西準噶爾寶貝金礦區(qū)小巖株鋯石U-Pb年代學及其對成礦的時代制約

王樂民，段豐浩，紀征寶，王冉，趙得龍，郭鑫，程萬里

(1.新疆維吾爾自治區(qū)國土資源廳,新疆 烏魯木齊 830002；2.長安大學地球科學與資源學院，陜西 西安 710054；3.新疆地質(zhì)礦產(chǎn)勘查開發(fā)局第七地質(zhì)大隊，新疆 烏蘇 833000)

西準噶爾寶貝金礦區(qū)小巖株鋯石U-Pb年代學及其對成礦的時代制約

王樂民1，段豐浩2，紀征寶3，王冉2，趙得龍2，郭鑫2，程萬里2

(1.新疆維吾爾自治區(qū)國土資源廳,新疆 烏魯木齊 830002；2.長安大學地球科學與資源學院，陜西 西安 710054；3.新疆地質(zhì)礦產(chǎn)勘查開發(fā)局第七地質(zhì)大隊，新疆 烏蘇 833000)

寶貝金礦區(qū)出露面積較小的二長花崗巖體，其對該區(qū)金礦的成礦作用貢獻如何是重要的地質(zhì)問題。為此，筆者進行了該巖體的年代學工作。為區(qū)域金礦的成礦時代提供精確的同位素年代學約束。該礦床硫化物組合單一，主要為黃銅礦。筆者選擇了1件樣品，進行LA-ICPMS鋯石U-Pb法定年。結(jié)果10個測點給出的等時線年齡為(300.3±8.6)Ma。這表明該區(qū)Au的成礦作用有可能是由該區(qū)晚石炭世—早二疊世的大規(guī)模巖漿活動來提供物質(zhì)來源和熱動力條件等，具有十分重要的成礦意義。

寶貝金礦；LA-ICP-MS鋯石U-Pb定年；區(qū)域成礦；西準噶爾

西準噶爾地區(qū)已發(fā)現(xiàn)較多的金礦床，尤其在達爾布特斷裂帶北側(cè)較為集中。該帶晚古生代巖漿活動強烈，火山巖和侵入巖廣布，峰期為石炭紀—早二疊世(韓寶福等，2006, 蘇玉平等，2006, Tang, et al., 2010, Yin, et al., 2010, 魏少妮等，2011, 尹繼元等，2011)。該帶Cu-Mo-W-Be等成礦元素組合好，異常有一定規(guī)模分布(陳宣華等，2015)，西準噶爾地區(qū)發(fā)育還原性斑巖銅礦和石英脈型-斑巖型鎢鉬礦，具有Cu-Au-Mo-W組合(Shen, et al., 2013)。前人對該區(qū)金礦和巖漿活動的關(guān)系有一定認識。從成巖時代上看，堿性花崗巖類時代集中在308～296Ma之間(蘇玉平，2006, 韓寶福，2006, Geng, et al., 2009, 馮乾文等，2012)。對于鈣堿性的中酸性小巖體而言，包古圖一帶小巖體的年代學資料較多，主要集中在313～319Ma之間(張連昌等，2006, 宋會俠，2007, 宋會俠等，2007, Song, et al., 2007, 鄭波等，2009, Liu, et al., 2009, Shen, et al., 2009, 魏少妮等，2010, Shen, et al., 2010, Shen, et al., 2010, Tang, et al., 2010, 魏少妮，2011, Shen, et al., 2012, Tang, et al., 2012, Shen, et al., 2013, 鄭波等，2014)。統(tǒng)計意義上看，區(qū)域上與Cu-Mo的成礦可能與鈣堿性系列的中酸性小巖體有關(guān)，尤其是斑巖型礦床(點)(張連昌，2006, Liu, et al., 2009, Tang, 2010, 李永軍等，2012, Wang, et al., 2013, 鄢瑜宏等，2014, 鄢瑜宏等，2015, 申萍等，2015)。

然而，區(qū)域金礦的成礦地質(zhì)背景尚需進一步探討，缺乏與區(qū)域巖漿活動關(guān)系的探討(陳衍景，1996)。寶貝金礦是其中一個較大金礦，該礦床與區(qū)域巖漿活動有何關(guān)系也未得到深入的研究。要解決這一問題，年代學工作十分必要。筆者為此而展開礦區(qū)二長花崗巖的鋯石U-Pb法定年工作，探討礦區(qū)巖漿活動的時代。這為金礦的形成背景提供了重要年代學制約。

1 區(qū)域地質(zhì)

