红旗岭铜镍硫化物矿床地质地球化学特征及找矿技术方法研究
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摘要
红旗岭矿床是我国的第二大岩浆型铜镍硫化物矿床。本文系统地研究了该矿床的地质特征、镁铁—超镁铁岩体的时空分布规律、成矿岩体的地质地球化学特征和矿床成矿机理，深化了红旗岭铜镍矿床的成岩成矿机理认识；在此基础上，对各种找矿方法的有效性进行了研究，首次系统阐述了同类型矿床的找矿技术流程。
红旗岭铜镍矿床位于兴安—蒙古造山带东部，中朝准地台与天山—兴安地槽区之交汇处。红旗岭矿区内出露的地层主要为下古生界寒武—奥陶系呼兰群变质岩系，茶尖矿区内出露的地层主要为下二叠统寿山沟组碎屑岩系。北东向辉发河深大断裂诱导出的北西向断裂是该矿床的控岩控矿构造，也是主要的导矿和容矿构造。
红旗岭铜镍矿床包括红旗岭和茶尖两个矿区。红旗岭矿区由3个镁铁—超镁铁岩带组成：Ⅰ岩带包括1号、7号、3号、2号和32号等含矿岩体及33号、23号等不含矿岩体，其中多为多岩相岩体；Ⅱ、Ⅲ岩带岩相相对简单，未发现工业矿体，且Ⅱ岩带岩体普遍具有片麻状构造。茶尖矿区由3个岩带组成：西部超镁铁质亚带分布有8号和9号岩体；后水—茶尖—南水镁铁—超镁铁质亚带分布有1号、2号、14号、10号、5号等岩体；和平—齐家—上富太镁铁—超镁铁质亚带分布有3号、6号、7号岩体等。其中含矿性较好的岩体主要有1号、9号和新6号岩体。红旗岭铜镍矿床成矿岩体均形成于印支期。茶尖矿区的成矿岩体年龄略早于红旗岭矿区，显示了成矿岩体形成时代具有由西南至东北逐渐变新的趋势。
成矿岩体的岩相组合主要有3种型式：1号岩体型、7号岩体型和3号岩体型。1号岩体型为辉长岩相+辉岩相+辉石橄榄岩相+橄榄二辉岩相，含矿岩相为橄榄二辉岩相；7号岩体型为二辉岩相+辉石橄榄岩相，两相均为含矿岩相；3号岩体型为辉长岩相+含长角闪辉石岩相+橄榄二辉岩相，含矿岩相主要为含长角闪辉石岩相。红旗岭矿区各岩体橄榄石和斜方辉石均以富镁为特点，橄榄石均为贵橄榄石，斜方辉石En一般在80%以上。成矿岩体单斜辉石主要为顽透辉石、普通辉石和异变普通辉石，化学成分变化大，尤其是单斜辉石Di端元的比例变化最大。成矿岩体角闪石均属于钙质角闪石类，化学成分变化大。
成矿岩体岩石化学成分变化大，表现出岩浆强烈分异的特点。红旗岭1号岩体的镁铁比值（m/f）为2.69～5.99，平均为4.79，Mg~#为73.40～85.89，平均为82.31；7号岩体的镁铁比值（m/f）为1.01～5.03，平均为3.75，Mg~#为50.49～83.84，平均为77.44；3号岩体的镁铁比值（m/f）为0.74～5.11，平均为2.98，Mg~#为42.76～83.84，平均为72.58。成矿岩体总体成分均属于铁质超基性岩。
成矿岩体U、K、Pb含量相对富集以及Nb、Ta含量的相对亏损是本区成矿岩体固有的地球化学特征，与岩浆演化分异无明显关系。Nd稳定同位素显示，成矿岩浆来自亏损地幔。Sr、Os同位素等研究显示成矿岩体均具有明显的地壳物质混染，而成矿岩体中发现的捕获锆石为地壳物质混染提供了直接证据。综合研究表明，岩浆来源应为亏损地幔，并受到明显的地壳物质混染。
稀土元素、铂族元素研究显示，成矿岩体经历了明显的岩浆分离结晶作用。红旗岭1号岩体和3号岩体成矿作用以就地熔离为主，7号岩体以深部熔离为主。分离结晶作用和地壳物质混染是促使硫饱和而发生硫化物熔离成矿的主要机制。成矿后期热液的叠加改造对矿化的再富集有一定的作用，甚至局部（如7号岩体深部）存在富PGE的热液脉状矿体。岩体强烈蚀变以及闪长伟晶岩、石英—硫化物脉等广泛分布是成矿岩体重要的地质标志之一。
根据造岩矿物地质温压计，估算红旗岭成矿岩体橄榄石结晶的开始温度为1400～1500℃，主要成矿岩体二辉石共结温度为1000～1200℃。成矿岩体冷凝固结温度略低于不成矿岩体，与成矿岩体普遍挥发性组分较高有关。成矿岩体的成岩压力为3.7～6.2kb，深度为12.3～20.7km。成矿温度为300℃～500℃，成矿深度与成岩深度相近。
