Study on Dynamics Mechanism of Magmatic Copper-Nickel Sulfide Deposits in Orogenic Belts
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摘要:
针对造山带岩浆铜镍硫化物矿床成矿岩浆具有富水、源区不均一、弧岩浆元素特征以及矿床中的硫来源多样的特征，前人提出其成矿动力学模式主要包括地幔柱叠加造山带、板块俯冲和地幔柱相互作用、俯冲交代改造的岩石圈地幔部分熔融、后碰撞伸展阶段软流圈地幔和岩石圈地幔共同作用以及板块断裂引起软流圈地幔上涌减压熔融等多种观点。纵观地球演化历史，经历多期次造山作用，但并不是所有造山带均形成了岩浆铜镍硫化物矿床。因此，造山带中能够形成岩浆铜镍硫化物矿床成矿的关键因素有待进一步明晰。基于上述模式均指向造山带岩浆铜镍硫化物矿床均来源于俯冲交代地幔源区，形成时限滞后于俯冲峰期的研究结果和地质事实，笔者提出了造山带铜镍硫化物矿床两阶段成矿动力学模式。第一阶段：俯冲期内地幔橄榄岩被俯冲板片形成的硅质熔体交代，交代过程中，俯冲熔体导致镍等元素从橄榄石中释放以及自身携带硫的释放，从而形成含有斜方辉石和镍硫化物的辉石岩为主地幔源区，第二阶段：俯冲碰撞期结束后，富集辉石和镍硫化物地幔通过拆沉方式进入软流圈地幔发生再次熔融，熔融条件转变成近似无水条件，镁铁质岩浆会分异形成富集亲铜元素形成的硫化物堆晶或岩浆硫化物矿床。区域上深大断裂、韧性剪切带和缝合带作为岩浆通道，是母岩浆脱离熔融源区后岩浆过程的富集通道，源区和岩浆过程共同作用形成造山带岩浆铜镍硫化物矿床。
Abstract:Previous studies have proposed various ore-forming dynamic models for Cu-Ni sulfide deposits in orogenic belts, including mantle plume overlapping orogenic belts, plate subduction and mantle plume interaction, partial melting of the lithospheric mantle, mixing of asthenospheric and lithospheric mantle during post-collision extension, and decompression melting caused by tearing of slab leading to asthenospheric mantle upwelling. However, the multiple episodes of subduction-accretion orogeny throughout the history of Earth evolution, the above dynamic processes have occurred, but Cu-Ni sulfide deposits have not been formed. Therefore, the key factors for the formation of Cu-Ni sulfide deposits in orogenic belts await further clarification. Based on the fact that the above models all point to Cu-Ni sulfide deposits in orogenic belts originating from subducted metasomatic mantle sources and forming after the peak subduction period, we propose a two-stage ore-forming dynamic model for Cu-Ni sulfide deposits in orogenic belts. Stage One: During the subduction period, interactions between mantle peridotites and silicic melts from the subducting slab lead to the release of elements such as nickel from olivine and sulfur carried by the subduction melts, thus forming a mantle source dominated by pyroxenite containing orthopyroxene and nickel sulfides. Stage Two: After the end of the subduction-collision period, the pyroxenite mantle source enriched during subduction enters the asthenospheric mantle through delamination and undergoes remelting, where the melting conditions change to near hydrous-free conditions. In this condition, these mafic magmas differentiate to form sulfur-rich, copper-affinitive sulfides crystallizing into sulfide piles or magma sulfide deposits. The large depth fault, ductile shear zones, and suture zones serve as magma channels for the enrichment of the parent magma, with the combined action of source region and magmatic process leading to the formation of Cu-Ni sulfide deposits in orogenic belts.