西準噶爾構(gòu)造帶位于中亞造山帶西南部，是中亞古生代俯沖-增生復合造山帶的主要組成部分(Feng, et al., 1989, 肖序常等，1992, 何國琦，2004, 李錦軼等，2006, Xiao, et al., 2009, 李錦軼等，2009, Wilhem, et al., 2012, Choulet, et al., 2013, Zhu, et al., 2013)，發(fā)育多條蛇綠(混雜)巖帶(Zhang, et al., 2011, Yang, et al., 2013, Zhu, 2013)和大量中酸性侵入巖(圖1)。NE向的達爾布特斷裂帶兩側(cè)侵入巖尤其發(fā)育，包括夏爾莆(克拉瑪依)、紅山、鐵廠溝、阿克巴斯陶等大巖基以及包古圖、別魯阿嘎希、玉依塔勒盆克提等小巖體(金成偉等，1993)，構(gòu)成了著名的達爾布特構(gòu)造巖漿帶和具有找礦潛力的巖漿成礦帶(李永軍，2012)。該帶地層主要為泥盆紀—石炭紀陸源碎屑巖-火山碎屑巖建造，見有火山巖夾層，火山巖時代為(328.1±1.8)Ma～(357.5±5.4)Ma(王瑞等，2007, 安芳等，2009, 佟麗莉等，2009)。

寶貝一帶的二長花崗巖體侵入于早石炭世地層中(圖2)。斷層發(fā)育，礦化體賦存于巖體圍巖中，部分為石英脈型礦化，石英脈和斷層帶中礦化特征明顯。該巖體出露面積有限，地表顯示為啞鈴狀。位于西準噶爾的寶貝金礦主要由石英脈型礦石組成，主要含金礦物為銀金礦，以裂隙金和包裹金的形式賦存在毒砂、黃鐵礦和石英中(王瑞，2007)。

2 樣品和分析方法

用于鋯石LA-ICP-MS U-Pb測年的樣品采自巖體近中心，樣品編號BBRZ-1。采樣位置利用GPS定位，經(jīng)緯度為：45°54'17.87"北，84°38'35.17"東，海拔為961m(圖2)。

樣品巖性為淺肉紅色細粒二長花崗巖，未見包體。巖體周圍見有大量含金石英脈。巖石由斜長石、鉀長石、石英組成，含少量黑云母。斜長石約占40%：呈半自形板狀，粒徑0.2～1.0mm，可見聚片雙晶，輕度絹云母化、泥化。鉀長石約占30%：他形粒狀，粒徑0.3～1.4mm，具條紋結(jié)構(gòu)，為條紋長石，輕度泥化。石英約占30%：他形粒狀，粒徑0.2～1.6mm，波狀消光，分布不均勻。黑云母少量：片狀，片徑0.1～0.4mm，黃-褐色。磁鐵礦微量：粒狀，粒徑0.1～0.2mm。

JFS.加甫薩爾蘇;XEP.夏爾莆;BGT.包古圖;HS.紅山;TCG.鐵廠溝;HT.哈圖;AKB.阿克巴斯套;MEG.廟爾溝;TEG.塔爾根;DLNL.多拉那勒;YGZ.也格孜卡拉;HGLL.洪古勒楞;N.TC.塔城北;TST.托斯特;KWSY.孔吾薩伊;KSB.卡桑布拉克;KYTS.闊依塔斯;KEJ.卡爾交;KLMS.庫魯木蘇;SLK.賽力克;TLG.托洛蓋;AL.寶貝金礦區(qū);BL.別魯阿嘎希;YY.玉依塔勒盆克提;HLZ.黃梁子;GETS.加爾塔斯;LB.拉巴;DLH.都倫河東;TS.塔斯闊臘; BE.布爾科斯臺;KZ.克孜勒巴斯陶;JW.吉烏爾沙克;AL.阿拉散布拉克;K1.克I巖體;K2.克II巖 體;HSD.紅山東巖體;SETH.薩爾托海巖株;BB.寶貝二長花崗巖體圖1 西準噶爾地質(zhì)簡圖及Au、Cu、Mo礦點(化)(改自新疆維吾爾自治區(qū)地質(zhì)礦產(chǎn)局, 1993，ChenJ, et al., 2010,ChenJ, et al., 2014)Fig.1 Geological map of the West Junggar region with the location of Au-Cu-Mo deposit occurrences (Modified from XJBGME, 1993;Chen J, et al., 2010; Chen J, et al., 2014)

鋯石分選在廊坊誠信地質(zhì)服務有限公司完成，樣品重量約5kg。樣品人工破碎并使用可清洗分選設備淘洗和富集重礦物，后以磁選和電磁選獲非電磁性礦物，再行淘洗富集鋯石，最后在雙目鏡下手工挑選鋯石。

將待測鋯石以環(huán)氧樹脂固定，拋光至暴露出鋯石中心面，用反射光、透射光照相。然后用體積百分比為3%的HNO3清洗樣品并鍍碳，進行陰極發(fā)光(CL)照相。照相之后用3%的HNO3清洗靶標的表面。

