Variation patterns of boron and lithium isotopes in salt lakes on the Qinghai–Tibetan Plateau and their application in evaluating resources in the Damxung Co salt lake
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摘要: 近年，硼、锂同位素地球化学理论和分馏机理的深入，为盐湖体系硼、锂同位素示踪奠定了基础。基于现有大量研究数据，文章系统归纳盐湖体系硼、锂同位素分馏变化特征，总结盐湖演化过程硼、锂同位素组成的变化规律，建立它们的示踪方法。并以此为基础，对西藏典型富硼、锂盐湖−当雄错开展了硼同位素示踪，解决了当雄错与其物源硼同位素特征不符的难题，提出当雄错湖底蕴含大型硼、锂矿床的新认识，并预测了湖底的硼、锂资源量。根据盐湖体系硼、锂同位素地球化学特征，揭示了溶蚀湖的盐湖资源评价意义，为盐湖体系硼、锂同位素示踪和盐湖资源评价奠定理论基础。此外，借助硼同位素地球化学手段建立的当雄错“围岩−地热水−盐湖”的物源补给模式在西藏和全球具有普遍性。Abstract:
Objective The Qinghai–Tibet Plateau is rich in salt lake resources, known particularly for the concentration of elements such as boron and lithium, forming many distinctive resource-type salt lakes. Compared with ordinary salt lakes, a notable characteristic of resource-type salt lakes is the abundant supply of elements such as boron and lithium. Consequently, these elements' sources and accumulation patterns are key scientific issues for understanding the genesis and mineralization patterns of resource-type salt lakes. Boron and lithium isotopes, characterized by significant mass differences and variations in natural isotope ratios, serve as effective tracers for studying the material sources of boron and lithium in salt lakes. However, the application of boron and lithium isotopes in salt lake systems faces the following three challenges: (1) There is insufficient understanding of how boron and lithium isotopes respond to the fundamental geochemical processes of salt lakes. The salt dissolution process that occurs when supply water flows into lake basins is the main reason for drastic changes in geochemical parameters. Inadequate recognition of salt dissolution processes can lead to an overinterpretation of boron and lithium isotope fractionation changes, weakening their tracking capabilities. (2) Isotope fractionation degree is conflated with changes in isotope composition. In salt lake research, discussions of the solid phase's influence on boron and brine's lithium isotopes are often based solely on fractionation factors between the solid and liquid phases, without considering the ratios of boron and lithium amounts involved in the fractionation process. (3) Discrepancies still exist in understanding the fractionation patterns of boron and lithium isotopes during salt crystallization. Methods In light of these problems, our study systematically reviews and analyzes the mechanisms of boron and lithium isotopic fractionation in salt lake systems and summarizes some essential understandings. Conclusion (1) Only salt crystallizations have specific impacts on B and Li isotopes in salt lakes. Since there is a genetic association between salt assemblages and specific salt lake hydrochemical types, the salt lakes with the same hydrochemical type exhibit consistent patterns of B and Li isotope changes during their evolutionary