研究表明，与岩浆硫化物矿床有关的镁铁—超镁铁岩群均产出于板块边缘带、槽台边界或造山带中深大断裂旁侧次一级断裂中。矿化较好的镁铁—超镁铁岩群在1:20万水系沉积物中常具有较明显的Ni异常，且Ni/Co高；但对矿化程度较低、岩体规模较小的镁铁—超镁铁岩群Ni、Ni/Co的指示效果不明显。在中比例尺的航磁中，镁铁—超镁铁岩群常位于条带状、线状以及串珠状的负磁异常带中或正负异常的分界处。
镁铁—超镁铁岩体与大比例尺高磁异常、重力高值圈闭以及Ni、Co、Cu组合异常均有较好的对应关系，表明高精度地磁、高精度重力以及土壤地球化学测量是寻找镁铁—超镁铁岩体的有效方法。而岩体的地质地球化学评价是筛选成矿岩体，寻找矿体的最佳途径。瞬变电磁法是铜镍硫化物矿体定位的有效手段，可控源音频大地电磁测深法和地电化学法对铜镍硫化物矿体定位也具有一定的效果。
综合研究提出的岩浆型铜镍硫化物矿床找矿技术流程分为战略选区阶段、岩体定位阶段、岩体评价阶段以及矿体定位4个阶段。战略选区阶段：通过构造背景分析、区域化探异常分析以及航磁异常分析等确定镁铁—超镁铁岩体分布远景区；岩体定位阶段：通过高精度地磁、高精度重力以及土壤地球化学测量圈定镁铁—超镁铁岩体；岩体评价阶段：对镁铁—超镁铁岩体的含矿性进行评价，选出成矿潜力较高的镁铁—超镁铁岩体；矿体定位阶段：采用瞬变电磁法、可控源音频大地电磁测深法和地电化学法联用对深部矿体进行定位。
Hongqiling deposit is a magmatic Cu-Ni sulfide deposit that ranks second in China. Thegeological characteristics of Cu-Ni deposit, temporal and spatial distribution of mafic-ultramafic intrusions and the geological and geochemical characteristics of metallogenicintrusions have been studied systematically in this thesis, to deepen the understanding of itsmetallogenic mechanism. The effectiveness of various prospecting methods is studied and theprospecting technical process for this type Cu-Ni sulfide deposits has been carried out for thefirst time.
Hongqiling Cu-Ni deposit is located in the east of Xing’an-Mongolia Orogenic belt, theintersection of Xing’an geosyncline and Sino Korean paraplatform. The stratum outcroppedare mainly the Cambrian-Ordovician Hulan Group metamorphic rocks of Lower Paleozoic inHongqiling mine field and Shoushangou formation clastic rock series of Lower Permian inChajian mine field. NW-trending faults induced by the NE-trending Huifahe deep fracture arethe rock and ore controlling structures. Meanwhile, they are also the ore leading and hostingstructures of the deposit.