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近年来，随着计算机技术的不断发展，磁法勘探资料反演研究已由原始的手工计算发展到以计算机为主的算法研究，由单一反演方法发展到多方法的综合反演技术，由二维平面向三维立体发展。磁法三维反演解释技术是近年来国内外重磁研究的热点之一。磁性反演主要有两类，一类是将场源的边界形态作为反问题求解的形态反演；一类是将场源的物性参数作为反问题求解的物性反演。形态反演的模拟是通过任意多边体或多面体来模拟复杂地质体，它可以利用人的经验对反演进程加以引导，通过人机交互模式将反演结果反馈，根据反馈结果进行约束，进而提高反演效率和形态。磁法建模基于磁法形态反演的发展，经历了的人机交互建模技术、三维可视化技术等，对于真实地质体的模拟能力有了较大提升。
通过各种地球物理观测数据建立地表以下地质模型，结合地球物理异常数据及地质剖面进行建模是了解地下深处构造单元的重要方法，B.R.Goleby等（2001）在澳大利亚Yilgarn东Norseman-Wiluna地区采用2.5Ｄ重力模拟，研究了该区绿岩的深度及与花岗岩之间的位置关系。Roy和Clowes（2000）利用反射地震、重磁2.5Ｄ和3Ｄ建模，对加拿大哥伦比亚省富含斑岩型铜钼矿的Guichon Cheek岩基进行了深部结构研究，建立了三维模型，岩基的边界、内部结构、岩浆通道清晰可见；Malehmir等（2006，2009）在瑞典北部Skellefte成矿带进行了的３Ｄ地质－地球物理建模，瑞典Upplasa大学在该成矿带西部的Kristineberg矿集区开展了高分辨率反射地震剖面和重、磁、震联合反演解释研究，建立了该地区３Ｄ地质－地球物理模型；向中林（2009）将三维地质建模及可视化用于矿床的成矿地质条件分析，应用于危机矿山找矿；吕庆田等（2010）在铜陵矿集区狮子山矿田利用反射地震成像及钻孔资料约束，进行重力3D反演，建立了３Ｄ地质模型,初步实现了狮子山－铜官山矿田地壳结构“透明化”；祁光等（2012）以安徽泥河铁矿为例开展先验地质信息约束的三维地质重磁建模研究；严加永等（2014）在安徽省沙溪铜矿进行三维重磁反演，通过反演磁化率体和密度体，识别了四种主要的岩体类型，为三维地质建模提供借鉴型;陈炳锦（2021）在陕西省龙王沟地区以磁测数据为基础建立了三维地质体模型，只管预测磁铁矿的空间分布和形态。王昊（2022）基于航磁数据开展位场分离获取重磁反演的异常数据，完成人机交互反演，通过剖面建立了朱溪矿矿区三维地质建模。随着信息化的发展，三维地质建模及可视化已呈现出较为明显的优势，也是对于开展深部找矿研究的必要手段。
1984年，法国地质物理学家Morlet首次提出“小波分析”的概念，引入了被命名为“Morlet小波”的一种基函数，用于时间和频率的局域变化，进而在信号中提取信息，通过伸缩和平移等功能实现对信号的多尺度细化分析，解决了许多难题。1987年，信号分析专家Mallat将计算机的多尺度分析思想引入到小波分析中，提出了多分辨分析的概念，研究了小波变换的离散化情形，提出了著名的分解与重构快速算法，即“Mallat”算法。wickerhuaes（1991）、Beylkin（1990）、Coifman（1990）等人提出了“小波包”的概念，将Mallat进一步优化，提出了小波包算法，进过30多年的发展，小波理论不断完善，成熟，小波分析在信号处理，图像处理语音识别等众多非线性学科领域取得了重大成就。小波多尺度分析法可以将磁异常分解到不同的尺度空间中，并且尺度的大小决定了异常所反映的地质体的规模和埋深情况。侯尊泽（1995，1997）、杨文采（2001，2004）等人将小波变化应用于重力异常分析，李宗杰（1997）在位场数据处理中引入小波变换，将异常信号分解、滤波、重建，达到了提取区域异常和局部异常的目的。张恒磊（2009）研究了小波分析的磁测数据处理流程，
