Genetic type, formation age and tectonic setting of the Waitoushan banded iron formation, Benxi, Liaoning Province
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摘要:
辽宁鞍本地区位于华北克拉通东北缘，分布有诸多大型-特大型条带状铁矿床。本文对该区歪头山铁矿进行了岩石学、矿物学及年代学研究。歪头山铁建造以条带状铁矿石为主，兼含有少量的块状矿石，其顶底板围岩及矿体夹层主要为太古界鞍山群斜长角闪岩。元素地球化学分析表明，铁矿石富集重稀土[(La/Yb)PAAS=0.24~0.33]，具La正异常(La/La*=1.43~1.61)、Eu正异常(Eu/Eu*=2.40~4.54) 及Y正异常(Y/Y*=1.10~1.30)，Y/Ho值平均30.59，Sr/Ba值平均17.62，Ti/V值平均19.45，反映成矿物质可能来源于由海底火山活动带来的高温热液与海水的混合溶液。铁矿石无明显Ce负异常(Ce/Ce*=0.92~1.06)，暗示BIF沉积时海水处于缺氧环境。除Fe2O3T与SiO2外，铁矿石中其它氧化物含量均非常低，且贫Th、U、Zr等具有陆源性质的元素，表明大陆碎屑物质对BIF贡献极少。斜长角闪岩稀土元素配分型式近于平坦[(La/Yb)N=0.80~1.10]，无明显Ce异常(Ce/Ce*=0.95~0.99) 与Eu异常(Eu/Eu*=0.88~1.16)；其大离子亲石元素富集，高场强元素无明显亏损。地球化学分析表明，斜长角闪岩原岩可能为产于弧后盆地的玄武质火山岩。锆石形态与微量元素分析显示，斜长角闪岩中的锆石均属岩浆成因。SIMS锆石U-Pb定年显示斜长角闪岩原岩形成于2533±11Ma，代表了歪头山BIF的成矿年龄；在玄武质岩浆喷发过程中，还捕获了一组年龄为2610±5Ma的锆石。电子探针分析显示磁铁矿成分纯净(FeOT=92.04%~93.05%)，其标型组分特征暗示歪头山BIF属沉积变质型铁矿。综合分析认为，歪头山铁矿属Algoma型BIF，成矿与弧后盆地岩浆活动密切相关，指示了新太古代末华北克拉通普遍发育的一期BIF成矿事件。
Abstract:Anshan-Benxi area in Liaoning Province, where plenty of large-superlarge banded iron formations are distributed, is located at the northeastern part of the North China craton. Petrology, mineralogy and geochronology of the Waitoushan iron deposit in Anshan-Benxi area are studied in this paper. Iron ores in the Waitoushan deposit are predominantly banded, with a scrap of massive. The Archean amphibolites in the Anshan Group were developed as main wall rocks and interlayer among the orebodies. Geochemical analyses show the iron ores are enriched in HREE [(La/Yb)PAAS=0.24~0.33], and characterized by positive La anomaly (La/La*=1.43~1.61), positive Eu anomaly (Eu/Eu*=2.40~4.54) and positive Y anomaly (Y/Y*=1.10~1.30) with Y/Ho=30.59, Sr/Ba=17.62, Ti/V=19.45, indicating the ore-forming materials were derived from the intermixture of high temperature hydrotherm and seawater. There is no distinct negative Ce anomaly (Ce/Ce*=0.92~1.06), imlying the seawater was under anoxic condition during the deposition of the Waitoushan BIF. Apart from Fe2O3T and SiO2, the contents of other oxides are rather low, with depletion in continental origin elements (such as Tu, U, Zr), implying the continental detrital materials contributed little to the metallogenic process of the Waitoushan BIF. The chondrite-normalized REE pattern of amphibolites is flat [(La/Yb)N=0.80~1.10] with no distinct Ce anomalies (Ce/Ce*=0.95~0.99) and Eu anomalies (Eu/Eu*=0.88~1.16), while the N-MORB-normalized trace element pattern shows enrichment in LILE without pronounced depletion in HFSE. Geochemical analyses show the protolith of amphibolites was probably basic volcanics originating in back-arc basin setting. Morphology and trace element analyses of zircon grains indicate the zircons selected from amphibolites were all magmatic. SIMS zircon U-Pb dating shows the protolith of amphibolites was formed at 2533±11Ma, standing for the formation age of the Waitoushan iron deposit. During the eruption of basaltic magma, a group of zircons with the age of 2610±5Ma were captured. Electron microprobe analysis shows the composition of magnetites is pure and single (FeOT=92.04%~93.05%), and the typomorphic studies indicate the Waitoushan deposit is attached to metamorphosed sedimentary iron deposit. To sum up, we propose the Waitoushan deposit belongs to the Algoma-type BIF, showing an affinity with the magmation in back-arc basin setting and representing a Neoarehean metallogenic event of BIF widely developed in the North China craton.