Hongqiling Cu-Ni deposit includes two mine fields, Hongqiling and Chajian. There arethree mafic-ultramafic zones in Hongqiling mine field. Metallogenic intrusions such as No.1,No.7, No.3, No.2and No.32as well as other non ore-bearing intrusions such as No.33andNo.23are located in zone Ⅰ, most of which are multi-lithofacies. The lithofacies of zoneⅡand Ⅲ are relatively simple with no industrial ore-body. Intrusions in zoneⅡcharacterizedby gneissic structures generally. Chajian mine field also comprise three mafic-ultramaficzones. There are No.8and No.9intrusion distributed in western ultramafic sub zone, No.1,No.2, No.14, No.10and No.5intrusion in Houshui-Chajian-Nanshui mafic-ultramafic subzone and No.3, No.6, No.7intrusion in Heping-Qijia-Shangfutai mafic-ultramafic sub zone.Among them, No.1, No.9and new No.6intrusion are metallogenic intrusions. Themetallogenic intrusions in Hongqiling Cu-Ni deposit all formed in Indosinian. The ages ofmetallogenic intrusions in Chajian mine field is slightly older, shows a trend that therock-forming ages of metallogenic intrusions become younger from southwest to northeastgradually.
There are mainly three types of lithofacies association of the metallogenic intrusions:type No.1, No.7and No.3. The lithofacies association of type No.1is gabbro+pyroxenolite+pyroxene+peridotite+olivine-websterite, and ore-bearing lithofacies are lherzolites. Type No.7intrusion includes websterite+pyroxene peridotite, and they are also the ore-bearinglithofacies. No.3intrusion includes gabbro+anorthose-bearing hornblende pyroxenite+olivine-websterite, and the ore-bearing lithofacies are mainly anorthose-bearing hornblendepyroxenites. The olivines and orthopyroxenes are magnesium-rich in all intrusions ofHongqiling mine field. The olivines belong to chrysolite and En of orthopyroxenes isgenerally above80%. Clinopyroxenes in metallogenic intrusions mainly belong to diopside,augite and pigeonite-augite with great variation in chemical composition, especially thevariation of clinopyroxene Di end member. Amphiboles in metallogenic intrusions all belongto calcic amphibole with great variation in chemical composition.
The chemical composition of metallogenic intrusions varies greatly. It shows that thecharacteristic of strong magma differentiation. The ratio (m/f) of No.1intrusion ranges from2.69to5.99with an average of4.79, and Mg~#ranges from73.40to85.89with an average of82.31. No.7intrusion ranges from1.01to5.03with an average of3.75, and Mg~#ranges from50.49to83.84with an average of77.44. The ratio (m/f) of No.3intrusion ranges from0.74to5.11with an average of2.98, and Mg~#ranges from42.76to83.84with an average of72.58.The metallogenic intrusions all belong to iron ultrabasic rocks by constituents.
The enrichment of U, K and Pb and relative loss of Nb, Ta in metallogenic intrusions aretheir intrinsic geochemical characteristics which have no relationship with magma evolutionand differentiation. Stable isotope Nd indicates that the metallogenic magma originated fromdepleted mantle. The research on Sr, Os shows that metallogenic intrusions all have obviouscrustal contamination, and the found of capture zircon in metallogenic intrusions provides adirect evidence for crustal contamination. Comprehensive study shows that the magmaoriginated from depleted mantle and was affected by crustal contamination.
Rare earth elements and PGE characteristics show that metallogenic intrusionsunderwent obvious magmatic fractional crystallization. The mineralization of No.1and No.3intrusions are mainly in-situ liquiation, while No.7intrusion is liquation at deep-level. Strongfractional crystallization and crustal contamination are the main mechanism promoting thesulfur supersaturated and sulfide liquated to mineralize. Superimposition-reformation of thelatter metallogenic stage hydrotherm acts a part in the re-enrichment for mineralization, evenPGE-rich hydrothermal vein-like ore bodies exist (especially in deep No.7intrusion). Theappearance of alteration, diorite pegmatite and products of hydrothermal such as sulfide-quartz are the significant geological signs of metallogenic intrusions.
