新疆西天山查岗诺尔和智博火山岩型铁矿矿床地质特征与成因研究
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摘要
新疆西天山阿吾拉勒成矿带位于伊犁地块北缘，隶属于博罗科努-伊犁成矿区。近年来，随着多个亿吨级铁矿陆续发现而使该成矿带成为地质学界研究的热点。雾嶺-查岗诺尔-智博-敦德-备战铁矿位于同一构造岩浆带上，含矿围岩均为下石炭统火山岩，所以，这五个铁矿床构成了一条铁矿带。本文选择查岗诺尔铁矿和智博铁矿为重点研究对象，以矿区火山岩岩石学、岩相学、岩石地球化学、同位素年代学以及同位素地球化学研究为基础，通过对矿床地质特征、矿相学、矿床地球化学等方面的系统研究，探讨矿区火山岩岩石成因，矿床形成的大地构造背景、铁矿床母岩浆性质以及矿床成因类型。在此基础上，总结本区铁矿床成矿作用及其规律，建立该区铁矿床成矿模式。
查岗诺尔铁矿和智博铁矿位于西天山伊犁地块东北缘博罗科努山系主脊线上，属中天山北缘活动陆缘带。二者受同一个面积为314km2的破火山口控制。岩石学、岩石地球化学表明，这一地区的火山岩主要为下石炭统大哈拉军山组，少部分属上石炭统伊什基里克组。查岗诺尔矿区广泛出露的石炭纪火山岩由玄武岩、粗面玄武岩、玄武质粗面安山岩、粗面安山岩、粗面岩、流纹岩和火山碎屑岩组成，安山质岩石的数量明显多于其他岩石类型。智博铁矿区的主要火山岩岩石类型为玄武岩、玄武质粗面安山岩和粗面安山岩，还有少量的英安岩和流纹岩。两个矿区绝大部分火山岩的岩石化学组成属于钾玄岩系列和高钾钙碱性系列，少数玄武岩和安山岩属于钙碱性和低钾拉斑玄武岩系列。它们相对富集轻稀土元素和大离子亲石元素（Rb、Ba、Th和U），相对亏损高场强元素（Nb、Ta和Ti），具有活动陆缘型火山岩的亲和性。查岗诺尔铁矿区流纹岩LA-ICP-MS锆石U-Pb谐和年龄（321±1.4Ma）表明，该套火山岩形成于早石炭世末期北天山大洋型岩石圈向伊犁地块之下俯冲的活动陆缘带。尽管由消减板片脱水作用或部分熔融形成的流体或熔体反复交代地幔楔而导致玄武岩的Sr同位素组成变化大且多呈富集型，但玄武岩εNd(t)>0，仍可证明其源区在被交代前处于亏损状态的地幔楔。在莫霍面附近的岛弧型地壳根部，聚集的幔源岩浆和与其混杂的原有陆壳物质被以后贯入或穿过其上升的幔源岩浆加热发生部分熔融产生安山质岩浆。流纹岩的岩浆源区应该位于岛弧型下部地壳，主要由原有陆壳物质和幔源岩浆混合形成。
查岗诺尔铁矿区矿体产状受火山穹窿构造制约。该铁矿成矿期可划分为矿浆期和热液期，隐爆作用伴随成矿全过程。矿浆成矿期形成了浮渣状、斑点状、致密块状、贯入角砾状和阴影状等矿石；热液成矿期形成了对称条带状、复角砾状及网脉状等矿石。矿石的稀土元素和微量元素总体特征和安山岩一致。矿石和安山岩的Pb同位素数据在Pb同位素比值图上共线。大量薄片观察表明，安山质火山岩中普遍含有数量不等的磁铁矿，且磁铁矿只出现在安山岩中。这些特征均表明了矿石和安山岩的亲和性。矿石的氧同位素数据范围和典型岩浆型矿床一致。该矿床属于以安山质岩浆为母岩浆的矿（岩）浆矿床（主要）和热液矿床（次要）的复合型矿床。智博铁矿赋矿围岩主要为大哈拉军山组玄武质岩石。铁矿成矿期可划分为矿浆期和热液期。矿浆期形成隐爆角砾状、致密块状、浸染状、海绵陨铁状、斑杂状和条带状矿石，热液成矿期形成网脉状矿石。矿石的稀土元素和微量元素总体特征和玄武岩一致，且矿石和玄武岩的Pb同位素数据在Pb同位素比值图上共线。大量的薄片观察表明，在浸染状矿石中，原生硅酸盐矿物为单斜辉石和斜长石。智博铁矿同样以岩浆阶段的成矿作用为主，晚期叠加有高温火山热液阶段的成矿作用，成因类型亦属以玄武质岩浆为母岩浆的岩浆矿床为主的矿（岩）浆-热液复合型矿床。
