞花岗岩,在440—425 Ma形成后碰撞伸展环境下的高镁中性侵入岩、埃达克质岩和A型花岗岩,至泥盆纪又出现409—402 Ma和386 Ma左右的岩浆活动(Lu et al., 2019;Wang et al., 2020;李平等,2023)。此外,807~923 Ma、1854 Ma和2370 Ma等年龄可反映其较老基底组成。已有邻区沉积物研究表明,与南祁连源区对应的碎屑锆石年龄组分通常以~441 Ma为主峰,并伴随~248 Ma、~277 Ma、~807 Ma、~923 Ma、~1854 Ma和~2370 Ma等次峰(钱涛等,2025),这些年龄组成可作为本研究识别南祁连源区贡献的对比依据。

南祁连山的Hf同位素和微量元素特征同样能够为物源判别提供约束。祁连山寒武纪—奥陶纪侵入岩ε_Hf(t)和ε_Nd(t)变化范围较大,表明其源区中既有古老地壳重熔,也有较年轻地壳物质加入; 其中碰撞阶段花岗岩以强过铝质S型花岗岩为主,后碰撞阶段则出现具有正ε_Nd(t)、正ε_Hf(t)特征的埃达克质岩和A型花岗岩(李平等,2023)。地球化学方面,南祁连早古生代侵入岩普遍表现为高钾钙碱性、过铝质、轻稀土富集及Nb-Ta-Ti亏损,反映弧岩浆和碰撞花岗岩的共同特征; 泥盆纪以后岩浆活动明显减弱,仅零星发育中性—基性岩脉和少量晚期花岗岩(李平等,2023)。与此同时,红崖子盆地和柴北缘东段新生代沉积研究显示,南祁连山在中中新世以来能够持续向盆地北缘提供碎屑物质(谢皓,2024;钱涛等,2025)。总体上,南祁连山物源区特征可概括为: 以400~452 Ma为主,并伴随800~1000 Ma和1.8~2.5 Ga年龄; Hf同位素正负共存,但古老地壳再造特征较为明显。

4.1.4 柴北缘构造带

柴北缘构造带位于柴达木地块与南祁连之间,是研究区北侧重要的邻近源区。该区经历了新元古代Rodinia聚合与裂解,以及早古生代俯冲、碰撞和后碰撞伸展等多阶段构造演化(Niu et al., 2021),其岩浆活动归纳为前寒武纪、早古生代—泥盆纪和中晚二叠纪—三叠纪3个阶段。前寒武纪年龄主要记录欧龙布鲁克地块基底的形成与演化,常见2.0~2.6 Ga、1.8~1.9 Ga、1.2~1.6 Ga和0.9~1.0 Ga年龄组成(赵文涛等,2020)。早古生代—泥盆纪年龄则反映柴北缘地区由洋壳俯冲、碰撞—碰撞伸展的演化过程,其中与本研究的样品对比关系较为密切的年龄主要集中于400~430 Ma和~357 Ma;中晚二叠世—三叠纪年龄则与宗务隆洋南向俯冲背景下的弧岩浆作用有关,与本研究样品中252~273 Ma年龄组分具有较好的对应关系(吴才来等,2008;Xiong et al., 2012;董增产等,2015;徐旭明等,2017;庄玉军等,2020;彭璇等,2022)。

柴北缘构造带的Hf同位素和微量元素特征变化较大,这也是其物源判别的重要依据。小赛什腾山422.1±1.6 Ma片麻状花岗岩为高硅、高钾钙碱性、过铝质岩石,富集Rb、亏损Nb和Ti,轻稀土富集并具有弱负Eu异常,锆石ε_Hf(t)为-6.47~-12.85,表明其主要来源于古老地壳重熔(彭璇等,2022)。与之相比,429.9 Ma英云闪长岩锆石ε_Hf(t)为+9.3~+11.9,而428.0 Ma细粒闪长岩锆石ε_Hf(t)为-31.4~-9.9,表明同一时期不同岩浆体可分别代表较年轻地壳物质和古老陆壳物质2类来源(李治华等,2021)。357±4 Ma辉长岩脉锆石ε_Hf(t)为9.25~15.11,显示地幔物质参与较强(庄玉军等,2019);晚古生代盐场北山花岗岩则普遍具有大离子亲石元素富集、Nb-Ta-Ti亏损和ε_Hf(t)正值为主的特征(董增产等,2015)。