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Key words:
- Banded iron formation /
- Amphibolite /
- Neoarehean /
- Back-arc basin basalt /
- Waitoushan iron deposit /
- Anshan-Benxi area
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图 1
辽宁鞍本地区条带状铁建造与太古宙地质体分布图(据沈其韩，1998；Wan et al., 2011修改)
Figure 1.
The distribution of banded iron formations and Archean geological bodies in Anshan-Benxi area, Liaoning Province (modified after Shen, 1998; Wan et al., 2011)
图 2
歪头山铁矿地质图(a)、地层柱状图(b) 和剖面图(c) (据冶金工业部鞍山冶金地质勘探公司，1983①；周世泰，1994修改)
Figure 2.
Geological map (a), stratigraphic column (b) and stratigraphic section (c) of the Waitoushan iron mine (modified after Zhou, 1994)
图 3
歪头山矿区铁矿石与斜长角闪岩野外及镜下特征
Figure 3.
The field and microscopic characteristics of iron ores and amphibolites in the Waitoushan deposit
图 4
铁矿石主量元素含量(a) 和主量元素图解(b, 底图据Lepp and Goldich, 1964; 沈其韩等, 2009)
Figure 4.
Major element contents (a) and major element diagrams (b, the base map after Lepp and Goldich, 1964; Shen et al., 2009) of iron ores
图 5
铁矿石稀土元素PAAS标准化配分图(a, 标准化值据McLennan, 1989) 与微量元素原始地幔标准化蛛网图(b, 标准化值据Sun and McDonough, 1989)
Figure 5.
PAAS-normalized REE (a, normalization values after McLennan, 1989) and primitive-mantle-normalized trace element patterns (b, normalization values after Sun and McDonough, 1989) of iron ores
图 6
斜长角闪岩主微量元素原岩恢复图解(底图分别据Tarney, 1976; Moine and Roche, 1968; 赵振华, 1997; Winchester and Floyd, 1977)
Figure 6.
Major and trace element diagrams for protolith reconstruction of amphibolites (the base map after Tarney, 1976; Moine and Roche, 1968; Zhao, 1997; Winchester and Floyd, 1977 respectively)
图 7
斜长角闪岩稀土元素球粒陨石标准化配分图(a, 标准化值据Taylor and McLennan, 1985) 与微量元素N-MORB标准化蛛网图(b, 标准化值据Sun and McDonough, 1989)
Figure 7.
Chondrite-normalized REE (a, normalization values after Taylor and McLennan, 1985) and N-MORB-normalized trace element patterns (b, normalization values after Sun and McDonough, 1989) of amphibolites
图 8
不同类型铁矿石中的磁铁矿主要成分平均含量蛛网图
Figure 8.
The average content of main constituent in magnetite of different iron ores
图 9
歪头山斜长角闪岩锆石阴极发光图像
Figure 9.
Cathodoluminescence (CL) images of zircons selected from amphibolites in the Waitoushan deposit
图 10
斜长角闪岩锆石207Pb/206Pb年龄明显分为两组(a)、不同年龄组锆石的Th/U比值不同(b) 和斜长角闪岩锆石U-Pb年龄(c)
Figure 10.
Two groups of 207Pb/206Pb age of zircons selected from amphibolites (a), different Th/U ratios of zircons in different age groups (b) and zircon U-Pb age of amphibolites (c)
图 11
斜长角闪岩锆石稀土元素球粒陨石标准化配分图(标准化值据Taylor and McLennan, 1985)
Figure 11.
Chondrite-normalized REE pattern of zircons in amphibolites (normalization values after Taylor and McLennan, 1985)
图 12
华北克拉通与BIF相关岩系形成时代与变质时代直方图
Figure 12.
The histogram of formation and metamorphic ages of rocks associated with BIF in the North China craton
图 13
斜长角闪岩构造环境判别图解(底图分别据Mullen, 1983; Pearce and Cann, 1973; Meschede, 1986; Cabanis and Lecolle, 1989)
Figure 13.
Tectonic discrimination diagrams of amphibolites (the base map after Mullen (1983), Pearce and Cann (1973), Meschede (1986) and Cabanis and Lecolle (1989), respectively)
图 14
Ce异常判别图解(底图据Bau and Dulski, 1996)
Figure 14.
Ce/Ce*-Pr/Pr* discrimination diagram for Ce anomaly (the base map after Bau and Dulski, 1996)
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