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    青海大黑山鎢礦黑云二長(zhǎng)花崗巖的鋯石U-Pb同位素定年及巖石地球化學(xué)特征**

    2014-03-14 06:47:47劉敏張作衡向君峰曹德智楊光華LIUMinZHANGZuoHengXIANGJunFengCAODeZhiandYANGGuangHua
    巖石學(xué)報(bào) 2014年1期
    關(guān)鍵詞:加里東寶庫(kù)祁連

    劉敏 張作衡 向君峰 曹德智 楊光華LIU Min, ZHANG ZuoHeng, XIANG JunFeng, CAO DeZhi and YANG GuangHua

    1. 中國(guó)地質(zhì)大學(xué)地球科學(xué)與資源學(xué)院,北京 1000832. 中國(guó)地質(zhì)科學(xué)院礦產(chǎn)資源研究所,國(guó)土資源部成礦作用與資源評(píng)價(jià)重點(diǎn)實(shí)驗(yàn)室,北京 1000373. 青海省地質(zhì)調(diào)查院,西寧 8100124. 西安地質(zhì)礦產(chǎn)勘查開(kāi)發(fā)院,西安 7101001. School of Earth Sciences and Mineral Resources, China University of Geosciences, Beijing 100083, China2. MLR Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral Resources, CAGS, Beijing 100037, China3. Qinghai Geological Survey Institute, Xining 810012, China4. Xi’an Institute of Geological and Mineral Exploration, Xi’an 710100, China2013-09-02 收稿, 2013-12-09 改回.

    1 引言

    祁連山加里東造山帶是我國(guó)西北地區(qū)重要的鎢資源地,區(qū)內(nèi)相繼發(fā)現(xiàn)了塔兒溝和小柳溝大型鎢礦床及一些中小型礦床(《中國(guó)礦床》編委會(huì),1994;毛景文等,1999;Maoetal., 1999a, b; 張作衡等,2002;楊忠堂等,2002, 2004;林國(guó)芳和林鳳萍,2003),初步顯示了該成礦帶找鎢礦的巨大潛力。大黑山鎢礦位于青海寶庫(kù)河上游大黑山一帶,距大通縣城120km。該礦床由青海省地質(zhì)礦產(chǎn)勘查院于2002年發(fā)現(xiàn)(曹德智和薛培林,2008*曹德智,薛培林.2008.青海省大通縣大黑山地區(qū)鎢礦普查報(bào)告. 內(nèi)部資料, 1-93),目前正處于普查階段,研究程度較低,已有報(bào)導(dǎo)僅限于大黑山鎢礦地質(zhì)特征及找礦標(biāo)志的研究(曹德智和薛培林,2008;王飛等,2012;吳少鋒等,2012;丁成旺等,2013),對(duì)與成礦有關(guān)花崗巖的年代學(xué)、巖石學(xué)、地球化學(xué)尚未進(jìn)行詳細(xì)的研究,在一定程度上影響了鎢礦成因、形成環(huán)境等的深入探討。本文通過(guò)對(duì)與成礦有關(guān)花崗巖的巖石學(xué)、年代學(xué)和地球化學(xué)的研究,探討了花崗巖的形成時(shí)代、地球化學(xué)特征、巖石成因及來(lái)源,為祁連山加里東造山帶鎢礦成礦帶的成礦背景研究提供新的依據(jù)。

    2 礦區(qū)地質(zhì)

    青海大黑山鎢礦位于青海省門(mén)源回族自治縣、大通回族自治縣以及海晏縣三縣管轄地區(qū),其地理坐標(biāo)為:東經(jīng)101°02′15″,北緯37°24′130″(吳少鋒等,2012)。構(gòu)造上位于秦祁昆晚加里東造山系祁連造山帶北祁連造山亞帶與中祁連元古宙古陸塊體接合部位的南側(cè)(圖1)。該區(qū)地質(zhì)構(gòu)造十分復(fù)雜,經(jīng)歷了多次構(gòu)造運(yùn)動(dòng),其中以加里東運(yùn)動(dòng)最為強(qiáng)烈,是一條多旋回造山帶,總的構(gòu)造線方向?yàn)楸蔽魑飨?。區(qū)域構(gòu)造以斷裂構(gòu)造為主,褶皺構(gòu)造為輔。其主要的斷裂構(gòu)造是貫穿全區(qū)的北西西向的逆斷層,后期斷裂具明顯的繼承性活動(dòng)特點(diǎn),在其南、北側(cè)依次形成較多的次級(jí)斷裂。次級(jí)斷裂的附近巖石破碎蝕變及片理化現(xiàn)象較普遍,形成了多條與區(qū)域構(gòu)造線方向一致的破碎蝕變帶。此外還產(chǎn)生一組北北西向高角度平移斷層。中北祁連之間的深大斷裂呈北西-南東向延伸,傾向南西,該斷裂北東部為北祁連的上奧陶統(tǒng),斷裂長(zhǎng)期活動(dòng)對(duì)南北兩側(cè)沉積作用、變質(zhì)作用及巖漿活動(dòng)有明顯的控制作用。加里東褶皺構(gòu)造較為發(fā)育, 其主要表現(xiàn)在中、 下元古界及上奧陶統(tǒng)扣門(mén)子組的斜長(zhǎng)黑云片麻巖、黑云石英片巖之中,常見(jiàn)早期褶曲被后期次級(jí)褶曲所疊加,次級(jí)褶曲又被更次級(jí)褶曲所復(fù)雜化,同時(shí)其表現(xiàn)形態(tài)及其組合方式比較復(fù)雜,但主體產(chǎn)狀仍以北西-南東向?yàn)橹?。區(qū)域巖漿活動(dòng)強(qiáng)烈,規(guī)模較大,巖性從超基性-酸性均有出露。侵入巖巖性以酸性為主,中性、基性、超基性巖次之。以巖基式酸性花崗巖為主(寶庫(kù)河花崗巖體),巖株、巖脈式中、酸性閃長(zhǎng)巖、花崗巖次之,存在著多期次、侵入廣泛的特點(diǎn)。