processes. Until halite precipitation, the B and Li isotopic compositions in sulfate- and chloride-type salt lakes are in accord with δ11B and δ7Li values of their sources instead of being controlled by their salt deposits. In contrast, the paths of B and Li isotopic changes of carbonate-type salt lakes are complex and are divided into two branches: calcite subtype and hydromagnesite subtype. After calcite precipitation, the δ11B value of the salt lake increases, and its δ7Li value is marginally above source characteristics (less than 2‰). After hydromagnesite precipitation, the δ11B value of the salt lake is also marginally above source characteristics (less than 2‰). After the stage of halite precipitation, the B and Li isotopic compositions of salt lakes in all types show an increasing trend. (2) Based on the evolutionary processes of B, Li, and K during seawater evaporation, the amounts of B, Li, and K in the current salt lake represent most of the corresponding resources in the lake if the salt lake never experienced complete dryness such as playa. For the salt-dissolving lake, most of the B, Li, and K resources are preserved in salt deposits and interstitial brine at the bottom of the lake. It is optimal for the resource potential of a carbonate-type salt lake in the salt-dissolving lake. (3) The B sources of the current Damxung Co salt lake located in the Tibetan Plateau are from clay carbonates exposed to the lake shore and highly soluble salts and interstitial brine at the bottom of the lake. The geothermal waters produced during early hydrothermal activity are the original B source of the Damxung Co salt lake. Based on mass balance equations, it is estimated that the B resource at the bottom of the Damxung Co salt lake is at least 9.1×106t (B2O3), and the lithium resource is at least 8.6 ×106t (LiCl). -
Key words:
- Qinghai–Tibet Plateau /
- salt lake /
- boron /
- lithium /
- isotopic tracing /
- dissolving lake /
- resource evaluation
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0. 引言
阿尔金断裂带（Altyn Tagh fault）是青藏高原北缘一条岩石圈尺度的大型左旋走滑边界断裂，总体呈北东东—南西西向，是青藏高原最重要的边界断层之一。新生代阿尔金断裂带的构造活动受控于印度−欧亚板块碰撞的远程效应，多数研究者认为其走滑位移量约为360±70 km（Peltzer and Tapponnier，1988；许志琴等，1999；Meng et al.，2001；Sobel et al.，2001；Yue et al.，2001；Liu et al.，2007；Cheng et al.，2015a），吸收了印度与欧亚大陆之间20%～30%的缩短量（Avouac and Tapponnier，1993；Li et al.，2002；Clark，2012；Cheng et al.，2015b）。
阿尔金断裂带的扩展生长方式是青藏高原北缘最为重要的科学问题之一，也是理解青藏高原隆升生长的关键。目前，研究者针对青藏高原演化提出3个主要端元模型，不同模型均要求阿尔金断裂带有与之相适应的不同生长过程：刚性块体模型强调青藏高原内的块体拼贴增生与挤出，支持阿尔金断裂带自西向东逐步扩展（Tapponnier et al.，1982，2001）；黏性薄席模型支持高原作为整体缩短增厚，认为阿尔金断裂带应该在印度−欧亚板块碰撞之初快速贯通（England and McKenzie，1982；Molnar et al.，1993）；非均质岩石圈模型则强调高原内部岩石圈强弱有别，不同时期、不同地区的变形主导机制不同，此种模型下阿尔金断裂带的活动会更为复杂（Ding et al.，2022）。因此，阿尔金断裂带在新生代何时开始活动、如何演化到现今的状态，是限定高原北缘生长模型的重要边界条件。阿尔金断裂带空间差异性巨大，被多个受阻双弯曲分隔，与周缘断裂带有复杂的构造转换。阿尔金断裂带分别与祁连山造山带和祁曼塔格−东昆仑断裂带形成的三联点，是断裂分段演化的断点，更是构造转换的承载点。文章基于三联点概念，以阿尔金断裂带东段的肃北三联点与西段的吐拉三联点为例，聚焦阿尔金断裂带不同分段与周缘断裂带的构造转换，恢复阿尔金断裂带在新生代分段破裂−贯通的演化过程。
