Study of ore-forming theoretical innovation and prospecting breakthrough of magmatic copper–nickel–cobalt sulfide deposits in China
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摘要: 中国岩浆铜镍钴硫化物矿床是国家镍、钴、铂族元素等战略性关键金属资源的主要来源,是需要特别关注的具有未来价值的重要矿床类型。该类矿床来源于上地幔,特别是软流圈的部分熔融形成的镁铁质、超镁铁质岩浆,硫化物液相−硅酸盐熔体的不混溶(熔离)作用是成矿的主要机制。它们主要形成于两种背景:大陆裂谷和造山带中的伸展环境。中国是岩浆铜镍钴硫化物矿床的产出大国,但与国外相比,形成背景和成矿动力学机制比较独特。世界上绝大多数岩浆铜镍钴硫化物矿床都形成于古老的克拉通,是地幔柱地球动力作用的结果,太古代—早元古代的科马提岩镍钴硫化物矿床是鲜明的产出特点。中国缺少古老的科马提岩有关的镍钴硫化物矿床,成矿时代相对较晚,主要形成于新元古代、晚古生代早期和晚期三个时期,新元古代以镍金属资源量居世界第三的金川超大型矿床为代表,晚古生代早期以近年来找矿突破发现的夏日哈木超大型矿床为代表。夏日哈木矿床也是迄今世界上特提斯造山带中发现的唯一一例超大型岩浆铜镍钴硫化物矿床。中国学者基于中国找矿实际提出的“大岩浆−深部熔离−贯入”表现为“小岩体成大矿”的成矿理论,广泛为野外地质勘查工作者接受并应用,取得了重要的找矿突破性成果,同时为国外同行认可,改变了岩浆铜镍钴硫化物矿床传统的成矿认识。造山带中岩浆铜镍钴硫化物矿床的广泛分布是中国该类矿床的一个重要特色,按形成造山带演化和成矿历史的不同,可分为特提斯型和中亚型两种重要的类型。特提斯型以夏日哈木矿床为代表,它是特提斯构造转换,原特提斯造山后,古特提斯裂解的产物;中亚型以中亚造山带中东天山−北山、阿尔泰分布的大批晚古生代晚期早二叠世岩浆铜镍钴硫化物矿床为代表,是板块构造和地幔柱双重地球动力学机制作用的结果。中国岩浆铜镍钴硫化物矿床找矿潜力巨大,金川矿床作为水平的“岩床”被推覆至地表呈倾斜的“岩墙”产出的结果,深边部仍具有重要找矿潜力,目前已在含矿岩体两端发现了重要的新矿体;夏日哈木矿床所在的东昆仑及其邻区已发现十余处新的矿床(点)。区域上,塔里木陆块东南缘、塔里木陆块北缘、扬子陆块西缘和华北陆块东北缘是亟待加强勘查的找矿远景区,而扬子陆块北缘、华北陆块北缘是急需调查的找矿新区。
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关键词:
- 岩浆铜镍钴硫化物矿床 /
- 深部熔离作用 /
- 小岩体成大矿 /
- 成矿类型 /
- 找矿潜力
Abstract: Chinese magmatic copper–nickel–cobalt sulfide deposit is the main source of strategic key metal resources, such as nickel, cobalt and platinum group elements in China, and it is an important deposit type with a future value that needs special attention. This type of deposit comes from the mafic and ultramafic magma formed by the upper mantle, especially the asthenosphere, and the immiscible (liquation) action between sulfide liquid–silicate melt is the main mineralization mechanism. They are mainly formed in two geological settings: the continental rift and the extended environment in the orogenic zone. China is a major producer of magmatic copper–nickel–cobalt sulfide deposits, but compared with the world it is relatively unique. Most magmatic copper–nickel–cobalt sulfide deposits in the world are formed in the ancient craton, and are the result of the mantle plume geodynamics. Archeozoic–early Proterozoic komatiite nickel–cobalt sulfide deposits is a distinct metallogenic characteristics. Ancient komatiite-related nickel–cobalt sulfide deposits have been rarely discovered in China, and their mineralization age is relatively late, mainly in the Neoproterozoic, Early and Late Paleozoic. The Neoproterozoic is represented by the Jinchuan super-large deposit with nickel metal reserves ranked the third in the world, and the Early Paleozoic by the Xiarihamu super-large deposit discovered in the prospecting breakthrough of recent years. The Xiarihamu deposit is also the only super-large magmatic copper–nickel–cobalt sulfide deposit found in the Tethys orogenic belt in the world. Mineralization theory of “big magma–deep immiscibility–injection” and “forming big ore deposits in small intrusive rocks” proposed by Chinese scholars based on China’s prospecting practice has been widely accepted and applied by field geological exploration workers, and has made important prospecting breakthrough discoveries. At the same time, it has been recognized by foreign peers, which changed the traditional metallogenic understanding of magma copper–nickel–cobalt sulfide deposits. The extensive distribution of magmatic copper–nickel–cobalt sulfide deposits in orogenic belts is an important feature of such deposits in China. According to the different evolution of orogenic zones and metallogenic history, it can be divided into two important types: Tethys type and Central Asian type. The Tethys type is represented by the Xiarihamu ore deposit, and it is the product of the Tethys structural transformation, which the Paleo-Tethys cracking after the Proto-Tethys orogeny; the Central Asian type is represented by a large number of the early Permian of the Late Palaeozoic magmatic copper–nickel–cobalt sulfide deposits distributed in the Eastern Tianshan–Beishan and Altai zones of the Central Asian Orogenic belt, which is the result of the dual geodynamics mechanism of plate tectonics and mantle plume. China's magmatic copper–nickel–cobalt sulfide deposit has huge prospecting potential, and the Jinchuan deposit as a result of nappe structure from deep horizontal “sill” thrusted to the surface of the inclined “dyke”, it still has significant prospecting potential in its deep and marginal locations, in which important new ore bodies have been found at both ends of the ore-bearing rock body; more than 10 new ore deposits (points) have been found in East Kunlun and its adjacent areas, where the Xiarihamu deposit is located. In the region, the southeastern margin of Tarim Landmass, the northern margin of Tarim Landmass, the western margin of Yangtze Landmass and the northeast margin of North China Landmass are the exploration prospect areas to strengthen prospecting, while the northern margins of Yangzi Landmass and North China land block are the new prospecting areas for urgent investigation. -
图 3 金川含矿超镁铁岩Nb/Yb–Th/Yb图解(据Tang et al.,2013修改)
Figure 3. Nb/Yb–Th/Yb diagram of the Jinchuan ore-bearing ultramafic intrusions (modified from Tang et al., 2013)
图 6 夏日哈木含矿镁铁–超镁铁岩Sr-Nd同位素对比图解(据Zhang et al.,2021修改)
Figure 6. Comparison of the Sr–Nd isotope of the Xiarihamu ore-bearing mafic-ultramafic intrusions(modified from Zhang et al., 2021)
图 7 东昆仑古特提斯裂谷构造–岩浆–成矿事件示意图(据李文渊等,2021修改)
Figure 7. Schematic diagram of the rift formation–magma–metallogenic event of Paleo-Tethys in East Kunlun (modified from Li et al.,2021)
图 8 东天山–北山含矿镁铁–超镁铁质侵入岩分布图(Xiao et al.,2004;Su et al.,2011)
Figure 8. Distribution of ore-bearing mafic-ultramafic intrusions in the Eastern Tianshan–Beishan region(Xiao et al.,2004;Su et al.,2011)