基于上述研究，本文建立本区铁矿床成矿模式如下：俯冲板片脱水并交代俯冲带上方的地幔楔，继而使地幔楔的橄榄岩部分熔融，形成富铁的玄武质岩浆。岛弧型地壳根部由于受幔源岩浆活动影响而部分熔融生成富铁的安山岩质岩浆。经深大断裂上侵的岩浆，沿火山口中心部位及锥状向心断裂喷溢形成火山岩。由于岩浆分异及不混溶作用而形成矿浆或富含矿浆的岩浆。这些富铁的岩浆和矿浆沿同一通道上侵，在破火山口中心部位及锥状向心断裂带产生隐爆成矿作用。由于大量岩浆、矿浆喷发，岩浆房处于高温、负压状态，雨水、地下水向负压带汇聚并与火山热液混合。因而矿浆成矿期形成的矿体又受到后期热液叠加矿化，并在其周围形成强烈的面型蚀变。成矿作用结束后，矿体受区域构造控制。
Western Tianshan is one of the most famous metallogenetic belt in China with lots oftypes of mineral deposits. Awulale Metallogenetic Belt (AMB) belongs to the metallogenicprovince of Bonuokenu-Yili, which is located in the northern corner of the Yili block in theWestern Tianshan Mountains (NW-China). The metallogenic belt has become a hot spot ofresearch on geological field because of discovery and exploration of several iron deposits inhundred million ton. These iron deposits including the Wuling Fe, the Chagangnuoer Fe-Cu,Zhibo Fe and Dunde Fe-Pb-Zn deposits are situated at the same tectonic magmatic zone.They are all hosted in Carboniferous volcanic and volcanoclastic rocks and so they composea Fe metallogenetic belt. Research of the paper focused on the Chagangnuoer and Zhibo irondeposits, with the study of volcanic petrology, petrography, petrochemistry, isotopicchronology and isotopic geochemistry. After study of the mineragraphy, geological featuresof iron deposits and geochemistry, we will further discuss the key issues, such as thepetrogenesis of volcanic rocks, the type of mother magma of iron ore, the tectonic setting ofiron deposits, the source of minerals and the genetic types of iron deposit. On this basis, wewill summarize mineralization and regularity of iron ore formation in this area, and thenestablish the model for iron ore formation.