1. 阿尔金断裂带基本特征
阿尔金断裂带长达1600 km，自西向东分隔了塔里木盆地与东昆仑山、柴达木盆地和祁连山，基于此可大致分为西段（昆仑山段）、中段（柴达木盆地段）与东段（祁连山段）。由于昆仑山、祁连山与柴达木盆地岩石圈强度和性质不同（Wang，2001；孙玉军等，2013；宋晓东等，2015；裴旭等，2022），不同分段的演化也相应有所不同。同时，中段包括平直的主断面和阿尔金山北部的北阿尔金断裂与金雁山断裂，发育平顶山双弯曲（约90.4°E）、阿克塞双弯曲（约93.7°E）等多个受阻双弯曲（图1）。而受阻双弯曲等复杂的障碍和其构造几何位置控制着断裂的起始、扩展和终止，现今仍未完全贯通的平顶山弯曲说明阿尔金断裂带中段的演化也并非全段整体破裂，其内部以弯曲为界亦有分段。因此，分段演化应该是阿尔金断裂带现今活动研究与构造历史恢复的重要研究思路。
图 1 阿尔金断裂带构造简图a—青藏高原主要走滑断裂分布图；b—阿尔金断裂带受阻双弯曲、三联点与邻区主要断裂的位置关系分布图（WATF、MATF、EATF分别代指阿尔金断裂带西段、中段与东段）；c—阿尔金断裂带地貌学与大地测量学研究获得的左旋走滑速率分布图（修改自Wu et al.，2019b）Figure 1. Simplified tectonic map of the Altyn Tagh fault (ATF)(a) Distribution of major strike-slip faults on the Qinghai-Tibet Plateau; (b) Extension of the ATF and its spatial relationships with neighboring major faults; the double bending, triple junctions, and the positions of the western, central, and eastern segments of the Altyn Tagh fault (WATF, MATF, and EATF, respectively) are shown；(c) Distribution of left-lateral strike-slip rates obtained from geomorphological and geodetic studies of the Altyn Tagh fault (modified from Wu et al., 2019b)阿尔金断裂带的不同分段与祁连山造山带和祁曼塔格−东昆仑断裂带共同构成了大型三联点，通过三联点与周缘断裂带的构造转换是其从分段演化到贯通的关键步骤。现今阿尔金断裂带与祁连山造山带的构造转换最受关注。大地测量学和构造地貌学研究发现，阿尔金断裂带中段的走滑速率约为10 mm/a，在阿克塞−肃北以东，速率快速下降到约7 mm/a，并在东端仅为1～2 mm/a（Zhang et al.，2007；Elliott et al.，2008；Li et al.，2018；图1）。徐锡伟等（2003）提出这一变化是三联点附近构造转换的结果，减少量转换为三联点派生出的祁连山内逆断层的隆升和走滑。这一观点与经典向东侧向挤出模型吻合（Tapponnier et al.，1982；Meyer et al.，1998），并得到越来越多构造地貌学、古地震学和大地测量学研究的支持（Xu et al.，2021；Li et al.，2022；Yan et al.，2024）。
相比第四纪构造活动研究，新生代演化历史中阿尔金断裂带−祁连山造山带构造转换的研究则相对不足，作为转换核心的三联点的活动则更加缺乏运动学机制的研究。Cheng et al.（2015b）提出祁连山地壳的新生代缩短量不足以吸收阿尔金断裂带约360±40 km的总走滑量，强调通过走滑运动祁连山向东挤出是实现阿尔金断裂带构造转换的重要方式。Yang et al.（2023）通过解析苏干湖地区的地表和地下构造，提出新生代早期党河南山的挤压缩短与增厚完全吸收了阿尔金断裂带的走滑量；中新世以来，祁连山内走滑断裂系统大规模启动，块体向东挤出与地壳缩短是阿尔金断裂带−祁连山造山带构造转换的主要形式。这些研究强调祁连山内部的走滑运动，但并未从运动学机制上深入探讨这些活动对阿尔金断裂带东段演化的影响。
由于野外条件和地质数据的限制，以往研究鲜少涉及阿尔金断裂带西段与祁曼塔格−东昆仑断裂带的构造转换，三联点也从未被清晰界定。Cheng et al.（2014）提出祁曼塔格断裂的分支是东昆仑断裂带西端在阿尔金断裂带作用下逐渐向北迁移的结果，即祁曼塔格−东昆仑断裂带与阿尔金断裂带的交汇位置（三联点）是不断移动的。
2. 三联点概念与应用
三联点（Triple Junction）概念是板块构造理论的重要基石之一，在3个岩石圈板块边界的交汇点即三联点处，相邻3个板块的相对运动速度矢量和为零。三联点概念最早由Mckenzie and Morgan（1969）提出，后经多位学者完善（York，1973；Patriat and Courtillot，1984）。研究者依据板块边界类型洋脊（R）、海沟（T）和转换断层（F），将三联点分为RRR、RRT、FFF等16种理论可能，但现实中出现的三联点类型有限（王振山和魏东平，2018）。同时，三联点可分为稳定三联点与不稳定三联点：前者位置和几何特征不会随板块运动而改变；相反，不稳定三联点无法长期存在，会通过转变断裂的性质、位置和几何特征，快速转化为不同类型的稳定三联点（Ingersoll，1982），这也是现今只能看到少数几种稳定三联点的原因。
通过3个板块边界的类型、方位以及相对运动速度可以分析三联点的稳定条件。用速度矢量代表每个板块的运动，这3个矢量的矢量和为零，形成闭合的三角形。一般来说，三联点的稳定性可以通过在速度矢量三角形中作辅助线来判定，辅助线代表板块交界处（断层）的方位，代表三联点可以移动的范围。当3条辅助线交于一点时，三联点达到稳定状态，否则不稳定。对于对称扩张的洋脊（R），辅助线为三角形中速度线的中垂线；对于转换断层（F），辅助线为速度的延长线；对于海沟（T），辅助线则需过逆冲断层上盘端点，作海沟的平行线，此时三联点不会因为俯冲而消亡（图2a、2b）。