    圖1 北祁連大坂山區(qū)域地質(zhì)圖(據(jù)王飛等,2012)Fig.1 Geological sketch map of Daban mountains in the northern Qilian (after Wang et al., 2012)

    礦區(qū)出露地層主要為下元古界托賴巖群片麻巖組、大理巖組和第四系。斷裂構(gòu)造不甚發(fā)育,裂隙、節(jié)理等緊緊圍繞寶庫(kù)河花崗巖體,具放射狀分布的特點(diǎn)。礦區(qū)褶皺構(gòu)造均以揉皺、褶曲形式出現(xiàn),較為發(fā)育,呈北西-南東向緊密-稀疏狀展布,與地層走向一致,局部亦有南北向褶曲。

    礦區(qū)內(nèi)巖漿巖主要有寶庫(kù)河花崗巖、大坂山蛇綠巖等。其中寶庫(kù)河花崗巖體為一復(fù)式巖體,是礦區(qū)的主要巖體,分布于礦區(qū)中南部,出露面積較大。巖性以灰白色粗中粒黑云二長(zhǎng)花崗巖、中細(xì)粒英云閃長(zhǎng)巖為主。

    礦區(qū)內(nèi)主要礦帶均位于花崗巖外接觸帶中,元古代片麻巖呈島嶼狀殘存于花崗巖體內(nèi),而含礦的矽卡巖帶又賦存在元古代片麻巖地層內(nèi),黑云二長(zhǎng)花崗巖呈巖枝狀沿片麻巖片麻理侵入的小巖體與圍巖的外接觸帶則是礦體集中賦存的部位。礦區(qū)共劃分出6個(gè)礦帶,其中以Ⅱ號(hào)礦帶規(guī)模最大,由6條斷續(xù)平行排列的礦體組合而成,礦體總體呈平行南北向分布(圖2),北端被一東西向斷層截?cái)嗖⑹芷淇刂?,其它礦帶規(guī)模較小。礦體形態(tài)較為復(fù)雜,呈似層狀、囊狀、分支脈狀、或具復(fù)合膨大的復(fù)雜透鏡體狀,走向穩(wěn)定,多產(chǎn)于透輝石矽卡巖中,矽卡巖圍巖為黑云石英片巖。

    礦化類型主要是白鎢礦化矽卡巖型,局部可見(jiàn)有白鎢礦化二長(zhǎng)花崗巖型和螢石石英脈型,其中,矽卡巖型是主要的礦石類型,目前約占全區(qū)礦石總量的90%以上。礦石主要呈均勻粒狀變晶結(jié)構(gòu),纖狀變晶結(jié)構(gòu)、柱狀變晶結(jié)構(gòu)、交代結(jié)構(gòu)和交代殘余結(jié)構(gòu),塊狀、浸染狀及斑雜狀構(gòu)造(丁成旺等,2013)。地表礦石中主要金屬礦物是白鎢礦,局部伴生微量黃鐵礦、磁黃鐵礦、黃銅礦、褐鐵礦;非金屬礦物有透輝石、石榴石、綠簾石、螢石、透閃石、斜長(zhǎng)石、硅灰石、矽線石、陽(yáng)起石、石英、磷灰石、方解石、榍石。深部鉆孔內(nèi)礦石中金屬礦物除白鎢礦、黃鐵礦、磁黃鐵礦、黃銅礦外還見(jiàn)有閃鋅礦等,非金屬礦物還出現(xiàn)了橄欖石、石榴石等典型矽卡巖的礦物組合。

    圍巖蝕變類型主要為矽卡巖化、硅化、云英巖化及黃鐵礦化等。成礦過(guò)程可劃分為4個(gè)階段,即:(1)矽卡巖階段:主要礦物有透輝石、符山石、石榴石等;(2)退化蝕變階段:除第1階段所形成的矽卡巖化的一般礦物外,尚有大量的透閃石、斜長(zhǎng)石、白云母及白鎢礦、綠簾石、石英等礦物生成,該階段為本礦床主要成礦階段。(3)石英硫化物階段:主要礦物為石英,含少量黃鐵礦、磁黃鐵礦、黃銅礦、輝鉬礦和白鎢礦等,多呈脈狀、細(xì)脈狀和浸染狀疊加于矽卡巖和退化蝕變巖之上;(4)碳酸鹽-螢石階段:以形成細(xì)脈狀、浸染狀和塊狀方解石和螢石組合為特征,方解石-螢石細(xì)脈疊加于石英-硫化物細(xì)脈之上(吳少鋒等,2012;丁成旺等,2013)。