Region of Chagangnuoer and Zhibo iron deposit, which are situated at Bonuokenumountains in northeast part of the Yili block in western Tianshan, belongs to activecontinental margin in northern corner of central Tianshan. Both of them are controlled by thesame caldera whose area is314km2. Petrology and petrochemistry indicated that most ofvolcanic and volcanoclastic rocks in this region belong to Dahalajunshan Formation and alittle of them belong to Yishijilike Formation. Carboniferous volcanic rocks are exposedwidely in region of Chagannur iron deposit, such as basalt, andesite, trachyte, rhyolite andvolcaniclastic rocks. The number of andesite is significantly more than other type volcanicrocks. Region of Zhibo iron deposit is mainly composed of basalt, basaltic trachyte andesite,a little dacite and rhyolite. Most of volcanic rocks of these region belong to high-Kcalc-alkaline and shoshonite series, whereas a few basalt and andesite belong to calc-alkalineand low-K tholeiitic basalt. They are enriched in LREE and LILE (Rb, Ba, Th, U) with obvious depletions of Nb, Ta and Ti. It suggests that they have a blood relation withvolcanic-arc rocks. LA-ICP-MS ziron U-Pb dating of rhyolite suggests an isotopic age of321.2±2.3Ma, which indicates that they are created by the subduction of ocean lithosphereof north Tianshan Ocean toward south beneath the Yili block. Fluids or melts derived fromthe dehydration or partial melting of subducted slab likely reacted with mantle wedgeperidotite, and the reaction leads to the variable and enriched Sr isotopic composition ofbasalt. However, Nd isotopic composition of basalt (εNd(t)<0) suggests that basaltic magmashould be generated from a depleted mantle before interaction. Magma derived form mantleintruded into crustal rocks, and then these magma became mafic migmatites. Later magmasderived from mantle would intrude into or pass through these migmatites. So the partialmelting of migmatites would generate andesitic magma by this way. Rhyolitic magma sourceshould be located in the underpart of lower crustal of continental arc, and it was generatedfrom partial melting of crustal rocks with lots of magam derived from mantle.
The attitude of ore body in Chagangnuoer is restricted to volcanic fornix. Wall rocks,mainly consisting of andesite and andesitic volcaniclastic rock, belong to the Dahalajunshanformation. The deposit was formed during magma ore-forming period and hydrothermalmetallogenic period, with the former being dominant and cyptoexplosion in wholemetallogenic period. There are some kinds of ore formed during magma ore-forming period,such as scum ore, speckles ore, block ore, injection and breccia ore and shadow ore. Thereare many ore formed in hydrothermal metallogenic period, such as symmetrical banding ore,multi-breccia ore and netted vein-like ore. Ore and andesite are almost same in REEfractionations patterns and trace elements fractionations patterns. Pb isotopic ratios of ore andandesite are liner correlation in Pb isotopic ratios graph. Microscopic fabric indicates thatthere are varying amounts of magnetite in andesitic volcanic rocks and magnetite appearedonly in andesite. It indicates that they have a blood relation with volcanic rocks and ore.Furthermore, range of oxygen isotopic dates of ore is keeping up with these of typicalmagmatic deposits. Hence, this deposit is a polygenetic ore magmatic deposit(predominant)and hydrothermal deposit(subordinate), with the andesitic magma as primary magma. The orebody in Zhibo iron deposit is hosted in basaltic rocks of the Dahalajunshan formation.Metallogenic period includes magma ore-forming period and hydrothermal metallogenic period. Some kinds of ore, including cryptoexplosive breccia ore, block ore, impregnated ore,sideronitique ore, taxitic ore and banding ore, formed during magma ore-forming period; andnetted vein-like ore formed in hydrothermal metallogenic period. Ore and basalt are verysimilar in REE fractionations patterns and trace elements fractionations patterns. Numerousmicrographs suggest that the protogenic silicate minerals are clinopyxene and plagioclase inimpregnated ore. Magmatic metallogenesis dominated in whole metallogenic period, and thisore body forming during magma period underwent complex metasomatism which formed inhydrothermal metallogenic period. Consequently, this deposit is a polygenetic ore magmaticdeposit(predominant) and hydrothermal deposit(subordinate), with the basltic magma asprimary magma.
Based on the above study, a model for iron metallogenesis in this area is suggested asfollow: Fluids or melts derived from the subducted slab likely reacted with mantle wedgeperidotites, and the reaction led to mantle wedge peridotite partial melting. Partial melting ofmantle wedge peridotite formed iron-rich basaltic magma. The underneath rocks of lowercrustal of continental arc partial melted because of activity of magma derived from mantle,and these melt mass formed Iron-rich andesitic magma. These magma upward invadedthrough deep fault and the volcanic rocks formed with the eruption and overflow of magmaalong the central part of crater or pyramidal centripetal fault. Ore magma or ore-rich magmaformed due to the magmatic differentiation and immiscibility effect. These Ore magma orore-rich magma upward invaded through volcanic vent and had cryptoexplosion along thecentral part of crater or pyramidal centripetal fault. After eruption of magma or ore magma,condition of the magma chamber became high temperature and negative pressure. As a resultof this, rainwater and groundwater gathered around the negative pressure area, and then theymixed volcanic hydrothermal water. In a word, the ore body forming during magma periodunderwent complex metasomatism in hydrothermal metallogenic period, and there were lotsof area metasomatism around ore body. Ore body were restricted by regional tectonic activity.