图 2 三联点原理示意图A、B、C代表不同的板块；红色实线代表板块边界，蓝色虚线ab、bc、ac则代表板块AB、板块BC和板块AC之间的边界辅助线；ab、bc共线或者ac、bc共线时稳定a—三联点稳定性辅助线作法示意图；b—以FFT型三联点为例，说明三联点速度三角形及辅助线的作法，修改自McKenzie and Morgan（1969）；c—Mendocino三联点（FFT型）( Ingersoll，1982)Figure 2. Schematic diagram of triple junction principles(a) Schematic diagram illustrating the method of constructing auxiliary lines for triple junction stability; (b) An FFT-type triple junction is used as an example for the construction of the triple junction velocity triangle and auxiliary lines, adapted from McKenzie and Morgan (1969); (c) Mendocino triple junction (FFT-type) (Ingersoll, 1982) In (a) and (b), A, B, and C represent different tectonic plates; the red solid lines denote plate boundaries, while the blue dashed lines ab, bc, and ac represent auxiliary boundary lines between Plate AB, Plate BC, and Plate AC, respectively. The triple junction is stable when ab and bc are collinear or when ac and bc are collinear.三联点概念对分析断裂之间的相互作用、断裂的演化及对地质地貌具有重要意义。位于北美板块、太平洋板块和胡安德富卡（Juan De Fuca）板块之间的美国西部的门多西诺（Mendocino）三联点（图2c）稳定性研究是经典实例之一（Dickinson and Snyder，1979；Ingersoll，1982）。作为一个FFT型三联点，门多西诺三联点的稳定条件需要2条边界断裂共线（图2b）。然而，由于卡斯卡迪亚俯冲带和圣安德烈斯断裂并没有完全共线，门多西诺三联点并未达到稳定，而是持续沿圣安德烈斯断裂向北移动，三联点留下的“岩石圈空隙”导致了周边沉积盆地的沉降、火山喷发和环形地幔流（Levander et al.，1998；Furlong and Schwartz，2004；Zandt and Humphreys，2008）。时至今日，门多西诺三联点迁移对加州岩石圈、地震和地貌的影响依然备受研究者关注（Clubb et al.，2020；Shobe et al.，2021；Yeck et al.，2023）。
随着板块构造理论的发展，三联点概念也被广泛地用于陆内构造块体间的运动学分析，板块边界类型的洋脊、转换断层和海沟，可以分别对应块体间的正断层、走滑断层和逆断层（田勤俭和丁国瑜，1998；Steigerwald et al.，2020），但对应条件需要进一步厘定。一般来说，相对刚性的岩石块体的整体运动可以类比到板块运动，可以借鉴三联点概念分析，岩石圈块体边界属性可以类比不同的板块边界，而造山带或者盆地内部的构造转换不宜使用三联点分析。
青藏高原东北缘的三联点研究最早可以追溯到田勤俭和丁国瑜（1998）对海原附近青藏块体、鄂尔多斯地块和阿拉善块体形成的三联点的运动和构造特征分析。徐锡伟等（2003）利用地貌学识别了阿尔金断裂带东段肃北、石包城、疏勒河等多个三联点，并强调了左旋走滑与垂直活动之间的构造转换关系，完善了高原北缘的运动学模型。实际上，在造山带或者陆内一般断裂带相交位置构造运动学的转变，并非都是三联点的转换，三联点关注的核心是块体边界断层的相互影响。
青藏高原北缘的主要构造单位之间有较大的性质差异：①塔里木盆地和柴达木盆地均为巨厚中新生代沉积盆地，地球物理研究揭示了二者基底都是典型的刚性克拉通块体，相较周缘山脉具有低温热结构和更高的岩石圈强度（Wang，2001；孙玉军等，2013；宋晓东等，2015）；东昆仑山和祁连山同为青藏高原内部大型造山带，均为古生代—中生代造山带重新活化而成，且现今依然活跃（Law and Allen，2020）。②大地电磁研究显示，阿尔金断裂带形成巨大的电磁各向异性异常，而祁连山内部的异常较小（Dong et al.，2024）；东昆仑山岩石圈强度大，形成高电阻屏障（Yu et al.，2020）。③大地测量学研究也指出青藏高原北缘地区的水平应变集中于阿尔金断裂带主断裂沿线（Liu et al.，2024），祁连地块和东昆仑地块内部相对稳定，且具有旋转等刚性块体特征。因此，文中在讨论青藏高原北缘的构造运动中主要关注塔里木地块、柴达木地块、祁连地块和东昆仑地块之间的相对运动，当然不可否认的是其内部也都发育明显的变形，但与块体间的运动相比可能不在一个数量级，因此可以简化借用三联点概念进行分析。
文中所使用的地震数据下载自Global CMT（www.globalcmt.org；Dziewonski et al.，1981；Ekström et al.，2012），在Python软件中通过PyGMT绘制震源机制解（Tian et al.，2024）。原始GPS数据来自Wang and Shen（2020）与Ge et al.（2022），并使用FORTRAN语言将GPS数据从ITRF2014旋转至塔里木参考系，获得研究区域相对塔里木盆地的运动速度，并使用PyGMT绘制成图（Tian et al.，2024）。
3. 阿尔金断裂带与祁连山造山带构造转换：以肃北三联点为例
3.1 断裂特征与活动历史
祁连山造山带由一系列北西走向的断裂组成，自南向北包括党河南山断裂、野马河−大雪山断裂和昌马断裂等多条大型断裂。这些断裂向西止于阿尔金断裂带，与阿尔金断裂带形成了多个交点。文章以阿尔金断裂带与南祁连山党河南山断裂西段形成的肃北三联点为例，探究阿尔金断裂带东段构造转换的特点。
肃北三联点可视为塔里木地块、祁连地块和柴达木地块的交汇处，现在由阿尔金断裂带中段、东段和党河南山断裂组成（图3）。野马河−大雪山断裂的西段也汇入肃北地区，具有复杂的几何构造：西段为北东东向，与阿尔金断裂带平行；中段沿大雪山向东延伸；东段为北西向，与党河南山断裂平行。
图 3 肃北三联点及周边区域构造简图Figure 3. Tectonic map of the Subei triple junction and the surrounding area肃北盆地的沉积序列记录了三联点区域最早的构造活动。研究者曾对西水沟、铁匠沟等剖面进行了磁性地层学、沉积学和低温年代学研究，认为该地区的渐新世泥岩（Yin et al.，2002）或中新世晚期的砾岩（Wang et al.，2003；Sun et al.，2005；Lin et al.，2015；Lu et al.，2022）指示了初始构造变形与抬升。低温年代学研究提出党河南山在古新世至渐新世就已经隆升并剥露（Li et al.，2017；He et al.，2020），在中新世构造抬升更为显著（Shi et al.，2018；Yu et al.，2019），并持续活动至今（Yi et al.，2022；图3）。