激光剝蝕電感耦合等離子體質(zhì)譜(LA-ICP-MS)原位U-Pb 定年在西北大學大陸動力學國家重點實驗室完成。實驗采用的ICPMS 為美國Agilent 公司生產(chǎn)的Agilent 7500 a，激光剝蝕系統(tǒng)為德國MicroLas公司生產(chǎn)的GeoLas 200 M，該系統(tǒng)由德國Lambda Physik 公司的ComPex102 ArF 準分子激光器(波長193 nm)與MicroLas 公司的光學系統(tǒng)組成。激光剝蝕束斑直徑約為30μm，激光剝蝕樣品的深度為20～40 μm。詳細分析步驟和數(shù)據(jù)處理方法參見參考文獻(Yuan, et al., 2008)。用LA-ICP-MS Common Lead Correction(v. 3.15)對其進行了普通鉛校正(Andersen, 2002)，使用Isoplot軟件計算U-Pb年齡(Ludwig, et al., 1991)。

圖2 (a)寶貝金礦一帶二長花崗巖鋯石U-Pb諧和圖和(b)年齡直方圖及代表性鋯石的 陰極發(fā)光圖像(小插圖)Fig.2 (a) LA-ICPMS U-Pb Concordia plots and (b)statistical histograms of U-Pb dating for zircons from the Baobei pluton. The insert picture showing representatives of Cathodoluminescence image of zircons from monzonitic granite in Baobei area.

3 分析結(jié)果

本次自未有明顯蝕變的樣品BBRZ1中獲得的鋯石為棱柱狀，CL圖像顯示其為典型的巖漿鋯石(圖2中小插圖)，具有明顯的環(huán)帶狀結(jié)構(gòu)。鋯石U-Pb分析結(jié)果列于表1，其中17個測點由于206Pb/238U和207Pb/235U年齡不諧和(圖2b)，為離群點，沒有參與計算。RZ-23、24兩個測點年齡偏老，沒有參與計算。這類誤差較大的數(shù)據(jù)表面年齡集中在晚石炭世至早二疊世，有可能遭受了熱液的改造造成U-Pb體系的破壞以及Pb的丟失。

其余有效測點年齡數(shù)據(jù)總計10個，206Pb/238U加權(quán)平均年齡為(300.3±8.6)Ma(2σ)(圖2b)，代表了巖漿結(jié)晶的時代。該年齡十分接近于紅山等A2型花崗巖體(韓寶福，2006, 蘇玉平，2006)，而明顯晚于包古圖一帶的小巖體(Tang, 2010)。

4 討論與結(jié)論

4.1 成巖成礦時代

區(qū)域重要礦點的成礦年代學已有數(shù)據(jù)積累。宏遠斑巖體輝鉬礦的Re-Os等時線年齡為 294.6±4.6 Ma之間(Wang, 2013)，但也有(314.3±1.9)Ma(鄢瑜宏，2014)的可能。包古圖一帶的輝鉬礦的Re-Os 年齡將成礦年齡限定在(310±6.4)～(316 ±6.4)Ma(宋會俠，2007, 申萍等，2010)。該巖體侵入于早石炭世地層中，也證實其是在晚石炭世之后侵位的。銅礦脈空間上賦存于夏爾浦巖體靠北的花崗閃長巖中。該巖體的時代也有較多鋯石U-Pb年代學數(shù)據(jù)，其中的花崗巖體、輝綠巖脈和花崗巖脈時限為301～321Ma(Kwon, et al., 1989, 韓寶福，2006, 賀敬博等，2011)。本研究的結(jié)果(300.3±8.6)Ma與之非常接近而略晚，表明成礦流體可能來自于巖漿熱液或者成礦熱源來自巖漿。

按照前人對該區(qū)成礦區(qū)帶規(guī)律的研究，區(qū)內(nèi)的金等礦床主要就位于晚石炭世—二疊紀,集中分布在碰撞造山作用較強烈的地帶,礦床形成于碰撞作用的擠壓-伸展轉(zhuǎn)變期(陳衍景，1996)。

