西天山智博铁矿石炭纪火山作用与铁成矿研究
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摘要
火山岩型铁矿是重要的铁矿类型之一,也是近年来国内外铁矿研究的热点。火山作用与铁成矿作用之间的联系是认识这类矿床的关键。本论文选择新疆西天山地区新发现的智博火山岩型铁矿为研究对象,围绕火山作用与铁成矿这一主题,对智博铁矿进行综合研究。在系统的野外地质调查基础上,通过矿物学、矿物化学、-磁铁矿LA-ICP-MS原位微量元素分析、全岩地球化学、锆石U-Pb测年、榍石U-Pb测年、流体包裹体测温以及稳定同位素示踪等研究工作,对成矿地质背景、成矿地质特征、火山岩成因、成矿时代、成矿物质来源、矿床成因及成矿模型等科学问题做了较为深入的研究和探讨。同时,结合前人研究资料,论文对成矿带区域火山作用与铁成矿规律进行了初步总结。
智博铁矿赋存于石炭纪火山岩中。矿体以厚板状、似层状、透镜状为主。矿石类型主要有块状矿石、浸染状矿石、条带状矿石以及角砾状矿石。矿石矿物以磁铁矿为主,含少量赤铁矿,硫化物以黄铁矿为主；磁铁矿主要呈板条状、半自形-他形粒状结构。围岩蚀变广泛发育,以Na-Ca质蚀变和K-Ca质蚀变为主,形成透辉石、阳起石、绿帘石、钠长石、钾长石等主要脉石矿物。划分出四阶段矿物共生序列：第一阶段矿物组合以透辉石+钠长石±阳起石+磁铁矿为主；第二阶段矿物组合主要为钾长石+阳起石±绿帘石+磁铁矿；第三阶段蚀变以脉状绿帘石+黄铁矿±磁铁矿为主；第四阶段以石英+方解石+赤铁矿细脉状为主。
智博铁矿的磁铁矿Ti含量较低,亏损热液流体中的惰性元素(如Ti、 Al、Cr, Zr、 Hf、Zn、 Co、 Sc等),富集与岩浆磁铁矿高度不相容的元素(如Si、 Ca、Y等),Ni、 Cr含量呈现解耦现象,Ni/Cr值多大于1,平均为8.6。这些微量元素特征表明磁铁矿主要由富铁的岩浆-热液流体充填交代形成。
智博矿区火山岩为基性-中性-酸性连续系列,以中基性岩为主,主要由玄武岩、玄武安山岩、安山岩、英安岩以及安山质凝灰岩组成。火山岩属钙碱性到高钾钙碱性系列,富集轻稀土元素(LREE)和大离子亲石元素(LILE;如Rb、Th、K),亏损重稀土元素(HREE)和高场强元素(HSFE;如Nb、Ta、Ti),整体表现出俯冲带弧火山岩的地球化学特征。火山岩母岩浆由俯冲带流体交代地幔楔发生部分熔融形成,低程度的混染了上地壳物质。铁成矿形成于于大陆边缘弧环境的局部伸展地带。
利用LA-ICP-MS锆石U-Pb测年技术获得安山岩(12ZB56)和矿化火山岩(12ZB06)的结晶年龄分别为328.7士3.1Ma、329.9士1.5Ma,英安岩(ZB382)和闪长岩(ZB360)的结晶年龄分别为300.3士1.1Ma、305士1.1Ma.三件矿石样品中榍石LA-ICP-MS原位U-Pb年龄分别为310.0±2.1Ma、310.6±2.6Ma.315.2士2.8Ma,表明成矿时代为310-315Ma。智博铁矿与查岗诺尔铁矿成矿时代接近,产于同一火山机构中,属于同一火山-热液成矿事件。年代学数据表明,智博铁矿在石炭纪至少有两期火山-岩浆活动,分别为成矿前中基性火山岩的喷发(330～316Ma)和成矿后中酸性岩浆侵入(307～295Ma),成矿作用发生于晚石炭世(310～315Ma)。
透辉石平衡水的δ18O在4.0～10.0‰之间,表明早期阶段成矿流体以岩浆水为主；阳起石平衡水的δ18O介于9.9～12.6‰,钾长石平衡水的δ18O为7.9～18.9%0,可能与成矿流体和火山岩围岩的同位素再平衡有关；晚期阶段的绿帘石平衡水δ18O值为-1.7～4.2‰,石英平衡水618O值为-3.7～1.4‰,显示有大气水的加入。统计资料显示磁铁矿的δ180值为0.5%0～8.8%0,平均为3.3‰,表明铁质以岩浆来源为主。黄铁矿的δ34S集中于-2.4%0～0.3%o,平均为-0.8%0,具幔源硫特征。绿帘石、石英和方解石均一温度分布莅131～391℃,盐度分布于3.23-22.44wt.%NaCleq.和31.85-37.40wt.%NaCleq.两个区间,表明晚期阶段成矿流体以低温中-高盐度为特征。总体而言,智博矿床的成矿物质主要来源于深部岩浆,与火山岩具有同源的特征。
智博铁矿的形成与区域内石炭纪陆缘弧岩浆-热液活动有关。成矿母岩浆由俯冲流体交代的亏损地幔部分熔融形成,经液态不混溶作用或者低氧逸度下演化分异形成的富铁流体,沿火山通道与断裂向上运移,在火山岩裂隙或层间薄弱带聚集成矿。主成矿阶段以贯入充填成矿为主,形成大量块状富矿石,蚀变不发育,与围岩截然接触,磁铁矿呈板条状、树枝状；中晚期成矿伴有强烈的围岩蚀变,形成浸染状、条带状矿石。角砾状矿石的形成与隐爆作用或者贯入充填成矿作用有关。智博铁矿属于火山岩浆-热液型矿床。
本论文对阿吾拉勒铁成矿带区域成矿规律进行了总结,认为区内火山岩型铁矿存在成因联系,成矿过程具有整体性,受区域火山岩浆-热液作用及火山沉积作用的控制,成矿物质以深部岩浆来源为主。