相比之下，由于野外交通条件的限制，阿尔金断裂带东段和野马河−大雪山断裂的启动时间研究不足。Jolivet et al.（2001）曾对野马河与阿尔金断裂带间山脉的热年代学定年获得其冷却年龄约为19 Ma。冯志硕等（2010）通过剖析石包城盆地疏勒河组的岩石沉积特征，发现该盆地沉积颗粒呈东南粗、西北细的特征，古流向证据进一步指示其物源来自大雪山；而现今西北部的阿尔金断裂带东段沿线并未发育边缘相的粗碎屑沉积物，而是发育沉积中心相的细粒层系。据此推测，野马河−大雪山断裂在中新世活动增强，大雪山快速隆升，石包城盆地整体呈东南高、西北低的构造背景；之后阿尔金断裂带东段启动，在走滑拉分作用下形成了现今的石包城盆地。
党河南山断裂现今的构造属性和运动速度依然存在争议。该断裂第四纪逆冲活动强烈，发育大量断层陡坎，其活动特征已被深入研究（Shao et al.，2017；罗浩等，2020）。Xu et al.（2021）通过对错断的河流阶地进行宇宙成因核素10Be定年，提出党河南山断裂的抬升速率约为0.6±0.2 mm/a。与此同时，党河南山断裂是否具有走滑运动分量或走滑属性始终存在分歧。Meyer et al.（1998）基于震源机制解结果，提出党河南山断裂具有左旋走滑分量。但由于GPS数据受到台站分布的影响，目前尚没有足够清晰的数据表征其走滑运动方向特征（图3；Xu et al.，2021）。因此，文章暂时将党河南山断裂作为逆断层进行分析，即使其具有走滑分量也不影响相关运动学分析。
震源机制解显示，野马河−大雪山断裂西段以左旋走滑为主，兼具逆冲分量（图3）。通过实测地貌面错动数据和热释光定年，估算该断裂的平均水平滑动速率为1.27±0.18 mm/a，平均逆冲速率为0.4±0.07 mm/a。Luo et al.（2015）基于更为精细的地貌测量和年代学分析，提出野马河−大雪山断裂水平滑动速率约为2.18±0.32 mm/a、逆冲速率为0.4±0.07 mm/a。相比阿尔金断裂带在肃北以西约10 mm/a、肃北以东约7 mm/a的走滑速率，野马河−大雪山断裂的滑动速率较小，且不同分段走向、性质有所区别，说明其可能经历了多期复杂的构造演化。
3.2 三联点运动学分析与演化
在肃北三联点，将构造活动简化为塔里木地块、柴达木地块和祁连地块这3个地块之间的相对运动（图4）。按上文断裂发育时限分析，阿尔金断裂带中段和党河南山断裂最晚在渐新世已有活动，且阿尔金断裂带东段的活动晚于野马河−大雪山断裂。因此，推测阿尔金断裂带中段最早活动，在尾部形成挤压型马尾扇，组成马尾扇的断裂即为党河南山断裂与野马河−大雪山断裂的雏形。由于此时变形发生在祁连块体内部而非块体之间，因此不适用三联点分析。
图 4 肃北三联点稳定性演化示意图速度矢量三角形中tq、tql、qql分别代表塔里木地块与柴达木地块、塔里木地块与祁连地块、柴达木地块与祁连地块的辅助线Figure 4. Diagram of the stability evolution of the Subei triple junctionIn the velocity vector triangle, tq, tql, and qql represent auxiliary lines connecting the Tarim and Qaidam blocks, the Tarim and Qilian blocks, and the Qaidam and Qilian blocks, respectively.随着中新世阿尔金断裂带走滑运动的加速，显著增加的大位移量造成不同单元块体间的大规模相对位移，党河南山断裂与野马河−大雪山断裂成为分隔3个块体间明显相对运动的边界，在肃北附近形成三联点。此时三联点的组成为：阿尔金断裂带中段为左旋走滑断裂（F），党河南山为逆冲断裂（T），野马河−大雪山断裂西段以左旋走滑为主（F），肃北三联点可以被视为FFT型的三联点。由于地质体走滑速率的计算往往是依据地质体在一定地质历史时期内的位移获得的平均速度，难以分段测量，而且结果争议较大。因此文章借鉴现今GPS监测得到的断裂运动速率，将其作为阿尔金断裂带不同分段中新世的运动速率。阿尔金断裂带中段的走滑速率为10 mm/a，即塔里木地块与柴达木地块的相对速度；阿尔金断裂带东段的走滑速率取7 mm/a，即塔里木地块与祁连地块相对速度在阿尔金断裂带方向上的分量为7 mm/a（Zhang et al.，2007）。根据速度矢量三角形可知，除阿尔金断裂带东段的走滑分量外，祁连地块相对于塔里木地块有垂直于阿尔金断裂带的拉张分量，约为3.5 mm/a，即两者间存在伸展环境。这一伸展环境即是祁连造山带最西端发育石包城盆地、昌马盆地而非挤压隆升高山的构造条件。
由三联点分析可知，只要党河南山断裂和野马河−大雪山断裂不平行，边界辅助线tql（塔里木与祁连地块）、qql（柴达木与祁连地块）与tq（塔里木与柴达木地块）就没有交点，即阿尔金断裂带中段、党河南山断裂与野马河−大雪山断裂这3条断裂无法形成稳定的三联点（图4），这种情况不会长期存在。为了转化成稳定三联点，阿尔金断裂带向东直线延伸，野马河−大雪山断裂被逐渐置换替代，其西段被改造至与阿尔金断裂带平行。阿尔金断裂带的中段、东段与党河南山断裂形成了稳定的三联点。值得注意的是，尽管分析中使用现今速度数据对中新世三联点进行分析，但速度大小变化仅影响速度矢量三角形的相对形状，稳定性判断主要取决于3条边界的方向位置，与速度大小无关，因此该三联点稳定性分析不受相对运动速度的具体数值影响。
在现今阿尔金断裂带扩展的最前缘，红柳峡断裂并不与阿尔金断裂带主断裂平行，而是呈约20°的夹角，与当时野马河−大雪山断裂极为相似。因此可以推测，随着阿尔金断裂带运移量的不断累积，阿尔金断裂带、红柳峡断裂与北祁连山断裂组成的三联点会经历与当初肃北三联点相似的构造演化，并最终促使阿尔金断裂带继续沿直线扩展。
4. 阿尔金断裂带与祁曼塔格−东昆仑断裂带构造转换：以吐拉三联点为例
4.1 断裂特征与活动历史
祁曼塔格−东昆仑断裂带是位于柴达木盆地与东昆仑地块之间的大型左旋走滑断裂系，主体为东西向展布，西端在祁曼塔格地区形成一系列北西西向的线性断裂，并组成弓形构造。这些线性断裂与阿尔金断裂带在吐拉盆地处相交，因此，文章将由塔里木地块、柴达木地块和东昆仑地块交汇区域简化成三联点，称为吐拉三联点（图5）。