According to the geological thermobarometer of rock-forming minerals, the calculatedtemperature of crystallization beginning of olivines in metallogenic intrusions is1400℃-1500℃. Eutectic temperature of websterite is1000℃-1200℃. Condensation and console-dation temperature of metallogenic intrusions is slightly lower than that of none-metallogenicintrusions, which is related to high volatile components in metallogenic intrusions. Thediagenetic pressure and depth of the metallogenic intrusions are3.7to6.2kb and12.3to20.7km. The metallogenic temperature is300℃-500℃. The metallogenic depth is consistentwith diagenetic.
The research shows that the mafic-ultramafic rocks related to magmatic sulfide depositsare located in the plate margin, boundary between platform and geosyncline or secondaryfaults of the deep fracture in the orogenic belt. The better mineralized mafic-ultramaficintrusions often have a prominent Ni abnormalities and high Ni/Co in1:200000streamsediment. The indication effect of Ni, Ni/Co is not obvious when the level of mineralization islow or the scale of mafic-ultramafic intrusion is small. In medium-scale aeromagneticprospecting, mafic-ultramafic intrusions are often located in banded, lined and beadednegative magnetic anomaly zones or the boundary between positive and negative anomalies.
Mafic-ultramafic intrusions have good correlations with large-scale high magneticanomalies, the high value gravity traps and Ni, Co, Cu combination anomalies. Thehigh-precision geomagnetism, gravity and geochemical soil survey are effective ways formafic-ultramafic intrusions prospecting. Geological and geochemical evaluation of theintrusions is the best way to screen metallogenic intrusions and find ore bodies. Transientelectromagnetic method is an effective mean for positioning the Cu-Ni sulfide ore bodies,controlled source audio-frequency magnetotellurics and geo-electrochemical method alsopossess certain effects.
Prospecting technology process for magmatic Cu-Ni sulfide deposits can be grouped intofour stages: strategic area selection stage, intrusions positioning stage, intrusions evaluationstage and ore bodies positioning stage. Strategic area selection stage: distribution prospect ofmafic-ultramafic intrusions are determined by tectonic setting, regional geochemicalexploration and aeromagnetic anomalies. Intrusions positioning stage: mafic-ultramaficintrusions are determined by high-precision geomagnetic and gravity measurement and soilgeochemical measurement. Intrusions evaluation stage: ore-bearing potential of mafic-ultramafic intrusions are evaluated by geological and geochemical characteristics. Ore bodiespositioning stage: deep ore bodies are located by means of transient electromagnetic method,controlled source audio-frequency magneto-tellurics and and geo-electrochemical method.