4.2 物源区示踪

本研究获得下更新统七个泉组和上新统狮子沟组碎屑锆石年龄(图13;图14),结合潜在物源区碎屑锆石U-Pb年代学资料,对柴西北大浪滩地区七个泉组和狮子沟组物源进行分析。

4.2.1 七个泉组物源特征

柴钾2井七个泉组4件样品在不同深度均稳定发育250~263 Ma主峰,并伴有300~401 Ma次峰,整体年龄结构较为一致(图14)。与周缘沉积源区对比,这组样品与东昆仑祁漫塔格的对应关系最为清楚(图15)。东昆仑祁漫塔格北缘广泛发育244~246 Ma的大陆弧岩浆活动和390~490 Ma早古生代岩浆活动,而柴钾2井七个泉组样品在214~304 Ma年龄段锆石ε_Hf(t)以正值为主,也与东昆仑祁漫塔格三叠纪花岗质岩浆岩整体表现出的弱负值至正值特征一致(Li et al., 2013;Song et al., 2020)。

相比之下,南祁连山虽然也出现了248~277 Ma次峰年龄,但其更常见的是约441 Ma主峰,并伴有807~923 Ma和1854~2370 Ma等组成; 阿尔金山则以435~469 Ma和939~954 Ma为主; 柴北缘除252~273 Ma外,通常还应伴随更明显的420~430 Ma及0.9~1.0 Ga、1.8~1.9 Ga年龄组成,而这些特征在柴钾2井七个泉组样品中均不突出(Wu et al., 2018;彭璇等,2022;钱涛等,2025)。因此,柴钾2井七个泉组样品应以东昆仑祁漫塔格相关物质来源为主,柴北缘可能有少量补充,南祁连山和阿尔金山贡献较小。

柴钾3井七个泉组样品GCJ-3-3则表现出完全不同的年龄结构,其主峰为409.3±2.9 Ma,次峰为465.6±3.7 Ma,不含印支期年龄,说明其物源组成明显不同于柴钾2井。该样品与阿尔金山、柴北缘和南祁连山均存在一定对应关系: 阿尔金山发育469—435 Ma和424—406 Ma岩浆活动,柴北缘可见422~429 Ma和400~409 Ma年龄,南祁连山则发育452—431 Ma、440—425 Ma、409—402 Ma和386 Ma岩浆活动(Wu et al., 2018;李平等,2023)。GCJ-3-3在335~514 Ma年龄段Hf同位素正负并存,整体接近中性至弱负,表明其来源中既有较年轻地壳物质,也有古老陆壳重熔成分,这与柴北缘和南祁连山早古生代侵入岩Hf同位素变化幅度较大、正负共存的特征更为接近,也与阿尔金早古生代花岗岩以正值为主、局部可见负值的特征相符(Wu et al., 2018;李治华等,2021;李平等,2023)。然而GCJ-3-3并不明显发育南祁连山常见的807~923 Ma和1.8~2.5 Ga年龄,也未出现柴北缘典型的252~273 Ma组成,因此南祁连山和柴北缘均不宜单独作为其唯一来源。综合判断,GCJ-3-3主要反映阿尔金山与柴北缘共同供源,南祁连山可能有一定参与,但并非主导来源。

2口钻井七个泉组物源的差异,反映了同一沉积阶段内研究区冲洪积扇相的横向分异。柴钾2井七个泉组4个样品指示其持续接受较稳定的南侧东昆仑祁漫塔格方向物源补给; 而柴钾3井七个泉组样品表明其主要记录了阿尔金山和柴北缘方向的碎屑供给。由此可见,七个泉组沉积时期研究区内部不同井位所对应的扇体展布、碎屑输送方向和近源补给范围已出现明显差异。晚上新世—早更新世阿尔金断裂活动增强、柴西北内部抬升并伴随沉积中心迁移,区域挤压作用进一步增强,促使山前冲洪积扇沉积体系重组(Chang et al., 2012;Chen et al., 2017;Zhang et al., 2022),此外,大浪滩—黑北凹地区域逆断层发育,山前地层抬升、相邻钻孔间岩性与储层差异明显,表明区域断裂进一步强化了沉积充填和物源记录上的横向差异(侯献华等,2021),最终形成柴钾2井以东昆仑祁漫塔格为主、柴钾3井以阿尔金山和柴北缘共同供源为主的分区供源格局。这一认识也与晚新生代柴达木盆地碎屑锆石年龄谱具有明显时空分异的研究结果(Jian et al., 2024)相一致。