图 5 吐拉三联点及周边区域构造简图Figure 5. Tectonic map of the Tula triple junction and surrounding area吐拉三联点处北东向的断裂包括阿尔金断裂带西段、中段，吐拉断裂与白干湖断裂。阿尔金断裂带基本平直，走滑速率约为9～10 mm/a（He et al.，2013）；白干湖断裂位于吐拉盆地与祁曼塔格山脉之间，发育线性构造地貌，东北段隐伏并可能延伸至阿尔金山中，表明其最新活动并不明显，断裂为左旋走滑断裂。
阿尔金断裂带西段沿线的热年代学研究揭示了其始新世与中新世的活动，而吐拉断裂与白干湖断裂的活动历史则更为复杂。相关学者通过对比吐拉剖面、安西煤矿附近剖面与柴达木盆地采石岭剖面的岩性、化石发育特征以及碎屑锆石组成指示的源区特征等证据，发现其发育相似的侏罗系、古新统和始新统地层特征，提出吐拉盆地和柴达木盆地因为阿尔金断裂带的早期活动而分离（郭召杰和张志诚，1998；Cheng et al.，2015a）。据此推断，此时作为吐拉盆地边界的吐拉断裂与白干湖断裂在中新世及之前为阿尔金断裂带的分支断裂。Liu et al.（2021）基于白干湖断裂的地貌学与低温热年代学研究，提出白干湖断裂是与阿尔金断裂带密切相关且相连的走滑断裂，在中新世存在强烈的活动。结合已有研究和现今的地貌特征，推测现今吐拉盆地的边界−吐拉断裂与白干湖断裂，在新生代早期为阿尔金断裂带的尾端分支断裂，在中新世发生大规模走滑运动，逐渐分离了吐拉盆地与柴达木盆地。
三联点处北西向的断裂为祁曼塔格−东昆仑断裂带。研究普遍认为，东昆仑断裂带在中新世启动，并伴随着东昆仑山的大规模隆升（Duvall et al.，2013；Wu et al.，2019a，2021）。Cheng et al.（2014）基于祁曼塔格山北缘断裂的地震剖面和地貌特征提出，东昆仑断裂带西端受阿尔金断裂带左旋走滑位移的影响，自中新世以来自南向北逐渐迁移，形成近平行的祁曼塔格断裂带。在此模型中，祁曼塔格断裂带是东昆仑断裂带尾端移动的记录。
东昆仑断裂带的左旋走滑运动缺乏定量制约，根据现今大地测量学和地貌学估计其走滑速率约为10 mm/a，向东逐渐降低至2 mm/a（Kirby et al.，2007；Harkins et al.，2010；Li et al.，2011）。震源机制解和台站相对塔里木盆地的GPS数据显示，现今祁曼塔格断裂带以逆冲运动为主，兼具左旋走滑分量（图5；Ge et al.，2022），而断裂的滑动速率则缺乏数据。由于祁曼塔格断裂带与东昆仑断裂带性质相似、成因相同，在后续讨论中，文章将两者简化为祁曼塔格−东昆仑断裂带。
4.2 三联点运动学分析与演化
在吐拉段，将构造活动简化为塔里木地块、柴达木地块和东昆仑地块之间相对运动（图6），塔里木−柴达木地块与柴达木-东昆仑地块间的边界速度取自阿尔金断裂带西段和祁曼塔格−东昆仑断裂带的走滑速率，均约为10 mm/a。由速度矢量三角形可知，东昆仑地块相对于塔里木地块的速度可以分解为沿阿尔金断裂带的左旋走滑分量和垂直阿尔金断裂带约为5 mm/a的拉张分量。因此，阿尔金断裂带西段以左旋走滑为主，且处于伸展环境。这一特征仍体现在现今的阿尔金断裂带西端，例如在伸展背景下发育的阿什库勒盆地。此外，该地区的地震活动以拉张型强震为主（Bie and Ryder，2014；Pan et al.，2015），并伴随活跃的火山活动（李海兵等，2006）。
图 6 吐拉三联点稳定性演化示意图速度矢量三角形中tq、tk、kq分别代表塔里木地块与柴达木地块、塔里木地块与东昆仑地块、东昆仑地块与塔里木地块的辅助线Figure 6. Diagram of the stability evolution of the Tula triple junctionIn the velocity vector triangle, tq, tk, and kq represent auxiliary lines connecting the Tarim and Qaidam blocks, the Tarim and Eastern Kunlun blocks, and the Eastern Kunlun and Qaidam blocks, respectively.结合白干湖断裂的几何特征，推测该三联点的运动演化过程为：阿尔金断裂带初始活动时以中段的运动为主，西部尾端派生的吐拉断裂与白干湖断裂组成伸展型马尾扇构造，此时变形局限于昆仑地块内部，3个块体间尚没有大规模相对位移，没有形成三联点。在东昆仑断裂中新世的大规模活动开始后，柴达木地块和东昆仑地块相对运动，形成了三联点，而此时3条边界辅助线不能相交于一点，即无法形成稳定三联点。为了达到稳定状态，阿尔金断裂带沿直线向西延伸，白干湖断裂的活动逐渐减弱。此时，边界辅助线tq（塔里木地块与柴达木地块）和tk（塔里木地块与东昆仑地块）重合，三联点在阿尔金断裂带与祁曼塔格−东昆仑断裂带的交点处达到稳定，形成了现今的构造格局。
值得注意的是，由于柴达木地块伴随着阿尔金断裂带的走滑活动向北移动，祁曼塔格地区的断裂会向北迁移，形成发散状的断裂带，而且具有逆冲分量。所以吐拉三联点无法如肃北三联点一样集中，而是在一定区域内移动，没有明确固定的位置。这与以往对祁曼塔格−昆北断裂带的研究相一致（Cheng et al.，2014，2015c）。
5. 讨论
5.1 阿尔金断裂带东西两端构造转换方式
阿尔金断裂带、祁连山造山带和祁曼塔格−东昆仑断裂带是青藏高原北部最为重要的3条大型构造带，三者的活动与相互影响控制着高原北缘的几何特征和构造框架。三联点作为大型块体边界断裂带的交汇点，是协调青藏高原不同块体间相互运移和构造变形的关键节点。肃北三联点和吐拉三联点的构造特征反应了阿尔金断裂带东、西两端构造转换的方式与差异。
在阿尔金断裂带东段，祁连山边缘与内部多个逆冲和走滑断裂共同吸收了阿尔金断裂带的左旋位移，表现为块体的抬升与挤出；在阿尔金断裂带西段，祁曼塔格−东昆仑断裂带共同通过大型左旋走滑运动吸收印度板块的运动量。地震统计数据表明，肃北三联点主要断裂沿线均有地震记录，吐拉三联点的地震活动则集中在阿尔金断裂带的双弯曲处，说明前者的构造运动更为活跃，三联点构造转换更加集中。从阿尔金断裂带的滑动速率测量中可知，在肃北三联点的东、西两侧，阿尔金断裂带的走滑速率明显下降；相反，在吐拉三联点附近，阿尔金断裂带的活动速率没有明显变化，而三联点位置也随着祁曼塔格−东昆仑断裂带的移动在一定范围内迁移。在地貌活动上，党河南山和大雪山断裂前缘均发育冲断带，且在第四纪以来具有持续加强的趋势（Xu et al.，2021；Yi et al.，2022）；祁曼塔格断裂与白干湖断裂的构造地貌发育则更为成熟，仅有小规模错断的河流显示较弱的断裂活动（Liu et al.，2021），体现断裂活动仅局限于块体内部。