    3 巖體地質(zhì)及巖相學(xué)特征

    寶庫(kù)河花崗巖是礦區(qū)的主要巖體,主要分布于礦區(qū)中南部,所占面積較大。巖體侵入于下元古界托賴巖群內(nèi),位于寶庫(kù)河背斜軸部。接觸界線中間部分向北凸起呈彎曲狀,內(nèi)接觸帶巖石顆粒變細(xì),暗色礦物具定向排列,長(zhǎng)石被交代呈蠶食狀邊緣。局部出現(xiàn)片麻狀構(gòu)造,接觸面與圍巖片理或片麻理基本一致。巖體邊緣部見(jiàn)有圍巖(黑云母石英片巖、角閃片巖、石英片巖)捕虜體。外接觸帶寬度不等,一般為300~500m。片巖、片麻巖遭受混合巖化。巖體侵入深度不大,成巖后剝蝕程度中等。目前所發(fā)現(xiàn)含白鎢礦矽卡巖多產(chǎn)于該套花崗巖和片麻巖之中。

    巖體的主要巖性為灰白色中粗粒黑云二長(zhǎng)花崗巖、中細(xì)粒-中粒英云閃長(zhǎng)巖。

    灰白色中粗粒黑云二長(zhǎng)花崗巖(圖3a-d):塊狀構(gòu)造,二長(zhǎng)結(jié)構(gòu),主要礦物為斜長(zhǎng)石、石英、微斜長(zhǎng)石、黑云母等。斜長(zhǎng)石25%~40%,屬更長(zhǎng)石,多呈半自形板柱狀,雙晶發(fā)育,晶粒粗大,具環(huán)帶狀結(jié)構(gòu),表面常發(fā)育泥化、絹云母化及高嶺土化而呈現(xiàn)土灰色(圖3c),聚片雙晶及卡鈉復(fù)合雙晶發(fā)育。鉀長(zhǎng)石20%~45%,屬微斜長(zhǎng)石、他形粒狀、半自形、格子雙晶,晶粒粗大有輕微粘土化,充填于斜長(zhǎng)石空隙之中。局部具有條紋結(jié)構(gòu)、蠕蟲(chóng)結(jié)構(gòu)。石英20%~35%,呈他形粒狀、柱狀充填于斜長(zhǎng)石之間的孔隙中,也見(jiàn)少量包裹于長(zhǎng)石中的呈半自形-自形粒狀的石英,多具波狀消光,部分石英在結(jié)晶后受壓破碎,呈集合體狀出現(xiàn),分布在長(zhǎng)石晶粒之間略具定向排列,有的交代長(zhǎng)石使得長(zhǎng)石邊緣呈蠶食狀。黑云母2%~10%(圖3c),褐色、多色性顯著,呈自形片狀,略具定向排列,部分被白云母、綠泥石交代呈殘留狀,見(jiàn)有鐵質(zhì)、榍石沿原解理縫充填。副礦物有鋯石、磷灰石、金紅石、螢石、白鎢礦、獨(dú)居石、磁鐵礦、石榴石、黃鐵礦、褐鐵礦、方鉛礦、釷石等呈微粒狀零星分布。

    圖2 大黑山鎢礦地質(zhì)圖(據(jù)曹德智和薛培林,2008修改)Fig.2 Geological map of Daheishan tungsten ore deposit (modified after Cao and Xue, 2008)

    圖3 寶庫(kù)河黑云二長(zhǎng)花崗巖的野外(a)及顯微(b-d)照片Qtz-石英;Kfs-鉀長(zhǎng)石;Bt-黑云母;Pl-斜長(zhǎng)石Fig.3 Photographs (a) and micrographes (b-d) of biotite monzonitic granite from Baokuhe plutons

    中細(xì)粒-中粒英云閃長(zhǎng)巖:塊狀構(gòu)造,花崗結(jié)構(gòu),主要礦物為斜長(zhǎng)石、石英、鉀長(zhǎng)石,少量黑云母、白云母等。斜長(zhǎng)石50%~65%,半自形板柱狀,具環(huán)帶狀結(jié)構(gòu)。粒度較小,不規(guī)則排列,且分布不均,絹云母化較發(fā)育。石英20%~30%,呈他形粒狀充填于斜長(zhǎng)石之間的孔隙中,略具定向排列,因動(dòng)力變質(zhì)作用的參與,使其原始結(jié)晶形態(tài)發(fā)生一定改變,常見(jiàn)有壓碎或沿某一方向拉長(zhǎng)的現(xiàn)象,具波狀消光,粒徑為0.06~1.26mm之間,常于局部聚集。鉀長(zhǎng)石10%~15%,屬微斜長(zhǎng)石,多呈他形-半自形粒狀,格狀雙晶發(fā)育,晶粒較斜長(zhǎng)石和石英粗大,充填于斜長(zhǎng)石空隙之中,且普遍發(fā)育輕微泥化,局部具有碎?;奶攸c(diǎn)。黑云母2%~15%,褐色、多色性顯著,呈自形片狀,部分被白云母交代。副礦物主要有鐵鋁榴石、榍石等。