红旗岭铜镍矿床位于兴安—蒙古造山带东部，中朝准地台与天山—兴安地槽区之交汇处。红旗岭矿区内出露的地层主要为下古生界寒武—奥陶系呼兰群变质岩系，茶尖矿区内出露的地层主要为下二叠统寿山沟组碎屑岩系。北东向辉发河深大断裂诱导出的北西向断裂是该矿床的控岩控矿构造，也是主要的导矿和容矿构造。
红旗岭铜镍矿床包括红旗岭和茶尖两个矿区。红旗岭矿区由3个镁铁—超镁铁岩带组成：Ⅰ岩带包括1号、7号、3号、2号和32号等含矿岩体及33号、23号等不含矿岩体，其中多为多岩相岩体；Ⅱ、Ⅲ岩带岩相相对简单，未发现工业矿体，且Ⅱ岩带岩体普遍具有片麻状构造。茶尖矿区由3个岩带组成：西部超镁铁质亚带分布有8号和9号岩体；后水—茶尖—南水镁铁—超镁铁质亚带分布有1号、2号、14号、10号、5号等岩体；和平—齐家—上富太镁铁—超镁铁质亚带分布有3号、6号、7号岩体等。其中含矿性较好的岩体主要有1号、9号和新6号岩体。红旗岭铜镍矿床成矿岩体均形成于印支期。茶尖矿区的成矿岩体年龄略早于红旗岭矿区，显示了成矿岩体形成时代具有由西南至东北逐渐变新的趋势。
成矿岩体的岩相组合主要有3种型式：1号岩体型、7号岩体型和3号岩体型。1号岩体型为辉长岩相+辉岩相+辉石橄榄岩相+橄榄二辉岩相，含矿岩相为橄榄二辉岩相；7号岩体型为二辉岩相+辉石橄榄岩相，两相均为含矿岩相；3号岩体型为辉长岩相+含长角闪辉石岩相+橄榄二辉岩相，含矿岩相主要为含长角闪辉石岩相。红旗岭矿区各岩体橄榄石和斜方辉石均以富镁为特点，橄榄石均为贵橄榄石，斜方辉石En一般在80%以上。成矿岩体单斜辉石主要为顽透辉石、普通辉石和异变普通辉石，化学成分变化大，尤其是单斜辉石Di端元的比例变化最大。成矿岩体角闪石均属于钙质角闪石类，化学成分变化大。
成矿岩体岩石化学成分变化大，表现出岩浆强烈分异的特点。红旗岭1号岩体的镁铁比值（m/f）为2.69～5.99，平均为4.79，Mg~#为73.40～85.89，平均为82.31；7号岩体的镁铁比值（m/f）为1.01～5.03，平均为3.75，Mg~#为50.49～83.84，平均为77.44；3号岩体的镁铁比值（m/f）为0.74～5.11，平均为2.98，Mg~#为42.76～83.84，平均为72.58。成矿岩体总体成分均属于铁质超基性岩。
成矿岩体U、K、Pb含量相对富集以及Nb、Ta含量的相对亏损是本区成矿岩体固有的地球化学特征，与岩浆演化分异无明显关系。Nd稳定同位素显示，成矿岩浆来自亏损地幔。Sr、Os同位素等研究显示成矿岩体均具有明显的地壳物质混染，而成矿岩体中发现的捕获锆石为地壳物质混染提供了直接证据。综合研究表明，岩浆来源应为亏损地幔，并受到明显的地壳物质混染。
稀土元素、铂族元素研究显示，成矿岩体经历了明显的岩浆分离结晶作用。红旗岭1号岩体和3号岩体成矿作用以就地熔离为主，7号岩体以深部熔离为主。分离结晶作用和地壳物质混染是促使硫饱和而发生硫化物熔离成矿的主要机制。成矿后期热液的叠加改造对矿化的再富集有一定的作用，甚至局部（如7号岩体深部）存在富PGE的热液脉状矿体。岩体强烈蚀变以及闪长伟晶岩、石英—硫化物脉等广泛分布是成矿岩体重要的地质标志之一。
根据造岩矿物地质温压计，估算红旗岭成矿岩体橄榄石结晶的开始温度为1400～1500℃，主要成矿岩体二辉石共结温度为1000～1200℃。成矿岩体冷凝固结温度略低于不成矿岩体，与成矿岩体普遍挥发性组分较高有关。成矿岩体的成岩压力为3.7～6.2kb，深度为12.3～20.7km。成矿温度为300℃～500℃，成矿深度与成岩深度相近。
研究表明，与岩浆硫化物矿床有关的镁铁—超镁铁岩群均产出于板块边缘带、槽台边界或造山带中深大断裂旁侧次一级断裂中。矿化较好的镁铁—超镁铁岩群在1:20万水系沉积物中常具有较明显的Ni异常，且Ni/Co高；但对矿化程度较低、岩体规模较小的镁铁—超镁铁岩群Ni、Ni/Co的指示效果不明显。在中比例尺的航磁中，镁铁—超镁铁岩群常位于条带状、线状以及串珠状的负磁异常带中或正负异常的分界处。
镁铁—超镁铁岩体与大比例尺高磁异常、重力高值圈闭以及Ni、Co、Cu组合异常均有较好的对应关系，表明高精度地磁、高精度重力以及土壤地球化学测量是寻找镁铁—超镁铁岩体的有效方法。而岩体的地质地球化学评价是筛选成矿岩体，寻找矿体的最佳途径。瞬变电磁法是铜镍硫化物矿体定位的有效手段，可控源音频大地电磁测深法和地电化学法对铜镍硫化物矿体定位也具有一定的效果。
综合研究提出的岩浆型铜镍硫化物矿床找矿技术流程分为战略选区阶段、岩体定位阶段、岩体评价阶段以及矿体定位4个阶段。战略选区阶段：通过构造背景分析、区域化探异常分析以及航磁异常分析等确定镁铁—超镁铁岩体分布远景区；岩体定位阶段：通过高精度地磁、高精度重力以及土壤地球化学测量圈定镁铁—超镁铁岩体；岩体评价阶段：对镁铁—超镁铁岩体的含矿性进行评价，选出成矿潜力较高的镁铁—超镁铁岩体；矿体定位阶段：采用瞬变电磁法、可控源音频大地电磁测深法和地电化学法联用对深部矿体进行定位。
Hongqiling deposit is a magmatic Cu-Ni sulfide deposit that ranks second in China. Thegeological characteristics of Cu-Ni deposit, temporal and spatial distribution of mafic-ultramafic intrusions and the geological and geochemical characteristics of metallogenicintrusions have been studied systematically in this thesis, to deepen the understanding of itsmetallogenic mechanism. The effectiveness of various prospecting methods is studied and theprospecting technical process for this type Cu-Ni sulfide deposits has been carried out for thefirst time.