宁津生（2010）等人利用连续小波变换进行了干扰源分离和场源深度确定的模拟，发现小波变换边缘分析可有效确定场元深度。刘芳（2013）等人通过二位小波多尺度分析，实现了不同场源深度密度体与重力异常分离的目的。刘天佑（2007）、张恒磊（2009）、王建复（2013）、尚世贵（2014）、宋小超（2016）、蒋勇平（2018）等人将小波多尺度分析用于重磁法数据处理，精细处理携带了多尺度地质信息的位场信号，使得小波多尺度分析方法在资料的位场分离领域得到了广泛的应用。
根据频率与深度的对应关系可知：小波尺度代表高频信号，大尺度代表低频信号，低频部分反映的是浅层信息，高频部分反应深部信息，通过小波多尺度因子变化将异常信号进行分解到不同的细节。借助功率谱计算，来反映不同细节对应的异常源深度。功率谱可以借助重磁异常的径向对数功率谱分析，来定量的确定重磁异常的场源深度。Bhattacharyya（1966）给出了频率域内单个均匀磁化棱柱体的总磁场场强表达式，提出了一种矩谱法来直接计算磁性体界面深度；Spector和Grant（1970）提出了一种基于统计理论模型的“等效论”磁异常数据处理方法，侯重初（1985）等利用磁性体导数异常的对数功率谱直接计算磁性体下底深度推导出利用磁异常垂向一阶导数的对数功率谱计算二度板状体下底埋深的近似公式；申宁华（1985）提出先计算磁性体的顶深和质心深度，在“磁性体顶部距离质心与质心距离底部相等”的假设条件下，间接求出磁性体的底部埋深。张先（2007）等人研究了不同尺度磁性体的场源深度。
党月辉（2008）研究了功率谱估算磁源深度的方法，给出了使用条件和范围。段瑞锋（2016）将功率谱计算用于银额盆地居延海坳陷磁测异常解释中笔者利用小波多尺度分解将陕西省略阳县金子山地区磁测数据分解为几个不同阶的细节，通过引用直立矩形棱柱体功率谱计算各阶细节异常的对应的场源深度。结合区域地质背景，地形地貌及打钻的钻孔信息，利用Voxler平台，在虚拟环境下实现二维小波多尺度分解数据的三维离散可视化，建立三维地质体模型。预测岩浆热液通道部位、岩体空间形态，并结合时间域激电测深，圈定矿体的赋存空间，提高地球物理勘探解释的准确性、可靠性，实现地质、物探和地表及深部信息的集成展示，服务于分析研究和决策支撑，为下一步钻孔设计提供依据。
1. 研究区区域地质背景
陕西勉（县）-略（阳）-阳（平关）三角区是重要的多（贵）金属矿集区，常见有中酸性沉积岩带和超基性—中基性—中酸性侵入岩及古生代碎屑岩和碳酸盐岩。整体上呈“东收西开”的扇骨形区域构造。南侧为汉江大断裂控制，北面为二里坝—铜厂-七里沟断裂，控制着区域内构造活动和岩浆活动。金子山金铜多金属矿即分布在二里坝—铜厂-七里沟断裂中段（图1）。
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图 1 勉略阳地区区域地质构造略图（据西北有色地质勘查局七一一总队，2015）1.勉略康构造混杂岩带；2.震旦纪碎屑碳酸盐岩；3.太古界绿岩；4.中部火山岩浆岩带；5.中晚元古界中酸性火山岩；6.基性岩体；7.中下元古界基性火山岩；8.基底拼合主构造线；9.超基性岩；10.闪长岩；11.太古界鱼洞子岩群；12.中下元古界东沟坝组13.中下元古界何家岩岩群；14.金矿床；15.铜矿床；16.多金属矿床；17.镍矿床；18.铁矿床；19.古基底缝合带；20.地名；21.工作区Figure 1. The Regional geological structure of Mianlveyang area2. 研究区地质地球物理特征
工作区出露地层主要为郭家沟组第一亚层、震旦系断头崖组及第四系（图2）。郭家沟组第一亚层主要岩性为细碧岩。震旦系断头崖组主体分布在测区西北部，与下伏火山岩呈不整合接触。是一套以灰岩、白云质灰岩、含碳绢云母板岩、碳质板岩、板岩、凝灰质板岩构成的碎屑化学沉积变质岩。区内断裂构造发育，分为近EW向、NW向、近SN向和NE向4组。控矿断裂为NE向断裂，其余为破矿构造。区内侵入岩发育，超基性岩大面积分布，基性、中酸性岩体多呈岩墙、岩脉或岩株产出。