    4 樣品和分析方法

    分析測(cè)試樣品均為無(wú)蝕變和礦化影響或蝕變甚弱的樣品,其中用于定年的樣品為黑云母二長(zhǎng)花崗巖(BKY-20)。

    主量元素、微量元素、稀土元素的測(cè)試在國(guó)家地質(zhì)實(shí)驗(yàn)測(cè)試中心測(cè)試完成,主量元素主要采用X熒光光譜儀(2100)測(cè)定;微量元素及稀土元素采用等離子質(zhì)譜(X-series)測(cè)定,以AMH-1和GBPG-1為參考標(biāo)樣,相對(duì)偏差(RSD)均小于5%。

    用于U-Pb測(cè)年的鋯石是將樣品經(jīng)人工破碎,采用常規(guī)的重力和磁選方法分離后,在雙目顯微鏡下人工挑選獲得。將代表性的鋯石顆粒粘在雙面膠上,然后用無(wú)色透明的環(huán)氧樹(shù)脂固定,待環(huán)氧樹(shù)脂充分固化后拋光至鋯石露出一個(gè)平面。然后進(jìn)行透、反射和陰極發(fā)光(CL)照像,結(jié)合這些圖像選擇適宜的測(cè)試點(diǎn)位。鋯石LA-ICP-MS U-Pb分析在南京大學(xué)內(nèi)生金屬礦床成礦機(jī)制國(guó)家重點(diǎn)實(shí)驗(yàn)室完成。采用儀器為Agilent 7500a ICP-MS,實(shí)驗(yàn)原理和詳細(xì)測(cè)試方法對(duì)照J(rèn)acksonetal.(2004)所述。其工作參數(shù)為:等離子氣體Ar 16L/min,輔助氣體Ar 1L/min,剝蝕物質(zhì)載氣He 0.9~1.2L/min。激光剝蝕系統(tǒng)波長(zhǎng)213nm,激光脈沖頻率5Hz,寬度5ns,剝蝕孔徑40μm,剝蝕時(shí)間80s,背景測(cè)量時(shí)間40s,脈沖能量為10~20J/cm2,206Pb、207Pb、208Pb、232Th 和238U的停留時(shí)間依次為15、30、10、10 和15ms。應(yīng)用鋯石標(biāo)樣GJ-1進(jìn)行同位素分餾校正,GJ-1鋯石標(biāo)樣的測(cè)試值為(601±12)Ma;此外,在分析中加入“未知”標(biāo)樣Mud Tank(分析值735±12Ma),用于監(jiān)控測(cè)試的重現(xiàn)性和儀器的穩(wěn)定性,本實(shí)驗(yàn)室對(duì)GJ-1和Mud Tank鋯石標(biāo)樣的測(cè)試結(jié)果與其他實(shí)驗(yàn)室的測(cè)試結(jié)果一致。質(zhì)譜的分析數(shù)據(jù)通過(guò)即時(shí)分析軟件GLITTER計(jì)算獲得相應(yīng)的同位素比值、年齡以及誤差,上述數(shù)據(jù)采用目前較為廣泛接受的方法進(jìn)行普通鉛校正,校正后的最終結(jié)果應(yīng)用Isoplot(路遠(yuǎn)發(fā),2004)程序完成年齡計(jì)算和諧和圖的繪制。

    5 分析結(jié)果

    5.1 鋯石U-Pb年代學(xué)

    用于鋯石定年的樣品中鋯石大小基本一致,顆粒較大,粒徑200~400μm,多呈長(zhǎng)柱狀,自形程度較好,大部分鋯石顆粒以灰白色、淡棕色為主。陰極發(fā)光(CL)圖像顯示(圖4),大部分鋯石具有明顯的密集振蕩環(huán)帶,顯示巖漿成因鋯石的典型特征(吳元保和鄭永飛,2004)。鋯石的LA-ICP-MS U-Pb同位素分析結(jié)果見(jiàn)表1及圖5。

    對(duì)樣品BKY20(黑云母二長(zhǎng)花崗巖)測(cè)試了21個(gè)點(diǎn),其中三個(gè)不諧和的206Pb-238U年齡(分別為151Ma、157Ma、431Ma)可能是Pb丟失的結(jié)果。其余的18個(gè)點(diǎn)均投影于諧和線上或諧和線附近,具有較一致的206Pb-238U年齡,變化于443~451Ma。黑云母二長(zhǎng)花崗巖中鋯石U的含量為55×10-6~1110×10-6,Th含量為65×10-6~1191×10-6,Th/U為0.48~1.60,平均為1.02,均大于0.4,屬巖漿成因鋯石。其206Pb-238U加權(quán)平均年齡為450.2±2.8Ma,MSWD值為0.102。

    可見(jiàn)寶庫(kù)河黑云二長(zhǎng)花崗巖形成于晚奧陶世,即加里東期花崗巖。

    表1寶庫(kù)河黑云母二長(zhǎng)花崗巖的LA-ICP-MS鋯石U-Pb年齡測(cè)試數(shù)據(jù)

    Table 1 LA-ICP-MS zircon dating result of the biotite monzonitic granite from Baokuhe plutons