图 9 东天山–北山含铜镍钴镁铁–超镁铁岩Nb/Yb–Th/Yb和Nb/Yb–TiO2/Yb图解(底图据Pearce,2008;数据来自尤敏鑫,2022修改)
a—Nb/Yb–Th/Yb图解;b—Nb/Yb–TiO2/Yb图解
Figure 9. Nb/Yb–Th/Yb diagram and Nb/Yb–TiO2/Yb diagram of ore-bearing mafic-ultramafic intrusions in the Eastern Tianshan–Beishan region(Base map after Pearce,2008; data modified from You,2022)
(a) Nb/Yb–Th/Yb diagram; (b) Nb/Yb–TiO2/Yb diagram
图 10 东天山–北山含铜镍钴镁铁–超镁铁岩Sr-Nd同位素对比图解(据Zhou et al.,2008;尤敏鑫,2022修改)
Figure 10. Comparison of the Sr–Nd isotope of the ore-bearing mafic-ultramafic intrusions from the Eastern Tianshan–Beishan region (modified from Zhou et al., 2008; You, 2022)
表 1 中国岩浆铜镍钴硫化物矿床成矿特征及类型一览表
Table 1. Schedule of mineralization characteristics and types of magmatic Ni–Cu–Co sulfide deposits in China
成矿背景 典型矿床 主要岩石类型 成矿元素 矿床规模 测年方法和成矿时代 文献来源 大
陆
裂
谷
环
境大陆
边缘
裂谷金川 二辉橄榄岩、纯橄榄岩 Ni、Cu、Co、PGE 超大型 SHRIMP锆石U–Pb,827 ± 8 Ma Li et al., 2005b 兴地 辉长岩、二辉岩、二辉橄榄岩 Ni、Cu 小型 锆石U–Pb,760 ± 6 Ma Zhang et al., 2011 大坡岭 变辉橄岩、变辉石岩、辉长辉绿岩 Ni、Cu、Co、PGE 小型 SHRIMP锆石U–Pb,828 ± 7 Ma 葛文春等,2001 周庵 二辉橄榄岩、橄榄辉石岩 Ni、Cu、PGE 大型 锆石U–Pb,641.5 ± 3.7 Ma 闫海卿等,2010 桃科 变橄榄辉长苏长岩、变辉长苏长岩 Ni、Cu、PGE 小型 锆石U–Pb,2715 ± 16 Ma 孙涛等,2016 铜硐子 蚀变辉长-辉绿岩 Ni、Cu 小型 元古代? 赤柏松 辉长辉绿岩、二辉橄榄岩 Ni、Cu、Co、PGE 小型 SHRIMP锆石U–Pb,134 ± 7 Ma 裴福萍等,2005 大火
成岩
省力马河 单辉橄榄岩、辉长-闪长岩 Ni、Cu 小型 SHRIMP锆石U–Pb,263 ±3 Ma Zhou et al., 2008 白马寨 橄榄岩、橄辉岩、辉石岩、辉长岩 Ni、Cu、Co、PGE 小型 SHRIMP锆石U–Pb,258.5 ± 3.5 Ma Wang,2006 金宝山 蚀变单辉橄榄岩、辉长辉绿岩 PGE、Ni、Cu、Co 大型 SHRIMP锆石U–Pb,260.6 ± 3.5 Ma Tao et al., 2015 杨柳坪 二辉橄榄岩、辉石岩、辉长岩 PGE、Ni、Cu 大型 晚二叠纪? 造
山
带
伸
展
环
境特提
斯造
山带夏日哈木 二辉岩、辉长岩、橄榄岩 Ni、Cu、Co 超大型 锆石U–Pb,411.6 ± 2.4 Ma Li et al., 2015 拉水峡 蚀变橄榄岩 Ni、Cu、Co、PGE 小型 ? 煎茶岭 蛇纹岩、滑镁岩、菱镁岩 Ni、Co 大型 硫化物Re–Os等时线,878 ± 27 Ma 王瑞廷等,2003 中亚
造山
带黄山东 角闪橄榄辉长岩、辉长橄榄岩 Ni、Cu、Co、PGE 大型 SHRIMP锆石U–Pb,274 ± 3 Ma 韩宝福等,2004 图拉尔根 角闪橄榄岩、辉石岩、辉长岩 Ni、Cu、Co、PGE 大型 SHRIMP锆石U–Pb,300.5 ± 3.2 Ma 三金柱等,2010 坡一 角闪辉长岩、橄榄辉石岩 Ni、Cu 大型 TIMS锆石U–Pb,274 ± 4 Ma 秦克章等,2007 菁布拉克 闪长岩、橄榄辉长岩、橄榄岩 Ni、Cu 小型 SHRIMP锆石U–Pb,434.4 ± 6.2 Ma 张作衡等,2007 黑山 斜长角闪橄榄岩、辉长岩 Ni、Cu 大型 SHRIMP锆石U–Pb,356.4 ± 0.6 Ma Xie et al., 2012 小南山 蚀变辉长岩 Ni、Cu、Co、PGE 小型 锆石U–Pb,272.7 ± 2.9 Ma 党智财,2015 喀拉通克型 方辉橄榄岩、辉长苏长岩 Ni、Cu、PGE 大型 SHRIMP锆石U–Pb,287 ± 5 Ma 韩宝福等,2004 红旗岭型 斜方辉石岩、橄榄岩、辉长岩 Ni、Cu、Co 大型 SHRIMP锆石U–Pb,239.6 ± 2.6 Ma 郝立波等,2013 五星 辉长岩、辉石岩、橄榄辉石岩 Ni、Cu、Co、PGE 小型 SHRIMP锆石U–Pb,37.79 ± 0.76 Ma 李光辉等,2010 表 2 玄武质岩浆R和N因子估算与Co的丰度值
Table 2. The Co concentration and calculated R and N factors for basaltic magmas
Xisil Disil R/N Yisul(Co,×10−6) 44 68 1 87/87 44 68 10 422/447 44 68 50 1293/1579 44 68 100 1799/2315 44 68 1000 2804/2992 44 68 10000 2972/2992 (Williams-Jones and Vasyukova,2022) 表 3 地球不同圈层中的PGE丰度(10−9)
Table 3. The PGE concentration in different layers of the earth(10−9)
位置 Pt Pd Os Ir Ru Rh ∑PGE 地核 13 5.5 8 2.6 16 3 48.1 下地幔 0.2 0.12 0.05 0.05 0.1 0.02 0.54 上地幔 0.2 0.09 0.05 0.05 0.1 0.02 0.51 地壳 0.045 0.01 0.001 0.001 0.001 0.001 0.059 (据黎彤,1976;Mcdonough and Sun,1995修改) -
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