Hongqiling Cu-Ni deposit is located in the east of Xing’an-Mongolia Orogenic belt, theintersection of Xing’an geosyncline and Sino Korean paraplatform. The stratum outcroppedare mainly the Cambrian-Ordovician Hulan Group metamorphic rocks of Lower Paleozoic inHongqiling mine field and Shoushangou formation clastic rock series of Lower Permian inChajian mine field. NW-trending faults induced by the NE-trending Huifahe deep fracture arethe rock and ore controlling structures. Meanwhile, they are also the ore leading and hostingstructures of the deposit.
Hongqiling Cu-Ni deposit includes two mine fields, Hongqiling and Chajian. There arethree mafic-ultramafic zones in Hongqiling mine field. Metallogenic intrusions such as No.1,No.7, No.3, No.2and No.32as well as other non ore-bearing intrusions such as No.33andNo.23are located in zone Ⅰ, most of which are multi-lithofacies. The lithofacies of zoneⅡand Ⅲ are relatively simple with no industrial ore-body. Intrusions in zoneⅡcharacterizedby gneissic structures generally. Chajian mine field also comprise three mafic-ultramaficzones. There are No.8and No.9intrusion distributed in western ultramafic sub zone, No.1,No.2, No.14, No.10and No.5intrusion in Houshui-Chajian-Nanshui mafic-ultramafic subzone and No.3, No.6, No.7intrusion in Heping-Qijia-Shangfutai mafic-ultramafic sub zone.Among them, No.1, No.9and new No.6intrusion are metallogenic intrusions. Themetallogenic intrusions in Hongqiling Cu-Ni deposit all formed in Indosinian. The ages ofmetallogenic intrusions in Chajian mine field is slightly older, shows a trend that therock-forming ages of metallogenic intrusions become younger from southwest to northeastgradually.
There are mainly three types of lithofacies association of the metallogenic intrusions:type No.1, No.7and No.3. The lithofacies association of type No.1is gabbro+pyroxenolite+pyroxene+peridotite+olivine-websterite, and ore-bearing lithofacies are lherzolites. Type No.7intrusion includes websterite+pyroxene peridotite, and they are also the ore-bearinglithofacies. No.3intrusion includes gabbro+anorthose-bearing hornblende pyroxenite+olivine-websterite, and the ore-bearing lithofacies are mainly anorthose-bearing hornblendepyroxenites. The olivines and orthopyroxenes are magnesium-rich in all intrusions ofHongqiling mine field. The olivines belong to chrysolite and En of orthopyroxenes isgenerally above80%. Clinopyroxenes in metallogenic intrusions mainly belong to diopside,augite and pigeonite-augite with great variation in chemical composition, especially thevariation of clinopyroxene Di end member. Amphiboles in metallogenic intrusions all belongto calcic amphibole with great variation in chemical composition.
The chemical composition of metallogenic intrusions varies greatly. It shows that thecharacteristic of strong magma differentiation. The ratio (m/f) of No.1intrusion ranges from2.69to5.99with an average of4.79, and Mg~#ranges from73.40to85.89with an average of82.31. No.7intrusion ranges from1.01to5.03with an average of3.75, and Mg~#ranges from50.49to83.84with an average of77.44. The ratio (m/f) of No.3intrusion ranges from0.74to5.11with an average of2.98, and Mg~#ranges from42.76to83.84with an average of72.58.The metallogenic intrusions all belong to iron ultrabasic rocks by constituents.