    測(cè)點(diǎn)號(hào)Th(×10-6)U(×10-6)Th/U207Pb206Pb1σ207Pb235U1σ206Pb238U1σ208Pb232Th1σ207Pb206Pb1σ207Pb235U1σ206Pb238U1σ208Pb232Th1σBKY20-12481941.280.054710.001140.546280.011570.072420.000970.021580.0008400254438451643216BKY20-33527400.480.055120.000770.550830.008330.072480.000910.022370.00081417154465451544716BKY20-43364300.780.055530.000950.55460.00990.072440.000940.021910.00081434194486451643816BKY20-52963420.870.062290.003080.613750.029060.071460.0010.021970.000286841084861844564395BKY20-66024261.410.055990.003980.549230.038230.071150.001020.022150.000274521634442544364435BKY20-72612271.150.055670.001130.556670.011520.072530.000970.022620.00084439244498451645217BKY20-82201571.410.055890.001970.557760.019120.072380.001190.023140.000984484745012450746219BKY20-965551.170.055930.002220.559130.021480.072520.001260.023750.001084505545114451847421BKY20-102853120.910.055210.001090.552080.011130.072530.000960.023650.00089421234467451647218BKY20-115065460.930.056810.001080.566580.010870.072330.000920.020580.00102484224567450641220BKY20-1211919561.250.056110.00090.560180.009310.072410.000890.023090.00112457184526451546122BKY20-138928601.040.056630.001020.559430.010210.071650.00090.022150.00108477204517446544321BKY20-141341071.250.05570.002740.555570.026340.072350.001370.025020.001454407244917450849929BKY20-155685451.040.057860.001010.577640.010260.072410.00090.023710.00116524194637451547423BKY20-1662511100.560.057260.000980.571730.009980.072430.00090.022250.0011502194596451544522BKY20-174919480.520.05520.000890.5510.009140.07240.000890.024410.0012420184466451548724BKY20-194816560.730.055020.001160.549110.011560.072390.000940.023370.00118413254448451646723BKY20-21155961.600.058390.003530.582850.033790.072410.001630.021660.0013554487466224511043327

    圖4 寶庫(kù)河黑云母二長(zhǎng)花崗巖體部分鋯石樣品陰極發(fā)光(CL)圖像Fig.4 Cathodoluminescence images of zircon from the biotite monzonitic granite from Baokuhe plutons

    圖5 寶庫(kù)河黑云母二長(zhǎng)花崗巖的鋯石U-Pb年齡諧和圖Fig.5 The zircon U-Pb concordia diagram of the biotite monzonitic granite from Baokuhe plutons

    5.2 地球化學(xué)特征

    5.2.1 主量元素

    元素地球化學(xué)分析結(jié)果見(jiàn)表2。黑云母二長(zhǎng)花崗巖的SiO2含量為73.03%~74.18%,平均為73.49%;Al2O3含量為13.48%~13.94%,平均為13.71%;K2O+Na2O含量為7.25%~8.51%,平均為8.00%;K2O/Na2O為1.13~1.94,平均為1.54。鋁飽和指數(shù)(A/CNK)介于1.04~1.12,平均為1.07。P2O5含量為0.03%~0.08%,平均為0.05%。

    黑云母二長(zhǎng)花崗巖主要為高鉀鈣堿性系列(圖6)。在A/NK-A/CNK圖中(圖7)主要落于過(guò)鋁質(zhì)花崗巖區(qū)域。

    5.2.2 稀土元素

    寶庫(kù)河花崗巖稀土元素組成測(cè)試結(jié)果及相關(guān)參數(shù)見(jiàn)表2。黑云母二長(zhǎng)花崗巖稀土元素總量(∑REE)偏低,為110.5×10-6~214.4×10-6,平均值為178.1×10-6,低于世界花崗巖的平均值(∑REE=254.3×10-6, Vinogradov, 1962)。

    表2寶庫(kù)河黑云母二長(zhǎng)花崗巖的主量(wt%)、微量和稀土元素(×10-6)組成

    Table 2 Major element (wt%) and trace element (×10-6) data for the biotite monzonitic granite from Baokuhe plutons