查岗诺尔铁矿和智博铁矿位于西天山伊犁地块东北缘博罗科努山系主脊线上，属中天山北缘活动陆缘带。二者受同一个面积为314km2的破火山口控制。岩石学、岩石地球化学表明，这一地区的火山岩主要为下石炭统大哈拉军山组，少部分属上石炭统伊什基里克组。查岗诺尔矿区广泛出露的石炭纪火山岩由玄武岩、粗面玄武岩、玄武质粗面安山岩、粗面安山岩、粗面岩、流纹岩和火山碎屑岩组成，安山质岩石的数量明显多于其他岩石类型。智博铁矿区的主要火山岩岩石类型为玄武岩、玄武质粗面安山岩和粗面安山岩，还有少量的英安岩和流纹岩。两个矿区绝大部分火山岩的岩石化学组成属于钾玄岩系列和高钾钙碱性系列，少数玄武岩和安山岩属于钙碱性和低钾拉斑玄武岩系列。它们相对富集轻稀土元素和大离子亲石元素（Rb、Ba、Th和U），相对亏损高场强元素（Nb、Ta和Ti），具有活动陆缘型火山岩的亲和性。查岗诺尔铁矿区流纹岩LA-ICP-MS锆石U-Pb谐和年龄（321±1.4Ma）表明，该套火山岩形成于早石炭世末期北天山大洋型岩石圈向伊犁地块之下俯冲的活动陆缘带。尽管由消减板片脱水作用或部分熔融形成的流体或熔体反复交代地幔楔而导致玄武岩的Sr同位素组成变化大且多呈富集型，但玄武岩εNd(t)>0，仍可证明其源区在被交代前处于亏损状态的地幔楔。在莫霍面附近的岛弧型地壳根部，聚集的幔源岩浆和与其混杂的原有陆壳物质被以后贯入或穿过其上升的幔源岩浆加热发生部分熔融产生安山质岩浆。流纹岩的岩浆源区应该位于岛弧型下部地壳，主要由原有陆壳物质和幔源岩浆混合形成。
查岗诺尔铁矿区矿体产状受火山穹窿构造制约。该铁矿成矿期可划分为矿浆期和热液期，隐爆作用伴随成矿全过程。矿浆成矿期形成了浮渣状、斑点状、致密块状、贯入角砾状和阴影状等矿石；热液成矿期形成了对称条带状、复角砾状及网脉状等矿石。矿石的稀土元素和微量元素总体特征和安山岩一致。矿石和安山岩的Pb同位素数据在Pb同位素比值图上共线。大量薄片观察表明，安山质火山岩中普遍含有数量不等的磁铁矿，且磁铁矿只出现在安山岩中。这些特征均表明了矿石和安山岩的亲和性。矿石的氧同位素数据范围和典型岩浆型矿床一致。该矿床属于以安山质岩浆为母岩浆的矿（岩）浆矿床（主要）和热液矿床（次要）的复合型矿床。智博铁矿赋矿围岩主要为大哈拉军山组玄武质岩石。铁矿成矿期可划分为矿浆期和热液期。矿浆期形成隐爆角砾状、致密块状、浸染状、海绵陨铁状、斑杂状和条带状矿石，热液成矿期形成网脉状矿石。矿石的稀土元素和微量元素总体特征和玄武岩一致，且矿石和玄武岩的Pb同位素数据在Pb同位素比值图上共线。大量的薄片观察表明，在浸染状矿石中，原生硅酸盐矿物为单斜辉石和斜长石。智博铁矿同样以岩浆阶段的成矿作用为主，晚期叠加有高温火山热液阶段的成矿作用，成因类型亦属以玄武质岩浆为母岩浆的岩浆矿床为主的矿（岩）浆-热液复合型矿床。
基于上述研究，本文建立本区铁矿床成矿模式如下：俯冲板片脱水并交代俯冲带上方的地幔楔，继而使地幔楔的橄榄岩部分熔融，形成富铁的玄武质岩浆。岛弧型地壳根部由于受幔源岩浆活动影响而部分熔融生成富铁的安山岩质岩浆。经深大断裂上侵的岩浆，沿火山口中心部位及锥状向心断裂喷溢形成火山岩。由于岩浆分异及不混溶作用而形成矿浆或富含矿浆的岩浆。这些富铁的岩浆和矿浆沿同一通道上侵，在破火山口中心部位及锥状向心断裂带产生隐爆成矿作用。由于大量岩浆、矿浆喷发，岩浆房处于高温、负压状态，雨水、地下水向负压带汇聚并与火山热液混合。因而矿浆成矿期形成的矿体又受到后期热液叠加矿化，并在其周围形成强烈的面型蚀变。成矿作用结束后，矿体受区域构造控制。
Western Tianshan is one of the most famous metallogenetic belt in China with lots oftypes of mineral deposits. Awulale Metallogenetic Belt (AMB) belongs to the metallogenicprovince of Bonuokenu-Yili, which is located in the northern corner of the Yili block in theWestern Tianshan Mountains (NW-China). The metallogenic belt has become a hot spot ofresearch on geological field because of discovery and exploration of several iron deposits inhundred million ton. These iron deposits including the Wuling Fe, the Chagangnuoer Fe-Cu,Zhibo Fe and Dunde Fe-Pb-Zn deposits are situated at the same tectonic magmatic zone.They are all hosted in Carboniferous volcanic and volcanoclastic rocks and so they composea Fe metallogenetic belt. Research of the paper focused on the Chagangnuoer and Zhibo irondeposits, with the study of volcanic petrology, petrography, petrochemistry, isotopicchronology and isotopic geochemistry. After study of the mineragraphy, geological featuresof iron deposits and geochemistry, we will further discuss the key issues, such as thepetrogenesis of volcanic rocks, the type of mother magma of iron ore, the tectonic setting ofiron deposits, the source of minerals and the genetic types of iron deposit. On this basis, wewill summarize mineralization and regularity of iron ore formation in this area, and thenestablish the model for iron ore formation.