Voleanogenic iron deposit is an important type of iron deposit, and has recently been the subject of research. The association between volcanisim and Fe mineralization is the key to undertand this ore type. In this contribution, we choose Zhibo iron deposit, a recently discovered voleanogenic iron deposit in the Western Tianshan, as the typical deposit to study. An integrated study of field investigation, mineralogy, mineral chemisty, LA-ICP-MS in situ trace element analysis of magnetite, whole-rock geochemistry, zircon U-Pb dating, titanite U-Pb dating, microthermometric studies of fluid inclusions and stable isotope was carried out to investigate the metallogenic tectonic setting, geological characteristics, the age of mineralization, source of metal, ore genesis and metallogenic model. Combined with previous data, we propose a preliminary metallogenic model of metallogenic belt.
The Zhibo iron deposit is hosted by Carboniferous volcanic and volcaniclastic rocks. Most magnetite orebodies are mainly tabular, stratoid and lenticular in shape. Ore types include massive, disseminated, banded, and brecciated ores. Ore minerals are predominantly magnetite, with traces of hematite. Pyrite is the most common sulfides. Magnetite usually occurs as euhedral-subhedral crystals or as dendritic and platy forms. Associated alteration assemblage is mainly characterized by Na-Ca alteration and K-Ca alteration, which produce various gangue minerals including diopside, albite, actinolite, K-feldspar, and epidote. Four paragenetic stages are recognized:stage I, characterized by albite-diopside-magnetitie assemblages; stage II, represented by widespread actinolite-K-feldspar-magnetitie assemblages; stage III, dominated by epidote-pyrite±magnetite veins; and stage IV, occurring chiefly as hematite-calcite-quartz veins.
Magnetite from Zhibo have low Ti content. Magnetite is depleted in elements that are relatively immobile in hydrothermal fluids (e.g., Ti, Al, Cr, Zr, Hf, Zn, Co, Sc), but is enriched in elements that are highly incompatible into magmatic magnetite (e.g., Si, Ca, Y). In addition, Ni and Cr of magnetite are decoupled and Ni/Cr ratio is high (>1), with an average value of8.6. The trace element characteristics indicated that the ore magnetite was formed by Fe-rich magmatic-hydrothemal fluids.
