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滇西北衙金多金屬礦床輝鉬礦Re-Os同位素年齡及其地質(zhì)意義

2015-03-07 06:34牛浩斌胡文懿寧括步董黎陽
地質(zhì)與勘探 2015年1期
關(guān)鍵詞:金屬礦床輝鉬礦斑巖

牛浩斌,胡文懿, 丁 俊, 李 俊, 寧括步,王 鵬,任 飛, 董黎陽

(1.成都地質(zhì)礦產(chǎn)研究所,四川成都 610081; 2.四川省科源工程技術(shù)測試中心,四川成都 610091)

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滇西北衙金多金屬礦床輝鉬礦Re-Os同位素年齡及其地質(zhì)意義

牛浩斌1,胡文懿2, 丁 俊1, 李 俊1, 寧括步1,王 鵬1,任 飛1, 董黎陽1

(1.成都地質(zhì)礦產(chǎn)研究所,四川成都 610081; 2.四川省科源工程技術(shù)測試中心,四川成都 610091)

北衙金多金屬礦床產(chǎn)出于滇西北富堿斑巖-多金屬成礦帶內(nèi)。礦床嚴(yán)格受富堿斑巖及其成生的深大斷裂構(gòu)造控制,并發(fā)育熱液交代現(xiàn)象,且在圍巖內(nèi)以產(chǎn)出充填型礦脈(囊)、交代型條帶礦(似層狀)為主,構(gòu)成斑巖-矽卡巖成礦系統(tǒng),具超大型金礦床規(guī)模。本文利用Re-Os同位素定年方法首次對北衙鐵金多金屬礦床全礦段金屬硫化物成礦年齡進(jìn)行精確測定,獲得5件輝鉬礦樣品的模式年齡為37.46~39.44 Ma,其加權(quán)平均年齡為(38.48±0.54)Ma,等時(shí)線年齡為(37.9±2.5)Ma,兩者在誤差范圍內(nèi)一致,與區(qū)域及區(qū)內(nèi)富堿斑巖鋯石U-Pb年齡基本保持一致;輝鉬礦中Re含量主體26.84×10-6~43.15×10-6之間,指示其成礦物質(zhì)來源于上地幔和下地殼,為殼?;旌显矗粌烧呔甘境傻V作用與該時(shí)期具幔殼混合源性質(zhì)的富堿巖漿淺成侵入關(guān)系密切。

輝鉬礦Re-Os同位素年齡 成礦年齡 動力學(xué)背景 北衙 滇西

Niu Hao-bin,Hu Wen-yi,Ding Jun,Li Jun,Ning Kuo-bu,Wang Peng,Ren Fei,Dong Li-yang. Re-Os isotope age of molybdenite in the Beiya Au-polymetallic deposit, western Yunnan Province and its geological implications[J]. Geology and Exploration, 2015, 51(1):0001-0012.

滇西北衙金多金屬礦床為西南三江富堿斑巖多金屬成礦帶重要、典型的富堿斑巖-熱液型、接觸交代型多金屬礦床;截止2010年底,金礦累積探明共伴生金屬量達(dá)160t以上,鐵礦資源量超過3000萬噸,已達(dá)超大型金礦及大型鐵礦規(guī)模,并伴有大量銀、鉛、鋅、銅等①;礦區(qū)外圍及整個礦集區(qū)內(nèi)具較好的找礦遠(yuǎn)景。目前已圈定南大坪-干海子-馬頭灣、響水河、觀音山、黃草坡、馬鞍山等重點(diǎn)找礦遠(yuǎn)景區(qū),并在黃草坡一帶已有新的礦化顯示②。前人對此礦床及礦集區(qū)控礦地質(zhì)特征、成礦作用及模式和成礦斑巖巖石及地球化學(xué)特征、成巖時(shí)代、演化過程及其成礦控礦作用等進(jìn)行了大量深入的研究(蔡新平等,1991a,1991b,1993;甫為民,1994;胡朝平等,1994;葛良勝等,2002;劉建云,2004;吳開興,2005;徐受民等, 2007;徐興旺,2006,2007;Xuetal.,2007a,2007b,2007c;薛傳東等,2008;Dengetal.,2010;肖曉牛等,2009,2011;楊金永,2010;和文言等,2012,2013;王宏偉等,2013;和中華等,2013),已獲得一批與成礦作用相關(guān)的成巖成礦時(shí)限,為區(qū)域成巖成礦系統(tǒng)研究和礦集區(qū)成礦找礦模式構(gòu)建提供基礎(chǔ)數(shù)據(jù),但本區(qū)金多金屬礦床主礦體至今未獲得精確成礦年齡數(shù)據(jù)。