超基性岩第一期主要为菱镁岩、滑镁岩，磁性较弱，据研究成果表明MgO含量明显偏高，CaO和Al2O3偏低，属深源浅成岩浆类型，据纯橄岩年龄测试Rb-Sr等时线年龄（927±49）Ma，属晋宁期产物；第二期主要为蛇纹岩，碎裂状蛇纹岩、纯橄榄蛇纹岩（原岩：橄榄石）、纤胶蛇纹岩、叶蛇纹岩、绢云母化蛇纹岩、斜辉绿橄岩、含磁铁矿蛇纹岩，磁性较强，与晋宁期超基性岩带同位产出，构成复合超基性岩带，同位素年龄328～540 Ma（K-Ar法），为加里东-海西期产物。根据定向标本的测定结果显示，二里坝-铜厂背斜发生于该期次岩体产出之后，最后在金子山地区出露剩磁方向较为凌乱的含磁铁矿角砾状蛇纹岩，为负异常，金子山的金铜矿出露于含磁铁矿角砾状蛇纹岩中。对前期施工的探槽钻探工程，结合民坑调研工作重新进行综合研究后，认为金子山金铜矿体是加里东-海西期产物，后被含磁铁矿角砾状蛇纹岩推覆至地表。
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图 2 工作区地质图1.灰岩；2.白云质灰岩；3.板岩；4.炭质板岩；5.凝灰质板岩；6.含炭绢云母板岩；7.斜长花岗岩；8.云英岩；9.闪长岩；10.辉绿岩；11.细碧岩；12.菱镁岩；13.石英菱镁岩；14.滑镁岩；15.蛇纹岩（原岩：橄榄石）；16.蛇纹岩（原岩：斜辉石）；17.含磁铁角砾状蛇纹岩；18.未见矿钻孔；19.见矿钻孔；20.断层Figure 2. Geological map of working area根据测定的物性标本显示（表1），磁性最强的是磁铁矿和蛇纹岩，郭家沟组的细碧岩、震旦系的碎屑化学沉积变质岩、晋宁期的菱镁岩和滑镁岩、云英岩、斜长花岗岩磁性较弱。在本工作区蛇纹岩呈低阻低极化，滑镁岩呈高阻低极化特点，但是含磁铁角砾状蛇纹岩中含有大量的硫铁矿，呈低阻高极化特点。综上所述利用蛇纹岩与围岩的磁性、电性差异，预测浆热液通道部位、岩体空间形态是可行的。
表 1 工区岩（矿）石标本磁参数测定统计表Table 1. Area of Rock (Ore) specimen magnetic parameters measurement calculation table岩（矿）石名称 κ/（4π×10−6 SI） Mr /（10−3 A/m） 变化范围 常见值 变化范围 常见值 磁铁矿 34 18000 ～63047 33480 2000～ 20000 12850 含磁铁角砾状蛇纹岩 40 14141 ～82764 40728 1863 ～27505 7546 蛇纹岩 54 1000 ～3600 1900 400～ 2600 1100 滑镁岩 39 100～800 433 150～600 226 细碧岩 30 80～300 175 78～425 179 斜长花岗岩 31 60～400 141 60～300 133 云英岩 30 100～600 244 100～500 268 金子山金铜矿前期勘查工作对成矿控制因素、矿化类型研究较少，致使勘查工程见矿不佳，对整个金子山地区的主攻矿化类型、主攻矿种缺少全面认识，进而在勘查靶区、靶位选取及工程布设方面存在一定的盲目性，造成进一步勘查工作难以深入，找矿无法取得突破。笔者主要对前期施工的探槽钻探工程结合民坑调研工作的重新进行综合研究后，认为金子山金铜矿为与加里东-海西期超基性岩有关的岩浆熔离型金铜镍多金属块状硫化物型，利用蛇纹岩与围岩的磁性、电性差异，确定蛇纹岩产生的异常与其对应三维空间的定量关系，把蛇纹岩产生的异常范围划分出来，从而约束反演结果，得到最优解。通过预测岩浆通道底部或者转折端位置，以期发现深部的盲矿体。
3. Voxler建模
根据小波多尺度分解塔式算法的低阶细节不变性，对略阳县金子山地区垂直磁异常（ΔZ）单位（nT）进行小波多尺度分解处理，根据小波多尺度因子的变化，将磁异常信号分解到不同阶的细节，不同阶的细节，代表了不同深度的局部场。
利用Voxler三维可视化科学制图软件，对离散的垂直磁异常数据进行小波多尺度分解，分解为1～6阶细节和逼近（图3）。
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图 3 二维小波多尺度分解a.垂直磁异常；b.一阶细节；c.二阶细节；d.三阶细节；e.四阶细节；f.五阶细节；g.六阶细节；h.六阶逼近Figure 3. 2D Wavelet Multiscale Decomposition据党月辉（2008）通过对Bhattacharrya提出的功率谱表达式进行化及处理和求取平均径向功率谱后，推导出的有限延深直立矩形棱柱体平均径向功率谱表达式