4.2 寶貝金礦與區(qū)域巖漿活動的關(guān)系及成礦意義

中亞造山帶是世界上最大的增生型造山帶，造就了巨量金屬堆積，形成了中亞成礦域(Seng, et al., 1993, Jahn, et al., 2004, Windley, et al., 2007, Pirajno, et al., 2008, Wilhem, 2012)。西準噶爾地體位于中亞造山帶西南一帶，且石炭紀-早二疊世是新疆北部最為重要的金屬礦床成礦期(Yakubchuk, 2004, Seltmann, et al., 2005, 肖文交等，2006, 朱永峰等，2007, 馮京等，2010, 楊富全等，2010, 尹繼元，2011)。西準噶爾南部尤其是達爾布特斷裂帶兩側(cè)，侵入巖分布廣泛，可分為小巖體、大巖基和中基性巖墻或者巖脈(沈遠超等，1993)。小巖體包括包古圖的Ⅰ至Ⅹ號(如魏少妮等, 2015)、加爾塔斯(劉建平等，2009)、玉依塔勒盆克提(Zhang, et al., 2015)等小巖體，均與Cu-Au礦床或礦化有關(guān)，這些小巖體巖性主要為石英閃長巖和花崗閃長巖。大巖基包括如哈圖、鐵廠溝、廟兒溝、阿克巴斯套、加甫沙爾蘇、紅山，這些大巖基大部分沒有Cu-Au礦化，大多數(shù)為A2型花崗巖(蘇玉平，2006)。大巖基的年代學研究較為深入，時代集中在308～296Ma之間(蘇玉平，2006, 韓寶福，2006, Geng, 2009, 馮乾文，2012)。小巖體的研究工作主要集中在包古圖一帶，時代主要集中在313～319Ma，具有埃達克型巖石的地球化學特征(張連昌，2006, Song, 2007, Shen, 2009, Tang, 2010, Shen, 2012)。但是，同時一些二長花崗巖和正長花崗巖往往出露面積也較小，周圍發(fā)育大量石英脈，往往產(chǎn)有Au礦床。

統(tǒng)計意義上講，區(qū)域上大多數(shù)Cu-Au礦與晚古生代巖漿作用有關(guān)。該帶Cu-Mo-W-Be等成礦元素組合好，異常有一定規(guī)模分布(陳宣華，2015)，西準噶爾地區(qū)發(fā)育還原性斑巖銅礦和石英脈型-斑巖型鎢鉬礦，具有Cu-Au-Mo-W組合(Shen, 2013)。此外，以前該區(qū)的成礦時代主要集中在晚石炭世早期如包古圖等(Song, 2007, Liu, 2009, Shen, 2009, Shen, 2012)。根據(jù)環(huán)形影像特征、色調(diào)差異及環(huán)形水系特征，該區(qū)還識別出了不同尺度的巖體和(或)隱伏巖體(魏永明等，2015)，也說明西準噶爾地區(qū)成礦地質(zhì)條件不僅優(yōu)越，而且有待進一步深入研究。

綜上所述，本次早二疊世早期的年代學資料證實該區(qū)可能存在晚石炭世—早二疊世的成礦作用，有可能是由該期大規(guī)模的A2型花崗質(zhì)巖漿作用供給成礦物質(zhì)來源和熱動力的。

致謝:野外地質(zhì)工作得到了新疆地礦局第七地質(zhì)大隊同行的大力幫助。長安大學李永軍教授在野外調(diào)研、論文寫作及分析測試工作中給予了幫助和指導。

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Zircon U-Pb Geochronology of Pluton from Baobei Gold Orefield in Western Junggar and Its Metallogenic Significance

WANG Lemin1, DUAN Fenghao2, JI Zhengbao3, WANG Ran2, ZHAO Delong2,GUO Xin2, CHENG Wanli2

(1. Xinjiang Department of Land and Resources; Urumqi 830002, Xinjiang , China; 2. Earth Science & Resources College of Chang’an University, Xi’an 710054, Shaanxi, China; 3. No.7 Geological Party，Xinjiang Bureau of Geology and Mineral Resources Exploration, Wusu 833000, Xinjiang, China)

The Baobei Au deposit is located in the West Junggar region of Xinjiang. The pluton has been found in the deposit area that intruded into Early Carboniferous sedimentary strata. U-Pb dating for samples obtained from the granite in the deposit yield a weighted mean age of (300.3 ± 8.6) Ma (2, N=10), which is consistent with the peak ages of the magmatic activity in the West Junggar region, indicating that the deposit is genetically related with an early Permian metallogenic system. This consistency suggests the relative large potentiality of finding more Cu deposits in the belt.

Baobei gold deposit; LA-ICP-MS zircon U-Pb dating; regional metallogenisis; west Junggar

2015-04-01；

2015-05-07

國家自然科學基金項目(41402044)、中國博士后基金特別資助項目(2013T60869)和新疆兩權(quán)中央留成專項資金項目(Y14-5-LQ06)聯(lián)合資助

王樂民(1971-),男,甘肅永登人, 本科，1997年畢業(yè)于東華理工大學地質(zhì)礦產(chǎn)勘查專業(yè)，高級工程師。E-mail：WLM66888@163.com

P618.51

A

1009-6248(2015)03-0241-10