The enrichment of U, K and Pb and relative loss of Nb, Ta in metallogenic intrusions aretheir intrinsic geochemical characteristics which have no relationship with magma evolutionand differentiation. Stable isotope Nd indicates that the metallogenic magma originated fromdepleted mantle. The research on Sr, Os shows that metallogenic intrusions all have obviouscrustal contamination, and the found of capture zircon in metallogenic intrusions provides adirect evidence for crustal contamination. Comprehensive study shows that the magmaoriginated from depleted mantle and was affected by crustal contamination.
Rare earth elements and PGE characteristics show that metallogenic intrusionsunderwent obvious magmatic fractional crystallization. The mineralization of No.1and No.3intrusions are mainly in-situ liquiation, while No.7intrusion is liquation at deep-level. Strongfractional crystallization and crustal contamination are the main mechanism promoting thesulfur supersaturated and sulfide liquated to mineralize. Superimposition-reformation of thelatter metallogenic stage hydrotherm acts a part in the re-enrichment for mineralization, evenPGE-rich hydrothermal vein-like ore bodies exist (especially in deep No.7intrusion). Theappearance of alteration, diorite pegmatite and products of hydrothermal such as sulfide-quartz are the significant geological signs of metallogenic intrusions.
According to the geological thermobarometer of rock-forming minerals, the calculatedtemperature of crystallization beginning of olivines in metallogenic intrusions is1400℃-1500℃. Eutectic temperature of websterite is1000℃-1200℃. Condensation and console-dation temperature of metallogenic intrusions is slightly lower than that of none-metallogenicintrusions, which is related to high volatile components in metallogenic intrusions. Thediagenetic pressure and depth of the metallogenic intrusions are3.7to6.2kb and12.3to20.7km. The metallogenic temperature is300℃-500℃. The metallogenic depth is consistentwith diagenetic.
The research shows that the mafic-ultramafic rocks related to magmatic sulfide depositsare located in the plate margin, boundary between platform and geosyncline or secondaryfaults of the deep fracture in the orogenic belt. The better mineralized mafic-ultramaficintrusions often have a prominent Ni abnormalities and high Ni/Co in1:200000streamsediment. The indication effect of Ni, Ni/Co is not obvious when the level of mineralization islow or the scale of mafic-ultramafic intrusion is small. In medium-scale aeromagneticprospecting, mafic-ultramafic intrusions are often located in banded, lined and beadednegative magnetic anomaly zones or the boundary between positive and negative anomalies.
Mafic-ultramafic intrusions have good correlations with large-scale high magneticanomalies, the high value gravity traps and Ni, Co, Cu combination anomalies. Thehigh-precision geomagnetism, gravity and geochemical soil survey are effective ways formafic-ultramafic intrusions prospecting. Geological and geochemical evaluation of theintrusions is the best way to screen metallogenic intrusions and find ore bodies. Transientelectromagnetic method is an effective mean for positioning the Cu-Ni sulfide ore bodies,controlled source audio-frequency magnetotellurics and geo-electrochemical method alsopossess certain effects.
Prospecting technology process for magmatic Cu-Ni sulfide deposits can be grouped intofour stages: strategic area selection stage, intrusions positioning stage, intrusions evaluationstage and ore bodies positioning stage. Strategic area selection stage: distribution prospect ofmafic-ultramafic intrusions are determined by tectonic setting, regional geochemicalexploration and aeromagnetic anomalies. Intrusions positioning stage: mafic-ultramaficintrusions are determined by high-precision geomagnetic and gravity measurement and soilgeochemical measurement. Intrusions evaluation stage: ore-bearing potential of mafic-ultramafic intrusions are evaluated by geological and geochemical characteristics. Ore bodiespositioning stage: deep ore bodies are located by means of transient electromagnetic method,controlled source audio-frequency magneto-tellurics and and geo-electrochemical method.
引文
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