The volcanic host rocks of Zhibo display a compositional continuum from basalt to rhyolite, dominated by basalt, basaltic andesite, andesite, dacite, and tuffaceous rocks. Geochemical analyses indicate that the volcanic host rocks are mainly of calc-alkaline to high-K calc-alkaline affinity, enriched in LILEs (e.g., Rb, K) and LREEs, and depleted in HFSEs (e.g., Nb, Ta, Ti) and HREEs, supporting a subduction origin for the volcanic rocks. The most likely origin of the parent magma is partial melting of a mantle wedge that had been fertilized by fluids released from subducted slab. The parental magma was slightly contaminated by crust during ascent. The iron mineralization were suggested to have formed in extensional zones of continental arc-setting.
LA-ICP-MS U-Pb dating of igneous zircon from an andesite (12ZB56) and a mineralized lava (12ZB06) yielded crystallization ages of328.7±2.1Ma and329.9±1.5Ma, respectively. A dacite (ZB382) and a diorite (ZB360) have been dated at300.3±1.1Ma and305±1.1Ma, respectively. In situ LA-ICP-MS U-Pb dating of hydrothermal titanite in thin sections of three ore sapmle yielded ages of310.0±2.1Ma,310.6±2.6Ma,315.2±2.8Ma, considered to represent the age of mineralization (310--315Ma). Iron mineralization at Zhibo and Chagangnuoer have formed more-or-less coevally in a single metallogenic episode generated by magmatic-hydrothermal activity within the same volcano. Geochronological data indicated that there were at least two episodes of volcanism at Zhibo, i.e. pre-mineralization volcanism (ca.330-316Ma) and post-mineralization magmatic intrusions (ca.307-295Ma). The timing of mineralization at Zhibo was bracketed between310Ma and315Ma.
Stable isotope compositions of pyroxene indicate a magmatic source for early mineralization stages:calculated δ18O composition of fluids in equilibrium with pyroxene ranging between4.0and10.0%o. Calculated δ18O composition of fluids in equilibrium with actinolite (9.9-12.6%o) and K-feldspar (7.9-18.9%o), probably resulted from the isotope reequilibration between Fe-rich fluids with host rocks. Calculated δ18O composition of fluids in equilibrium with epidote (-1.7-4.2%o) and quartz (-3.7-1.4%o) may indicate ingress of meteoric fluids in the late stage alteration. We show that magnetites from Zhibo have δ18O values between0.5and8.8%o, with an average value of3.3%o, indicative of magmatic origin. The δ18O values for pyrite from Zhibo vary from-2.4to0.3%o, with an average value of-0.8%o, consistent with a deep-seated sulfur source. Homogenization temperatures of epidote, quartz and calcite are between131℃and391℃with salinities of3.23-22.44wt.%NaCleq.and31.85-37.40wt.%NaCleq., indicate an involvement of low-T and medium to high-salinity chloride fluids in the late stage alteration. Taken together, fluid inclusion and stable isotope data suggest that iron is predominantly magmatic in origin, sharing common parental magma with volcanic host rocks.
Fe mineralzation at Zhibo was attributed to the regional magmatic-hydrothemal during Carboniferous. The most likely origin of the ore-related magma is partial melting of a mantle wedge that had been fertilized by fluids released from subducted slab. Fe-rich melts may be separated from the parent magma by liquid immiscibility or differentiation in low oxygen fugacity. Fe-rich melts were then channeled along major faults and fractures within a volcano into the volcanic hostr rocks, forming iron ores. The intrusive of Fe-rich melts is the dominant mineralization style, whieh formed massive ores, with little alteration, having sharp contacts with host rock, and dendritic or platy forms of magnetite. The banded and disseminated ores resulted from the metasomatic reaction between Fe-rich fluids with host rocks. The brecciated ore can plausibly be interpreted as resulting from an explosion of Fe-rich melt, caused by a sudden release of volatiles in response to decreasing pressure during ascent to near-surface levels. The Zhibo ore is typical of volcanogenic iron deposit formed in a volcanic magmatic-hydrothermal system.