Region of Chagangnuoer and Zhibo iron deposit, which are situated at Bonuokenumountains in northeast part of the Yili block in western Tianshan, belongs to activecontinental margin in northern corner of central Tianshan. Both of them are controlled by thesame caldera whose area is314km2. Petrology and petrochemistry indicated that most ofvolcanic and volcanoclastic rocks in this region belong to Dahalajunshan Formation and alittle of them belong to Yishijilike Formation. Carboniferous volcanic rocks are exposedwidely in region of Chagannur iron deposit, such as basalt, andesite, trachyte, rhyolite andvolcaniclastic rocks. The number of andesite is significantly more than other type volcanicrocks. Region of Zhibo iron deposit is mainly composed of basalt, basaltic trachyte andesite,a little dacite and rhyolite. Most of volcanic rocks of these region belong to high-Kcalc-alkaline and shoshonite series, whereas a few basalt and andesite belong to calc-alkalineand low-K tholeiitic basalt. They are enriched in LREE and LILE (Rb, Ba, Th, U) with obvious depletions of Nb, Ta and Ti. It suggests that they have a blood relation withvolcanic-arc rocks. LA-ICP-MS ziron U-Pb dating of rhyolite suggests an isotopic age of321.2±2.3Ma, which indicates that they are created by the subduction of ocean lithosphereof north Tianshan Ocean toward south beneath the Yili block. Fluids or melts derived fromthe dehydration or partial melting of subducted slab likely reacted with mantle wedgeperidotite, and the reaction leads to the variable and enriched Sr isotopic composition ofbasalt. However, Nd isotopic composition of basalt (εNd(t)<0) suggests that basaltic magmashould be generated from a depleted mantle before interaction. Magma derived form mantleintruded into crustal rocks, and then these magma became mafic migmatites. Later magmasderived from mantle would intrude into or pass through these migmatites. So the partialmelting of migmatites would generate andesitic magma by this way. Rhyolitic magma sourceshould be located in the underpart of lower crustal of continental arc, and it was generatedfrom partial melting of crustal rocks with lots of magam derived from mantle.