4.2.2 狮子沟组物源特征

与七个泉组相比,狮子沟组样品年龄分布范围明显变宽,且较老锆石数量增加,指示其物源组成更为复杂。柴钾2井狮子沟组样品GCJ-2-12的主峰为267.0±3.5 Ma,次峰为452.4±5.4 Ma,年龄范围可延伸至2387.3 Ma(图14)。这一年龄组合说明其来源不能由单一源区解释。267 Ma可与东昆仑祁漫塔格246—244 Ma岩浆活动对应,也可与柴北缘273—252 Ma岩浆活动及南祁连248—277 Ma次峰年龄对应(图15);452 Ma则可与南祁连452—444 Ma花岗岩、阿尔金469—435 Ma岩浆活动以及柴北缘早古生代侵入岩相联系(董增产等,2015;Wu et al., 2018;Song et al., 2020;李平等,2023)。样品中还出现2387 Ma等较老年龄,与南祁连常见的1854~2370 Ma组成、阿尔金的1.8~2.5 Ga组分以及柴北缘欧龙布鲁克地块的古老基底均可对应(赵文涛等,2020;曾旭等,2024;钱涛等,2025)。GCJ-2-12的ε_Hf(t)变化范围在全部样品中较宽,正值和负值同时出现,表明其来源中既包含较年轻地壳物质,也包含古老陆壳物质。综合判断,GCJ-2-12应解释为东昆仑祁漫塔格、柴北缘、南祁连山和阿尔金山共同供给的混合来源,其中267 Ma主要反映二叠纪岩浆物质输入,452 Ma和2387 Ma等组成则反映北侧—西北侧奥陶纪及古老基底物质的加入。

柴钾3井狮子沟组样品GCJ-3-8的主峰为386.6±5.1 Ma,次峰为942.9±7.7 Ma,年龄上限可达1912.2 Ma。这一组合与4个潜在源区均存在一定对应,但约束关系比GCJ-2-12更清楚。386 Ma可与南祁连泥盆纪386 Ma及409—402 Ma岩浆活动对应,也与东昆仑490—390 Ma早古生代岩浆活动吻合; 942.9 Ma则与阿尔金山939~954 Ma、东昆仑约920 Ma和南祁连807~923 Ma组成较为接近(Chen et al., 2018;Jian et al., 2020;李平等,2023)。GCJ-3-8整体以正ε_Hf(t)为主,但变化幅度较小,说明其来源中较年轻地壳物质加入较多,同时存在一定古老陆壳物质。考虑到该样品缺少250 Ma左右主峰,不宜解释为东昆仑三叠纪物源主导,更合理的解释是东昆仑祁漫塔格的早古生代—新元古代物源,与南祁连及阿尔金山物源的共同输入。其中,东昆仑祁漫塔格在386 Ma组分上仍具有较强解释力,而943 Ma和1912 Ma等年龄则反映南祁连、阿尔金及柴北缘古老地体的参与。

与七个泉组相比,狮子沟组在2口钻井中均表现出更明显的多源混合特征,说明该阶段研究区沉积体系对周缘山系碎屑的汇聚范围更广。柴钾2井狮子沟组样品反映东昆仑祁漫塔格与北侧—西北侧柴北缘、南祁连山及阿尔金山物质的共同加入; 柴钾3井狮子沟组样品显示其在接受东昆仑祁漫塔格物源的同时,也混入了南祁连、阿尔金及柴北缘古老地体的碎屑。整体上,狮子沟组沉积时期研究区处于以多源混合为主的盆地沉积格局,而至七个泉组沉积时期,随着阿尔金山前构造活动及柴西北抬升—挤压作用增强,山前粗碎屑沉积体系明显前推,原先较为宽泛的多源混合格局进一步演化为不同井位之间更清楚的分区供源格局(Chang et al., 2012;Chen et al., 2017;Zhang et al., 2022)。这一变化与晚新生代柴达木盆地碎屑物源由广泛混合向局部分异增强的总体趋势(Jian et al., 2024)相吻合。