Combined with previous data, we propose a preliminary metallogenic model of Awulale iron metallogenetic belt (ATMB) and suggest that iron deposit within AIMB are relevant ores that formed in a single metallogenic episode. Fe mineralizaion was controlled by volcanic-hydrothermal and volcanism-sedimentation. The metal source was magmatic in origin.
智博铁矿赋存于石炭纪火山岩中。矿体以厚板状、似层状、透镜状为主。矿石类型主要有块状矿石、浸染状矿石、条带状矿石以及角砾状矿石。矿石矿物以磁铁矿为主,含少量赤铁矿,硫化物以黄铁矿为主；磁铁矿主要呈板条状、半自形-他形粒状结构。围岩蚀变广泛发育,以Na-Ca质蚀变和K-Ca质蚀变为主,形成透辉石、阳起石、绿帘石、钠长石、钾长石等主要脉石矿物。划分出四阶段矿物共生序列：第一阶段矿物组合以透辉石+钠长石±阳起石+磁铁矿为主；第二阶段矿物组合主要为钾长石+阳起石±绿帘石+磁铁矿；第三阶段蚀变以脉状绿帘石+黄铁矿±磁铁矿为主；第四阶段以石英+方解石+赤铁矿细脉状为主。
智博铁矿的磁铁矿Ti含量较低,亏损热液流体中的惰性元素(如Ti、 Al、Cr, Zr、 Hf、Zn、 Co、 Sc等),富集与岩浆磁铁矿高度不相容的元素(如Si、 Ca、Y等),Ni、 Cr含量呈现解耦现象,Ni/Cr值多大于1,平均为8.6。这些微量元素特征表明磁铁矿主要由富铁的岩浆-热液流体充填交代形成。
智博矿区火山岩为基性-中性-酸性连续系列,以中基性岩为主,主要由玄武岩、玄武安山岩、安山岩、英安岩以及安山质凝灰岩组成。火山岩属钙碱性到高钾钙碱性系列,富集轻稀土元素(LREE)和大离子亲石元素(LILE;如Rb、Th、K),亏损重稀土元素(HREE)和高场强元素(HSFE;如Nb、Ta、Ti),整体表现出俯冲带弧火山岩的地球化学特征。火山岩母岩浆由俯冲带流体交代地幔楔发生部分熔融形成,低程度的混染了上地壳物质。铁成矿形成于于大陆边缘弧环境的局部伸展地带。
利用LA-ICP-MS锆石U-Pb测年技术获得安山岩(12ZB56)和矿化火山岩(12ZB06)的结晶年龄分别为328.7士3.1Ma、329.9士1.5Ma,英安岩(ZB382)和闪长岩(ZB360)的结晶年龄分别为300.3士1.1Ma、305士1.1Ma.三件矿石样品中榍石LA-ICP-MS原位U-Pb年龄分别为310.0±2.1Ma、310.6±2.6Ma.315.2士2.8Ma,表明成矿时代为310-315Ma。智博铁矿与查岗诺尔铁矿成矿时代接近,产于同一火山机构中,属于同一火山-热液成矿事件。年代学数据表明,智博铁矿在石炭纪至少有两期火山-岩浆活动,分别为成矿前中基性火山岩的喷发(330～316Ma)和成矿后中酸性岩浆侵入(307～295Ma),成矿作用发生于晚石炭世(310～315Ma)。
透辉石平衡水的δ18O在4.0～10.0‰之间,表明早期阶段成矿流体以岩浆水为主；阳起石平衡水的δ18O介于9.9～12.6‰,钾长石平衡水的δ18O为7.9～18.9%0,可能与成矿流体和火山岩围岩的同位素再平衡有关；晚期阶段的绿帘石平衡水δ18O值为-1.7～4.2‰,石英平衡水618O值为-3.7～1.4‰,显示有大气水的加入。统计资料显示磁铁矿的δ180值为0.5%0～8.8%0,平均为3.3‰,表明铁质以岩浆来源为主。黄铁矿的δ34S集中于-2.4%0～0.3%o,平均为-0.8%0,具幔源硫特征。绿帘石、石英和方解石均一温度分布莅131～391℃,盐度分布于3.23-22.44wt.%NaCleq.和31.85-37.40wt.%NaCleq.两个区间,表明晚期阶段成矿流体以低温中-高盐度为特征。总体而言,智博矿床的成矿物质主要来源于深部岩浆,与火山岩具有同源的特征。
智博铁矿的形成与区域内石炭纪陆缘弧岩浆-热液活动有关。成矿母岩浆由俯冲流体交代的亏损地幔部分熔融形成,经液态不混溶作用或者低氧逸度下演化分异形成的富铁流体,沿火山通道与断裂向上运移,在火山岩裂隙或层间薄弱带聚集成矿。主成矿阶段以贯入充填成矿为主,形成大量块状富矿石,蚀变不发育,与围岩截然接触,磁铁矿呈板条状、树枝状；中晚期成矿伴有强烈的围岩蚀变,形成浸染状、条带状矿石。角砾状矿石的形成与隐爆作用或者贯入充填成矿作用有关。智博铁矿属于火山岩浆-热液型矿床。
本论文对阿吾拉勒铁成矿带区域成矿规律进行了总结,认为区内火山岩型铁矿存在成因联系,成矿过程具有整体性,受区域火山岩浆-热液作用及火山沉积作用的控制,成矿物质以深部岩浆来源为主。