The attitude of ore body in Chagangnuoer is restricted to volcanic fornix. Wall rocks,mainly consisting of andesite and andesitic volcaniclastic rock, belong to the Dahalajunshanformation. The deposit was formed during magma ore-forming period and hydrothermalmetallogenic period, with the former being dominant and cyptoexplosion in wholemetallogenic period. There are some kinds of ore formed during magma ore-forming period,such as scum ore, speckles ore, block ore, injection and breccia ore and shadow ore. Thereare many ore formed in hydrothermal metallogenic period, such as symmetrical banding ore,multi-breccia ore and netted vein-like ore. Ore and andesite are almost same in REEfractionations patterns and trace elements fractionations patterns. Pb isotopic ratios of ore andandesite are liner correlation in Pb isotopic ratios graph. Microscopic fabric indicates thatthere are varying amounts of magnetite in andesitic volcanic rocks and magnetite appearedonly in andesite. It indicates that they have a blood relation with volcanic rocks and ore.Furthermore, range of oxygen isotopic dates of ore is keeping up with these of typicalmagmatic deposits. Hence, this deposit is a polygenetic ore magmatic deposit(predominant)and hydrothermal deposit(subordinate), with the andesitic magma as primary magma. The orebody in Zhibo iron deposit is hosted in basaltic rocks of the Dahalajunshan formation.Metallogenic period includes magma ore-forming period and hydrothermal metallogenic period. Some kinds of ore, including cryptoexplosive breccia ore, block ore, impregnated ore,sideronitique ore, taxitic ore and banding ore, formed during magma ore-forming period; andnetted vein-like ore formed in hydrothermal metallogenic period. Ore and basalt are verysimilar in REE fractionations patterns and trace elements fractionations patterns. Numerousmicrographs suggest that the protogenic silicate minerals are clinopyxene and plagioclase inimpregnated ore. Magmatic metallogenesis dominated in whole metallogenic period, and thisore body forming during magma period underwent complex metasomatism which formed inhydrothermal metallogenic period. Consequently, this deposit is a polygenetic ore magmaticdeposit(predominant) and hydrothermal deposit(subordinate), with the basltic magma asprimary magma.
Based on the above study, a model for iron metallogenesis in this area is suggested asfollow: Fluids or melts derived from the subducted slab likely reacted with mantle wedgeperidotites, and the reaction led to mantle wedge peridotite partial melting. Partial melting ofmantle wedge peridotite formed iron-rich basaltic magma. The underneath rocks of lowercrustal of continental arc partial melted because of activity of magma derived from mantle,and these melt mass formed Iron-rich andesitic magma. These magma upward invadedthrough deep fault and the volcanic rocks formed with the eruption and overflow of magmaalong the central part of crater or pyramidal centripetal fault. Ore magma or ore-rich magmaformed due to the magmatic differentiation and immiscibility effect. These Ore magma orore-rich magma upward invaded through volcanic vent and had cryptoexplosion along thecentral part of crater or pyramidal centripetal fault. After eruption of magma or ore magma,condition of the magma chamber became high temperature and negative pressure. As a resultof this, rainwater and groundwater gathered around the negative pressure area, and then theymixed volcanic hydrothermal water. In a word, the ore body forming during magma periodunderwent complex metasomatism in hydrothermal metallogenic period, and there were lotsof area metasomatism around ore body. Ore body were restricted by regional tectonic activity.
引文
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