    樣品號(hào)BKY-1BKY-3BKY-8BKY-10BKY-11BKY-13BKY-14BKY-21BKY-26SiO273.4373.0373.2373.3573.2973.5274.1873.5073.91Al2O313.7313.8013.5513.9413.7013.8713.4813.6813.60Fe2O30.140.320.110.390.140.450.220.170.30FeO1.451.421.511.491.381.241.241.451.10CaO1.591.381.151.501.041.571.291.331.08MgO0.370.390.430.500.360.460.370.420.37K2O4.074.835.423.945.504.274.745.205.47Na2O3.613.242.803.313.013.433.223.002.94TiO20.150.170.170.210.130.170.140.160.16MnO0.060.060.060.080.070.070.060.070.05P2O50.030.040.050.070.080.060.040.050.04H2O+0.640.720.700.760.420.620.620.640.62CO20.290.120.120.120.210.030.120.120.12LOI0.690.610.610.500.540.310.350.560.38K2O+Na2O7.688.078.227.258.517.707.968.208.41K2O/Na2O1.131.491.941.191.821.241.471.711.86A/NK1.331.311.291.431.251.351.291.291.26A/CNK1.041.051.081.121.071.061.051.051.07σ1.942.172.241.732.391.942.032.202.29Zr13414213216917913796.2125157Hf4.524.624.284.775.994.093.024.075.63Li18.218.924.525.036.536.719.228.820.0Be2.872.441.772.291.781.912.181.971.74Cr14.16.467.007.637.176.636.456.864.78Co1.631.641.902.411.712.271.682.001.63Ni6.043.172.753.463.103.503.833.583.00Cu8.7010.55.266.468.436.335.168.545.87Zn17.521.028.733.228.933.126.826.622.8Ga14.014.113.114.113.014.113.613.613.8Mo0.870.610.440.580.520.630.480.620.38Ta1.041.090.891.011.181.301.401.141.51W1.531.511.222.242.601.071.694.490.77Pb45.245.940.933.145.443.041.944.348.9Th46.356.754.136.937.327.526.441.754.1U6.437.964.172.763.832.413.184.145.76Ba5366671437122710018886791224652Sr110108187196131157129183112V9.4310.612.314.47.0710.39.8312.110.1Sc3.503.902.903.233.204.112.973.583.60Rb165205244192263216219256231Nb12.614.19.2211.012.413.014.213.011.3Cs14.413.96.4012.06.259.727.529.146.41Y37.530.212.110.812.814.810.416.011.4Rb/Sr1.501.901.300.982.011.381.701.402.06Nb/Ta12.1212.9410.3610.8910.5110.0010.1411.407.48La46.957.561.963.041.840.031.453.250.1Ce78.096.498.898.466.964.648.689.584.1Pr7.649.189.569.456.716.214.878.348.29Nd23.828.329.329.021.219.515.226.026.1Sm4.514.954.513.983.663.352.534.354.62Eu0.380.390.570.630.410.410.380.570.43Gd3.884.172.882.622.842.872.053.093.26Tb0.750.700.400.350.430.430.320.460.44Dy5.144.412.242.032.422.541.822.792.29Ho1.321.000.460.400.470.520.380.560.43Er4.083.131.251.161.361.531.141.731.22Tm0.630.490.180.170.190.220.190.260.17Yb4.373.301.261.231.371.541.431.761.36Lu0.650.480.190.190.210.230.210.260.20∑REE182.1214.4213.5212.6150.0144.0110.5192.9183.0L/H7.7411.1323.1025.0915.1413.5713.6616.6818.53δEu0.270.260.450.560.370.390.490.450.32(La/Yb)N7.7012.5035.2436.7421.8818.6315.7521.6826.42(La/Sm)N6.717.508.8610.227.377.718.017.907.00(Gd/Yb)N0.731.051.891.761.711.541.191.451.98

    圖6 寶庫(kù)河黑云母二長(zhǎng)花崗巖SiO2-K2O圖解(據(jù)Rickwood, 1989)Fig.6 SiO2 vs. K2O diagram of the biotite monzonitic granite from Baokuhe plutons (after Rickwood, 1989)

    圖8 寶庫(kù)河黑云母二長(zhǎng)花崗巖微量元素原始地幔配分模式圖(a)和稀土元素配分模式圖(b)(標(biāo)準(zhǔn)化值據(jù)Sun and McDonough, 1989)Fig.8 Primitive mantle-normalized trace element patterns and chondrite-normalized REE patterns diagrams of the biotite monzonitic granite from Baokuhe plutons (normalization values after Sun and McDonough, 1989)

    圖7 大黑山寶庫(kù)河花崗巖A/NK-A/CNK圖解(據(jù)Peccerillo and Taylor,1976)Fig.7 A/NK vs. A/CNK diagram of the biotite monzonitic granite from Baokuhe plutons(after Peccerillo and Taylor, 1976)

    其δEu值變化于0.26~0.56,(La/Yb)N值為7.70~36.74,(La/Sm)N值為6.71~10.22,(Gd/Yb)N值為0.73~1.98。

    稀土元素球粒隕石標(biāo)準(zhǔn)化圖解顯示(圖8b),黑云二長(zhǎng)花崗巖具有較一致的分布模式,其稀土配分模式曲線均為向右緩傾,Eu明顯負(fù)異常,其輕稀土La-Sm基本呈陡右傾式折線,LREE分異強(qiáng)烈;重稀土Cd-Lu曲線變化則較為復(fù)雜,呈一略向上或向下平緩折線,HREE分異不明顯。明顯不同于典型S型花崗巖常表現(xiàn)出的“海鷗型”稀土配分型式。

    5.2.3 微量元素

    寶庫(kù)河花崗巖微量元素組成測(cè)試結(jié)果及相關(guān)參數(shù)見(jiàn)表2。

    黑云母二長(zhǎng)花崗巖的高場(chǎng)強(qiáng)元素含量較高,Th為26.4×10-6~56.7×10-6,U為2.41×10-6~7.96×10-6,Pb為33.1×10-6~48.9×10-6,Zr為96.2×10-6~179×10-6,Hf為3.02×10-6~5.99×10-6,但Nb (9.22×10-6~14.2×10-6)與Ta (0.89×10-6~1.51×10-6)的含量相對(duì)較低,Nb/Ta比值較高,為7.48~12.94。大離子親石元素Ba含量為536×10-6~1437×10-6、Sr為108×10-6~196×10-6。此外巖石還具有較低的Cr (4.78×10-6~14.1×10-6)及Ni (2.75×10-6~6.04×10-6)。在原始地幔標(biāo)準(zhǔn)化蛛網(wǎng)圖中(圖8a)總體顯示了較為一致的分布模式,大離子親石元素Ba、Sr呈現(xiàn)明顯的負(fù)異常,高場(chǎng)強(qiáng)元素Th、U、Pb、Zr、Hf呈現(xiàn)明顯的正異常, Nb、Ta、Ti呈現(xiàn)負(fù)異常。P呈現(xiàn)負(fù)異常。