Voleanogenic iron deposit is an important type of iron deposit, and has recently been the subject of research. The association between volcanisim and Fe mineralization is the key to undertand this ore type. In this contribution, we choose Zhibo iron deposit, a recently discovered voleanogenic iron deposit in the Western Tianshan, as the typical deposit to study. An integrated study of field investigation, mineralogy, mineral chemisty, LA-ICP-MS in situ trace element analysis of magnetite, whole-rock geochemistry, zircon U-Pb dating, titanite U-Pb dating, microthermometric studies of fluid inclusions and stable isotope was carried out to investigate the metallogenic tectonic setting, geological characteristics, the age of mineralization, source of metal, ore genesis and metallogenic model. Combined with previous data, we propose a preliminary metallogenic model of metallogenic belt.
The Zhibo iron deposit is hosted by Carboniferous volcanic and volcaniclastic rocks. Most magnetite orebodies are mainly tabular, stratoid and lenticular in shape. Ore types include massive, disseminated, banded, and brecciated ores. Ore minerals are predominantly magnetite, with traces of hematite. Pyrite is the most common sulfides. Magnetite usually occurs as euhedral-subhedral crystals or as dendritic and platy forms. Associated alteration assemblage is mainly characterized by Na-Ca alteration and K-Ca alteration, which produce various gangue minerals including diopside, albite, actinolite, K-feldspar, and epidote. Four paragenetic stages are recognized:stage I, characterized by albite-diopside-magnetitie assemblages; stage II, represented by widespread actinolite-K-feldspar-magnetitie assemblages; stage III, dominated by epidote-pyrite±magnetite veins; and stage IV, occurring chiefly as hematite-calcite-quartz veins.
Magnetite from Zhibo have low Ti content. Magnetite is depleted in elements that are relatively immobile in hydrothermal fluids (e.g., Ti, Al, Cr, Zr, Hf, Zn, Co, Sc), but is enriched in elements that are highly incompatible into magmatic magnetite (e.g., Si, Ca, Y). In addition, Ni and Cr of magnetite are decoupled and Ni/Cr ratio is high (>1), with an average value of8.6. The trace element characteristics indicated that the ore magnetite was formed by Fe-rich magmatic-hydrothemal fluids.