$$ \mathrm{I}\mathrm{n}\mathrm{ }\mathrm{E}\left(\gamma \right)=A-2{h}_{t}\gamma +2In（1-{e}^{-tr}） $$ (1) 对公示中的r求极值，并取自然对数，得到：
$$ r=\frac{In\left(1+\dfrac{h}{t}\right)}{t} $$ (2) 其中A为常数，r为径向频率，t为棱柱体的延伸，h为埋深
由上式可知r存在极大值拐点。当已知棱柱体埋深时，可以根据径向频率的峰值位置估计其延深t，$ 2In（1-{e}^{-tr}） $的结果，反过来可以对果断埋深进行延伸影响的改正。
根据功率谱分析得出：1阶细节异常场源似深度为22 m；2阶细节异常场源似深度为61 m；3阶细节异常场源似深度为124 m；4阶细节异常场源似深度为238 m；5阶细节异常场源似深度为474 m；6阶细节异常场源似深度为860 m；6阶逼近场源似深度为1812 m。异常主要为大面积加里东-海西期磁性较强的蛇纹岩引起，磁性体较为简单，通过地形改正，用似深度代替真深度，将传统的二维小波多尺度分解数据整合为三维数据。（图4）。
借助VolRender（形体渲染）模块编制形体渲染图（图5），根据形体渲染图件色彩变化特征、区内地质及钻孔等先验信息，提取大于50 nT的磁异常区间，在Isosurface（等值面）模块下编制空间等值面图（图6）。
该等值面基本反映了金子山测区蛇纹岩的分布特征，代表了岩浆在金子山地区的侵入特征。从图中可以看出，金子山地区的超基性岩体仅为岩浆主通道的北侧的一部分，根部位于金子山地区的西南方向，岩浆主通道的北缘向北陡倾，按照同位产出的规律，金子山地区的含磁铁矿角砾状蛇纹岩为岩浆主通道的分支，推断向南陡倾，结果和时间域激电测深推断的产状一致（图7）。前期施工4个钻孔均未见矿（图8），ZK2501和ZK2502孔为交叉孔，钻孔岩性均为滑镁岩，未见矿原因分析认为矿体控制深度不够，均未穿透滑镁岩，达到含矿岩层。ZKA01和ZK2701孔未见矿，主要原因是未考虑控矿岩层的产状问题，从含矿岩层的背后和侧面穿过。
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图 7 激电测深剖面和磁性体分布关系图Figure 7. Distribution relationship between IP sounding profile and magnetic body![]()
图 8 钻孔和磁性体分布关系图Figure 8. Distribution relationship between boreholes and magnetic body通过对金子山金铜矿资料重新进行综合研究，结合岩浆通道的三维模型，推断在岩浆通道底部或者转折端位置存在与超基性岩有关的岩浆熔离型金铜矿体，施工了ZK2601孔（图8），在岩浆分支通道的底端，标高约
1270 m处见金铜矿体，Au品位5.2×10−6，Cu品位0.11×10−2，厚1.0 m。4. 结论
（1）笔者通过对陕西省略阳县金子山地区磁异常数据进行小波多尺度分解，通过功率谱与磁异常深度对应关系计算出磁源似深度，依靠钻孔数据进行约束反演，借助Voxler平台建立三维磁性体模型，直观的反映了不同异常源对应的地质体和构造信息，提高了磁异常的垂向分辨率，有助于提高对深部异常及矿体赋存位置的认识，提高深部找矿的工作效率。
（2）Voxler平台为磁法三维反演提供了良好的平台，其多个数据模块在实现交互式可视化三维地质建模重构中起到了较好的作用，通过平台的可视化重构，可以直观的预测了岩浆的通道位置，推断了岩浆通道底部或者转折端位置，大致圈定矿体的赋存空间，提高了地球物理勘探解释的准确性、可靠性。