5 结论

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1)综合柴达木盆地柴钾2井和柴钾3井碎屑锆石U-Pb定年及Hf同位素研究,结合周缘山系主要锆石U-Pb年龄,明确了盆地西北部大浪滩地区狮子沟组和七个泉组的物源组成特征。研究区碎屑锆石U-Pb年龄总体介于213~3307 Ma之间,主要包括200~300 Ma,330~510 Ma,740~990 Ma,1.1~3.3 Ga 共4组年龄。其中,柴钾2井七个泉组样品主要峰值年龄集中在250~263 Ma和300~401 Ma,柴钾3井七个泉组样品主要峰值年龄集中于409~466 Ma;狮子沟组样品年龄分布范围更宽,除267 Ma、386 Ma、452 Ma和943 Ma等峰值外,还出现1912 Ma和2387 Ma等较老年龄。

2)柴达木盆地西北部大浪滩地区不同井位和不同层位的碎屑锆石年龄谱及Hf同位素特征存在明显差异,表明其物源组成具有分区性和混合性。七个泉组沉积时期,柴钾2井物源以东昆仑祁漫塔格为主,柴北缘可能有少量参与; 柴钾3井则主要反映阿尔金山和柴北缘共同供源,南祁连山可能有一定参与。狮子沟组较七个泉组表现出更为复杂的多源混合特征,其中柴钾2井狮子沟组为东昆仑祁漫塔格、柴北缘、南祁连山和阿尔金山共同供源,柴钾3井狮子沟组则以东昆仑祁漫塔格和南祁连山相关物质占较高比例,同时接受阿尔金山和柴北缘的部分输入。2口钻井之间的物源差异反映了山前冲洪积扇沉积体系的横向分异特征,并受到晚新生代区域构造活动增强及断层的共同控制。

后记: 值恩师冯增昭先生百年诞辰之际,谨于本文致以崇高敬意与深切缅怀。冯增昭先生毕生从事沉积学与岩相古地理学的教学和研究,在碳酸盐岩沉积学、岩相古地理学及相关方法体系建设等方面作出了卓越贡献,对中国沉积地质学与古地理学的发展产生了深远影响。先生治学严谨,求实创新,奖掖后学,诲人不倦,其学术造诣与师者风范,为学界所敬仰。

作为学生,笔者在长期学术研究与教学实践中,始终深受先生学术思想与精神风范的启迪。值此百年之际,谨以此文追念恩师,表达由衷敬意与诚挚感念。冯增昭先生的学术思想、治学精神与师者风范,必将薪火相传,长久垂范后学,并继续激励后来者在沉积学与古地理学研究道路上守正创新、砥砺前行!

(通讯作者张永生为冯增昭先生的1992级博士研究生)

基金

收起

*国家重点研发计划项目(2023YFC2906501)
中国地质调查局地质调查项目(DD20230755)

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2026年第28卷第3期

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doi: 10.7605/gdlxb.2026.110

接收时间：2026-02-27
首发时间：2026-09-24
出版时间：2026-06-01

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收稿日期：2026-02-27
修回日期：2026-04-15

基金

National Key Research and Development Program of China(2023YFC2906501)

*国家重点研发计划项目(2023YFC2906501)

Geological Survey Project of the China Geological Survey(DD20230755)

中国地质调查局地质调查项目(DD20230755)

作者信息

中国地质科学院矿产资源研究所, 自然资源部盐湖资源与环境重点实验室, 北京 100037

通讯作者:

张永生,男,1963年生,博士,研究员,博士生导师,主要从事盐类矿床地质与“油钾兼探”研究。E-mail: zys_601@126.com。

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2种不同金属材料的力学参数

科 Family	属数 Number of genus	种数 Number of species	占总种数比例 Percentage of total species (%)	属 Genus	种数 Number of species	占总种数比例 Percentage of total species (%)
鹅膏菌科Amanitaceae	2	11	5.26	鹅膏菌属 Amanita	10	4.78
小菇科 Mycenaceae	2	12	5.74	丝盖伞属 Inocybe	5	2.39
多孔菌科 Polyporaceae	8	14	6.70	蜡蘑属 Laccaria	5	2.39
红菇科 Russulaceae	3	23	11.00	小皮伞属 Marasmius	6	2.87
				小菇属 Mycena	11	5.26
				光柄菇属 Pluteus	5	2.39
				红菇属 Russula	17	8.13
				栓菌属 Trametes	5	2.39

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