    6 討論

    6.1 巖體的形成時(shí)代

    本文獲得的黑云母二長(zhǎng)花崗巖鋯石的206Pb-238U加權(quán)平均年齡為:450.2±2.8Ma,即晚奧陶世,加里東期。可以代表該花崗巖的侵位結(jié)晶時(shí)代。

    黑云母二長(zhǎng)花崗巖450.2±2.8Ma的結(jié)晶年齡與已知的區(qū)域花崗巖的年齡及鎢大規(guī)模成礦時(shí)代很相近。毛景文等(1999, 2000a, b, 2003)及Maoetal. (2000)認(rèn)為北祁連西段發(fā)育有三條花崗質(zhì)巖帶,南部邊緣的花崗閃長(zhǎng)巖巖帶、北部邊緣的黑云母花崗巖帶及南部的堿性巖帶。這三條巖帶在1:20萬(wàn)區(qū)域地質(zhì)調(diào)查時(shí)被厘定為加里東期的產(chǎn)物。目前已獲得野牛灘巖體鋯石U-Pb年齡為459.6±2.5Ma(Maoetal., 2000);小柳溝二長(zhǎng)花崗巖鋯石LA-ICP-MS U-Pb年齡為454.0±2.0Ma(趙辛敏等,2014);車(chē)路溝巖體鋯石U-Pb年齡445.6±3.2Ma(賈群子等,2007);樺樹(shù)溝閃長(zhǎng)玢巖鋯石U-Pb年齡421±24Ma(張?zhí)m英等,2008);金佛寺巖體SHRIMP鋯石U-Pb諧和年齡為424Ma(吳才來(lái)等,2010);中祁連西段肅北巖體花崗巖SHRIMP鋯石U-Pb加權(quán)平均年齡為415±3Ma,石包城巖體花崗巖SHRIMP鋯石U-Pb加權(quán)平均年齡為435±4Ma(李建鋒等,2010)。眾多年齡均反映出在加里東及海西期祁連地區(qū)巖漿活動(dòng)強(qiáng)烈。Maoetal. (1995, 1998)、毛景文等(2003)、楊鐘堂等(2002,2004)、陳生民(2007)、楊國(guó)慶和楊春茂(2009)認(rèn)為祁連地區(qū)巖漿活動(dòng)強(qiáng)烈,加里東期及海西期是區(qū)內(nèi)中酸性巖漿活動(dòng)的鼎盛時(shí)期。吳少鋒等(2012)的研究表明本礦床中加里東期二長(zhǎng)花崗巖中鎢元素豐度值明顯高于其它花崗巖,空間上大黑山鎢礦也與加里東期二長(zhǎng)花崗巖關(guān)系最密切,說(shuō)明本區(qū)鎢礦的形成與加里東期酸性巖漿形成具有決定關(guān)系。

    6.2 巖石成因類型

    毛景文等(1999)認(rèn)為本區(qū)花崗巖為介于I型與S型花崗巖的一種過(guò)渡類型。吳才來(lái)等(2004)認(rèn)為在北祁連東部存在兩類I型花崗巖,一類以井子川巖體為代表,巖體形成的構(gòu)造環(huán)境類似島??;一類以黃羊河巖體為代表,巖體形成于造山后隆起環(huán)境或板內(nèi)環(huán)境。本次研究成果表明,寶庫(kù)河加里東期黑云母二長(zhǎng)花崗巖富硅、富鉀、鋁過(guò)飽和,屬于過(guò)鋁質(zhì)高鉀鈣堿性系列花崗巖。A/NK-A/CNK圖解(圖7)上基本落于I型花崗巖范圍內(nèi)。鋁過(guò)飽和,A/CNK值主要介于1~1.1,不同與典型S型花崗巖A/CNK>1.1 (Chappell and White, 1974, 1992) 。P2O5的含量低,表2顯示其含量具有隨SiO2含量的增長(zhǎng)呈現(xiàn)負(fù)增長(zhǎng)的趨勢(shì),也顯示了I型花崗巖的特征。稀土含量低,Eu明顯負(fù)異常,LREE分異強(qiáng)烈,HREE分異不明顯。微量元素元素蛛網(wǎng)圖中Th、U、Pb、Zr、Hf呈現(xiàn)明顯的正異常、Ba、Sr、Nb、P、Ti呈現(xiàn)負(fù)異常等。這些特征與本區(qū)的金佛寺花崗巖、野馬咀花崗巖(吳才來(lái)等,2010)、小柳溝花崗巖(趙辛敏等,2014)、新疆的鐵木爾特花崗巖(柴鳳梅等,2010)特征相類似,與南嶺燕山早期花崗巖(李獻(xiàn)華等,2007)的部分特征類似。結(jié)合本次研究成果認(rèn)為寶庫(kù)河加里東期黑云母二長(zhǎng)花崗巖應(yīng)該為I型花崗巖。