阿尔金断裂带东、西两端不同构造转换方式的差异反应了阿尔金断裂带和青藏高原演化的方向性和阶段性。随着青藏高原的向北、向外扩展，祁连山造山带的活动不断增强，并至今仍在向北逆冲；相反，祁曼塔格−东昆仑断裂带的活动主要受制于青藏高原的挤出，以东部的走滑断裂为主，逆冲活动相对较弱。因此，吐拉三联点记录了始新世—中新世阿尔金断裂带和祁曼塔格−东昆仑断裂带的活动；肃北三联点则反映了青藏高原北缘从早期响应碰撞到后期大幅隆升的全过程。
5.2 三联点演化对阿尔金断裂带扩展的意义
阿尔金断裂带长达1600 km，其扩展生长方式一直备受争议，具有代表性的观点包括北向扩展、快速贯通、双向扩展和构造重组4个模型。北向扩展模型依托于经典的青藏高原北向生长模型，认为阿尔金断裂带随青藏高原向东北方向扩展（Métivier et al.，1998；Meyer et al.，1998；Tapponnier et al.，2001；Wang et al.，2006，2016）。快速贯通模型基于低温年代学和沉积记录，认为阿尔金断裂带在新生代早期便作为大型走滑断裂带，快速贯通至祁连山，随后在断裂系统内部逐渐演化形成现今面貌（Yin et al.，2002）。这一假设更符合强调同步变形的黏性薄席高原模型。阿尔金断裂带在这两个经典模型之外，近年来学者依据更丰富的研究资料提出了更复杂的扩展模型，如双向扩展模型依据低温年代学数据分布、沉积速率的变化和古地磁磁偏角的研究，认为断裂从中段向东、西两端双向扩展，且强调中新世以来阿尔金断裂带构造活动在不断加强（Li et al.，2021；谢皓等，2022）；构造重组模型依托近年来对北阿尔金山的研究成果，提出阿尔金断裂带的走滑运动最初由北阿尔金断裂承担，并与金雁山形成大型的受阻弯曲，现今的主断裂在中新世才开始贯通活动（Wu et al.，2019b；Gao et al.，2022）。
虽然这些模型都能解释所在区域的构造现象，但结论扩展到阿尔金断裂带全段时，会出现矛盾或者难以解释之处。最重要的是，阿尔金断裂带中段和北段存在大量新生代早期走滑断裂的证据，北向扩展模型和构造重组模型难以解释。近期Yi et al.（2024）通过对同构造沉积中的碳酸盐岩U-Pb定年，证实59 Ma阿尔金断裂带的走滑活动在现今索尔库里盆地启动，即阿尔金断裂带中段最早破裂；肃北盆地始新世的快速沉积也与阿尔金断裂带构造活动有关（宋春晖，2006）；吐拉盆地与柴达木盆地的分离也需要早期阿尔金断裂带的走滑活动（Cheng et al.，2015a）。相比之下，快速贯通模型和双向扩展模型能解释绝大多数沉积和热年代学记录，但扩展的过程和机制讨论仍需完善。
在此基础上，文章提出分段破裂−双向扩展的模型：柴达木段的阿尔金断裂带最先启动，反映了阿尔金断裂带活动的本质−塔里木与柴达木2个大型刚性块体间的走滑运动。同时，断裂两端派生出了次级构造，在东端形成挤压型马尾扇，导致新生代早期党河南山西端的隆升与肃北盆地内沉积记录；在西段形成拉张型马尾扇，表现为吐拉盆地内沉积及其与柴达木盆地的初始分离（图7a）。中新世时期，由于青藏高原活动增强，阿尔金断裂带变形量增加，现有的断裂难以吸收全部的位移，造成多块体间规模较大的相对位移，在阿尔金断裂带两端形成三联点（图7b）。鉴于三联点稳定性的要求，阿尔金断裂带“截弯取直”，原本的马尾断裂被废弃，主断裂沿直线向东西两端扩展，与此前可能的分段断裂相连贯通，组成现今长达1600 km的大型断裂（图7c）。
图 7 阿尔金断裂带与三联点演化示意图Figure 7. Diagram of the evolution of the Altyn Tagh fault and triple junctions(a) Early Cenozoic segmental initiation of the Altyn Tagh Fault (ATF); (b) Miocene activity enhancement, leading to the formation of unstable triple junctions; (c) Post-Miocene shortcutting and through-going of the ATF.阿尔金断裂带这一双向扩展的演化过程，响应了青藏高原同步启动、变形向北扩展的特征，突出了柴达木盆地、祁连山和东昆仑山不同岩石圈特征对断裂演化的影响，支持了非均质岩石圈模型。青藏高原内断裂广布，大型断裂之间的构造转换复杂，构成了多个三联点，三联点概念和分析应用具有更大的推广空间。
6. 结论
（1）阿尔金断裂带在新生代经历了分段破裂−双向扩展的演化历程。
（2）中新世野马河−大雪山断裂与祁曼塔格−东昆仑断裂带的启动导致不稳定的肃北三联点和吐拉三联点形成，促使阿尔金断裂带“截弯取直”，向东西两端扩展。类似的扩展在现今的阿尔金断裂带两端持续进行，这是阿尔金断裂带扩展的主要方式。
（3）三联点特征分析对揭示板块/地块交界处的运动学关系、分析断裂之间的相互作用与断裂属性具有重要意义，在区域构造分析中有广泛应用价值。
致谢：感谢加州大学洛杉矶分校沈正康教授分享GPS数据与FORTRAN代码、并给予帮助。杨屹洲博士参与了最初讨论，在此表示感谢。
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图 1 当雄错构造地质背景与泉华群概况
DX—当雄错盐湖；DR—当若雍措；XR—许如错a—当雄错构造地质背景；b—当雄错泉华分布概况（红线区域指示新、老泉华的分布，影像呈现白色的区域为出露地表的碳酸盐）；c—当雄错泉华群野外概况（拍摄位置位于南泉华群一个泉华体顶部）
Figure 1. Tectonic setting of Damxung Co salt lake and overview of the travertine group
(a) Tectonic setting of the Damxung Co salt lake; (b) Overview of travertine distribution in the Damxung Co salt lake (The red lines indicate the distribution of new and old travertines, and the white areas in the image represent exposed carbonate on the surface); (c) Field photo of the travertine outcrops near the Damxung Co lake (taken at one of the travertine top of the southern outcrops) DX−Damxung Co salt lake; DR−Tangra Yumco lake; XR−Xuru Co lake
图 2 当雄错硼同位素地球化学行为与硼矿形成过程.