The volcanic host rocks of Zhibo display a compositional continuum from basalt to rhyolite, dominated by basalt, basaltic andesite, andesite, dacite, and tuffaceous rocks. Geochemical analyses indicate that the volcanic host rocks are mainly of calc-alkaline to high-K calc-alkaline affinity, enriched in LILEs (e.g., Rb, K) and LREEs, and depleted in HFSEs (e.g., Nb, Ta, Ti) and HREEs, supporting a subduction origin for the volcanic rocks. The most likely origin of the parent magma is partial melting of a mantle wedge that had been fertilized by fluids released from subducted slab. The parental magma was slightly contaminated by crust during ascent. The iron mineralization were suggested to have formed in extensional zones of continental arc-setting.
LA-ICP-MS U-Pb dating of igneous zircon from an andesite (12ZB56) and a mineralized lava (12ZB06) yielded crystallization ages of328.7±2.1Ma and329.9±1.5Ma, respectively. A dacite (ZB382) and a diorite (ZB360) have been dated at300.3±1.1Ma and305±1.1Ma, respectively. In situ LA-ICP-MS U-Pb dating of hydrothermal titanite in thin sections of three ore sapmle yielded ages of310.0±2.1Ma,310.6±2.6Ma,315.2±2.8Ma, considered to represent the age of mineralization (310--315Ma). Iron mineralization at Zhibo and Chagangnuoer have formed more-or-less coevally in a single metallogenic episode generated by magmatic-hydrothermal activity within the same volcano. Geochronological data indicated that there were at least two episodes of volcanism at Zhibo, i.e. pre-mineralization volcanism (ca.330-316Ma) and post-mineralization magmatic intrusions (ca.307-295Ma). The timing of mineralization at Zhibo was bracketed between310Ma and315Ma.
Stable isotope compositions of pyroxene indicate a magmatic source for early mineralization stages:calculated δ18O composition of fluids in equilibrium with pyroxene ranging between4.0and10.0%o. Calculated δ18O composition of fluids in equilibrium with actinolite (9.9-12.6%o) and K-feldspar (7.9-18.9%o), probably resulted from the isotope reequilibration between Fe-rich fluids with host rocks. Calculated δ18O composition of fluids in equilibrium with epidote (-1.7-4.2%o) and quartz (-3.7-1.4%o) may indicate ingress of meteoric fluids in the late stage alteration. We show that magnetites from Zhibo have δ18O values between0.5and8.8%o, with an average value of3.3%o, indicative of magmatic origin. The δ18O values for pyrite from Zhibo vary from-2.4to0.3%o, with an average value of-0.8%o, consistent with a deep-seated sulfur source. Homogenization temperatures of epidote, quartz and calcite are between131℃and391℃with salinities of3.23-22.44wt.%NaCleq.and31.85-37.40wt.%NaCleq., indicate an involvement of low-T and medium to high-salinity chloride fluids in the late stage alteration. Taken together, fluid inclusion and stable isotope data suggest that iron is predominantly magmatic in origin, sharing common parental magma with volcanic host rocks.
Fe mineralzation at Zhibo was attributed to the regional magmatic-hydrothemal during Carboniferous. The most likely origin of the ore-related magma is partial melting of a mantle wedge that had been fertilized by fluids released from subducted slab. Fe-rich melts may be separated from the parent magma by liquid immiscibility or differentiation in low oxygen fugacity. Fe-rich melts were then channeled along major faults and fractures within a volcano into the volcanic hostr rocks, forming iron ores. The intrusive of Fe-rich melts is the dominant mineralization style, whieh formed massive ores, with little alteration, having sharp contacts with host rock, and dendritic or platy forms of magnetite. The banded and disseminated ores resulted from the metasomatic reaction between Fe-rich fluids with host rocks. The brecciated ore can plausibly be interpreted as resulting from an explosion of Fe-rich melt, caused by a sudden release of volatiles in response to decreasing pressure during ascent to near-surface levels. The Zhibo ore is typical of volcanogenic iron deposit formed in a volcanic magmatic-hydrothermal system.
Combined with previous data, we propose a preliminary metallogenic model of Awulale iron metallogenetic belt (ATMB) and suggest that iron deposit within AIMB are relevant ores that formed in a single metallogenic episode. Fe mineralizaion was controlled by volcanic-hydrothermal and volcanism-sedimentation. The metal source was magmatic in origin.
引文
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