    6.3 地質(zhì)意義

    北祁連是我國(guó)最早鑒定出的俯沖帶之一,20世紀(jì)80年代以來(lái),該區(qū)早古生代的蛇綠巖、火山巖、高壓變質(zhì)巖及大地構(gòu)造演化研究,取得了許多重要進(jìn)展(王荃和劉雪亞,1976;肖序常等,1978;吳漢泉等,1990;許志琴等,1994;夏林圻等,1995,1996,1999,2000;馮益民,1997;張旗等,1997,2000;宋述光,1997;左國(guó)朝和吳漢泉,1997,左國(guó)朝等,1999;張建新和許志琴,1995;張建新等,1997,1998;毛景文等,1999;李文淵,2004;李文淵等,2005;吳才來(lái)等,2010)。馮益民(1997)認(rèn)為祁連山造山帶的構(gòu)造演化可以劃分為三個(gè)階段,即:(1)晉寧期基底的形成和其后的大陸裂谷構(gòu)造演化階段;(2)晚寒武-早中奧陶世洋底擴(kuò)張及溝弧盆體系大洋盆地演化;(3)早中奧陶世開(kāi)始的造山作用階段。在造山作用階段,祁連山經(jīng)歷了俯沖造山、碰撞造山和陸內(nèi)造山作用。俯沖造山開(kāi)始于460Ma或更早,其結(jié)果是在北祁連形成了島弧及島弧鏈,并造就了晚奧陶世殘留洋盆和中祁連北緣的陸緣裂谷。毛景文等(1999)認(rèn)為加里東期板塊俯沖晚期或碰撞造山早期及造山期后,在仰沖一側(cè)有一系列花崗巖先后侵位,與鎢礦有關(guān)花崗巖體由前期的花崗閃長(zhǎng)巖和晚期黑云母花崗巖組成,從早期到晚期,巖石體積變小,分異程度增高,鎢礦成礦作用與晚期巖體有密切關(guān)系。

    寶庫(kù)河黑云二長(zhǎng)花崗巖微量元素特征顯示Th、U、Pb、Zr、Hf呈現(xiàn)明顯的正異常、Nb、Ta、Ti呈現(xiàn)負(fù)異常等。具有島弧型巖漿作用的基本特征(Wilson, 1989)。在微量元素環(huán)境判別圖解上(圖9),寶庫(kù)河二長(zhǎng)黑云花崗巖也基本落于火山弧花崗巖的范圍內(nèi)。結(jié)合區(qū)域地質(zhì)演化研究表明450Ma北祁連仍處于俯沖造山階段,由于北祁連洋殼的俯沖,來(lái)自地殼的物質(zhì)熔融形成巖漿。巖漿在上侵或運(yùn)移過(guò)程中進(jìn)一步分異,下元古界托賴巖群被花崗質(zhì)巖漿交代,在巖漿熱液驅(qū)動(dòng)下,鎢元素從地層中被逐漸萃取并遷移,從而達(dá)到在有利部位的富集,含礦巖漿熱液首先形成矽卡巖,然后退化變質(zhì),形成白鎢礦,流體演化到石英硫化物階段又有白鎢礦沉淀。而后含鎢巖漿與后期含鎢熱液多次充填、交代作用下形成了現(xiàn)在的矽卡巖型白鎢礦床。

    圖9 寶庫(kù)河黑云母二長(zhǎng)花崗巖的微量元素環(huán)境判別圖解(據(jù)Pearce et al., 1984)(a)-(Y+Nb)-Rb; (b)-Y-Nb; (c)-Yb-Ta; (d)-(Yb+Ta)-RbORG-洋中脊花崗巖;VAG-火山弧花崗巖;WPC-板內(nèi)花崗巖;Syn-COLG-同碰撞花崗巖Fig.9 Tectonic discrimination diagrams of biotite monzonitic granite from Baokuhe plutons (after Pearce et al., 1984)

    7 結(jié)論

    (1)寶庫(kù)河黑云二長(zhǎng)花崗巖的鋯石LA-ICP-MS U-Pb加權(quán)平均年齡為:450.2±2.8Ma;為加里東期巖漿活動(dòng)的產(chǎn)物。

    (2)寶庫(kù)河黑云二長(zhǎng)花崗巖富硅、富堿,鋁過(guò)飽和,P2O5的含量低,且具有隨SiO2含量的增長(zhǎng)呈現(xiàn)負(fù)增長(zhǎng)的趨勢(shì),屬于過(guò)鋁質(zhì)高鉀鈣堿性系列花崗巖。稀土含量低,Eu明顯負(fù)異常,LREE分異強(qiáng)烈,HREE分異不明顯。微量元素元素蛛網(wǎng)圖中Th、U、Pb、Zr、Hf呈現(xiàn)明顯的正異常、Ba、Sr、Nb、P、Ti呈現(xiàn)負(fù)異常。為I型花崗巖。

    (3) 寶庫(kù)河黑云二長(zhǎng)花崗巖是由于北祁連洋殼的俯沖,地殼物質(zhì)重熔而形成的。

    致謝野外工作期間得到了青海地調(diào)院與大黑山鎢鉬礦項(xiàng)目組的大力支持與幫助;數(shù)據(jù)分析過(guò)程中得到了中國(guó)地質(zhì)科學(xué)院礦產(chǎn)資源研究所侯可軍助理研究員的大力幫助;在論文成文過(guò)程中得到了王曉霞研究員、袁順達(dá)副研究員的大量幫助;在此一并致以誠(chéng)摯的謝意。

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