a—湖水蒸发浓缩至碳酸盐析出阶段；b—干盐滩阶段；c—溶蚀湖阶段
Figure 2. Geochemical behavior of boron isotope and the formation process of boron minerals in the Damxung Co salt lake
(a) Evaporative concentration and carbonate precipitation of the Damxung Co salt lake; (b) Total desiccation of the Damxung Co salt lake; (c) Formation of a salt dissolving lake in the Damxung basin
图 3 当雄错湖岸碳酸盐沉积剖面及光释光年代序列
Figure 3. Lacustrine carbonate sections in the Damxung Co salt lake and their OSL dating results
图 4 随着总碳酸盐沉积的硼矿占比（n）和现今湖水来自碳酸盐的硼占比（m）变化，当雄错未剥蚀碳酸盐的硼矿资源量情况
Figure 4. Boron resource of residual carbonate on lakeshore as a function of proportion of boron in total boron resource derived from carbonate (n), proportion of boron from carbonate erosion in lake water (m) and the degree of carbonate erosion (s)
图 5 随着总碳酸盐沉积的硼矿占比（n）和现今湖水来自碳酸盐的硼占比（m）变化，当雄错总硼矿资源量情况
Figure 5. Total boron resource as a function of proportion of boron in total boron resource derived from carbonate (n), proportion of boron from carbonate erosion in lake water (m) and the degree of carbonate erosion (s)
图 6 随着总碳酸盐沉积的硼矿占比（n）和现今湖水来自碳酸盐的硼占比（m）变化，当雄错湖底未溶蚀的盐沉积和晶间卤水的硼矿资源量情况
Figure 6. Boron resource buried in the bottom of the Damxung Co salt lake as a function of proportion of boron in total boron resource derived from carbonate (n), proportion of boron from carbonate erosion in lake water (m) and the degree of carbonate erosion (s)
表 1 海水和盐湖卤水中黏土矿物吸附的硼同位素分馏系数
Table 1. Boron isotopic fractionation factor (α) during adsorption of boron on clay in seawater and salt lake brine
编号 研究对象 分馏系数α 文献出处 1 海水与沉积物 0.975，0.976 Spivack et al.，1987；Palmer et al.，1987 2 柴达木盐湖−咸水湖与对应沉积物 0.987~0.998 Shirodkar and Xiao，1997；肖应凯等，1999 3 大柴旦卤水与沉积物 0.987~0.992 Xiao et al.，1992 4 卤水与沉积物模拟吸附实验 0.982~0.999 Xiao and Wang，2001（不包括负分馏） 5 尕海盐湖（青海湖旁边）与湖底淤泥 0.985 孙大鹏等，1993 
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表 2 石盐蒸发实验硼含量和硼同位素组成（据Liu et al.，2000修改）
Table 2. Boron concentrations and isotopic compositions in rock salt evaporation experiments (revised after Liu et al., 2000)
卤水 石盐 α B/ (μg/g) δ11B/ ‰ B/ (μg/g) δ11B/ ‰ 实验-1（纯石盐） 677 10.9 4.4 10.8 0.9999 710 11.2 8.0 10.7 0.9995 1120 11.0 12.2 10.8 0.9999 2871 10.8 39.7 10.9 1.0000 实验-2（含石膏石盐） 585 11.1 6.9 10.8 0.99996 712 10.6 12.4 9.2 0.9987 1038 10.5 17.7 7.1 0.9966 2303 11.0 48.0 7.8 0.9965
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表 3 不同水化学类型盐湖的硼、锂同位素变化特征
Table 3. The characteristics of boron and lithium isotopes in salt lakes of different hydrochemical types
水化学类型 主要盐沉积 硼、锂同位素特征 代表盐湖 硫酸盐型 芒硝+石盐 δl=δi 大柴旦，一里坪，东台，西台等 氯化物型 芒硝+石盐 δl=δi 察尔汗，钾湖，巴仑马海等 碳酸盐型 碳酸钙+芒硝+石盐 δ11Bl>δ11Bi；δ7Lil-δ7Lii<2‰ 扎布耶，当雄错 碳酸盐型 碳酸镁+芒硝+石盐 δ11Bl-δ11Bi<2‰；δ7Lil与δ7Lii关系待定 班戈错
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表 4 当雄错各类样品硼含量和硼同位素组成
Table 4. Boron concentrations and isotopic compositions of samples from the Damxung Co salt lake
样品类型 B/×10−6 δ11B /‰ 数据来源 地热水 0.40~6.20 −9.8~−8.5 Lü et al.，2013 冷泉水 0.12~0.61 −14.5~-14.1 Lü et al.，2013 河水 0.02~0.15 −4.9~−1.2 Lü et al.，2013 盐湖卤水（0.1~14.6 m) 208.10~1760.80 −18.5~−17.4 北京绵平盐湖研究院，2006；Lü et al.，2013 钙华 90.40~236.00 −29.5~−24.9 Lü et al.，2013 碳酸盐 47.50~264.00 −37.2~−35.3 Lü et al.，2013
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表 5 当雄错泉华铀系年龄
Table 5. U-Th results of travertine samples near the Damxung Co salt lake
样品编号 样品类型 238U/×10−9 232Th/×10−9 230Th/232Th/×10−6 δ234U 230Th /238U 230Th年龄/a（未校正） 231Th年龄/a（校正） DXC003-1 泉华 670±2 10076±203 43.4±0.9 452.9±3.2 0.0395±0.0003 3003±23 2702±214 DXC003-15 泉华 302±1 14692±295 13.1±0.3 500.3±3.0 0.0386±0.0006 2836±44 1890±671 DXC003-8 泉华 454±1 8601±173 97.6±2.0 421.4±2.4 0.1122±0.0004 8935±36 8549±275 DXC009-2 泉华 125064±383 59295±1198 1227.8±25.1 521.4±2.5 0.0353±0.0002 2557±12 2548±14 DXC009-14 泉华 46742±165 496200±10093 72.2±1.5 592.3±3.9 0.0465±0.0003 3225±22 3032±139
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