（3）在功率谱计算时引用了有限延深直立矩形棱柱体功率谱公式，仅考虑直立矩形条件下，且将少量钻孔资料信息作为地质建模约束条件，条件过于单一，针对复杂模型还需进一步研究。
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图 1 典型造山带岩浆铜镍硫化物矿床分布图（据李文渊，2007修改）
Figure 1. Distribution of typical orogenic belt magmatic Cu-Ni sulfide deposits
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图 2 典型造山带岩浆铜镍硫化物矿床Sr-Nd同位素组成
数据来源：东天山-北山造山带（尤敏鑫，2022及参考文献）；东昆仑造山带（姜常义等，2015；Peng et al.，2016）；西班牙瓦里斯坎造山带（Casquet et al.，2001）；芬兰斯韦坎尼造山带（Makkonen et al.，2007）；塔里木地幔柱（余星，2009；Zhou et al.，2009；Zhang et al.，2012；Li et al.，2012；王振朝，2019；Wei et al.，2014）；金川铜镍矿（张宗清等，2004；Duan et al.，2016；Tang et al.，2018）；亏损地幔、大陆地壳和俯冲沉积物（Plank et al.，1998；Vervoort et al.，1999；Chauvel et al.，2009）
Figure 2. Sr-Nd isotopic composition of magmatic copper-nickel sulfide deposits in typical orogenic belts
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图 3 造山带铜镍硫化物矿床和典型大火成岩省地幔潜能温度（据Liu et al. 2017修改）
数据来源：东天山-北山造山带（苏本勋, 2011; Mao et al., 2014; 徐刚, 2013; 阮班晓等, 2020）；东昆仑造山带（李文渊等, 2020）；太古宙科马提岩和大火成岩省（Herzberg et al., 2009; Bizimis and Peslier, 2015; Herzberg, 2016; Liu et al., 2017）；平均MORB（Niu et al., 2011; Ivanov, 2015）。
Figure 3. Mantle potential temperature of Cu-Ni sulfide deposits in orogenic belt and typical large igneous provinces
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图 4 造山带和非造山带铜镍硫化物矿床S同位素组成
数据来源：东天山-北山造山带（尤敏鑫，2022及参考文献）；东昆仑和西班牙瓦里斯坎造山带 （Casquet et al.，2001 ；王冠，2014；姜常义等，2015；Zhang et al.，2017）；非造山带（Lightfoot et al.，1984；Grinenko，1985；Abzalov et al.，1997；Ripley et al.，1999；Barnes et al.，2001；Li et al.，2003；Ripley et al.，2003；Li et al.，2003；Ripley et al.，2005；Ding et al.，2009；Seat et al.，2009；Maier et al.，2010）
Figure 4. S isotopic composition of Cu-Ni sulfide deposits in orogenic and non-orogenic belts
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