本文基于“北衙地區(qū)三維地質(zhì)調(diào)查”項(xiàng)目地質(zhì)、物化、遙感及巖芯編錄等三維建模工作(孫岳等,2013),首次在北衙萬硐山采場及其深部鉆孔巖芯發(fā)現(xiàn)輝鉬礦,并對其進(jìn)行了Re-Os同位素年齡測定, 準(zhǔn)確地厘定了礦區(qū)內(nèi)萬硐山、紅泥塘礦段主礦體的金屬硫化物成礦年齡,結(jié)合前人已獲得的年齡數(shù)據(jù)探討該礦床及礦集區(qū)成礦物質(zhì)來源及其成礦地球動力學(xué)背景。

1 區(qū)域地質(zhì)背景

滇西北衙多金屬礦集區(qū)位于揚(yáng)子準(zhǔn)地臺西緣之麗江-鹽源臺緣西緣中生代坳陷,與德格-中甸陸塊、蘭坪-思茅陸塊呈弧形構(gòu)造結(jié)合部東側(cè),為金沙江-紅河、賓川-程海、麗江-木里斷裂所挾持范圍西側(cè)(圖1);整體處于西南三江構(gòu)造帶“蜂腰”地段和眾多深部、淺部構(gòu)造交匯、集中發(fā)育部位(李文昌等,2001;潘桂堂等,2003),為深源的富堿斑巖成群分布和巖漿熱液活動提供條件,形成新生代金沙江-紅河富堿斑巖帶(涂光熾,1984)及其多金屬成礦帶(侯增謙等,2004),并統(tǒng)一于晚二疊世以來的金沙江洋盆消減閉合-弧陸碰撞-陸內(nèi)碰撞造山-陸內(nèi)匯聚的多島弧盆碰撞造山過程(潘桂堂等,2003)。

區(qū)內(nèi)地層主要以上二疊統(tǒng)峨眉山玄武巖(P2β)為“基底”④,發(fā)育的一套三疊紀(jì)地層及小范圍的新生代地層;整體呈中新生代地層為玄武巖所圍繞的“四周老,中部新”的樣式分布(圖1)。玄武巖之上晚三疊紀(jì)地層為弧陸碰撞過程中弧后盆地轉(zhuǎn)變弧后前陸盆地內(nèi)沉積(潘桂堂等,2003),包括主要賦礦層北衙組(T2b)碳酸鹽巖;新生代地層多為陸內(nèi)造山過程中的走滑拉伸作用、拉分盆地沉積,局部發(fā)育較大規(guī)模的“紅色粘土型”鐵金礦⑥或現(xiàn)代殘坡積鐵金礦、河湖相沉積型(砂礫粘土型)及喀斯特堆積礫砂礦③(蔡新平等,1991a,1991b,1993)。

受金沙江-紅河、賓川-程海、麗江-木里斷裂控制,斷裂構(gòu)造主要有SN向弧形展布的天坪斷裂④、近SN向后本箐斷裂④、馬鞍山斷裂斷裂⑤、兩條近EW向隱伏基底斷裂(蔡新平等,1991a;葛良勝等,1999),以及近EW向構(gòu)造斷裂。

圖1 西南三江大地構(gòu)造分區(qū)圖(據(jù)潘桂堂等,2003整理)及北衙鐵金多金屬礦集區(qū)地質(zhì)圖(據(jù)②,④修改)Fig.1 Tectonic zone map of the Sanjiang in southwestern China ( modified from Pan Guitang et al.,2003 ) and geological map of the Beiya Au-polymetallic mineralization concentrated area Ⅰ-揚(yáng)子陸塊;Ⅱ-德格-中咱陸塊;Ⅲ-芒康-思茅陸塊;Ⅳ-保山-撣邦陸塊;Ⅴ-岡底斯-拉薩-騰沖陸塊;Ⅵ-印度陸塊;1-第四 系;2-三營組;3-寶相寺組;4-松桂組;5-中窩組;6-北衙組;7-青天堡組;8-峨眉山玄武巖;9-石英正長斑巖;10-采樣位置Ⅰ-Yangtze block; Ⅱ-Dege-Zhongdian block; Ⅲ-Mangkang-Simao block; Ⅳ-Baoshan-Shanbang block; Ⅴ-Gangdisi-Lasa-Tengchong block; Ⅵ-India block;1-Quaternary; 2-Sanying group; 3-Baoxiangsi group; 4-Songgui group; 5-Zhongwo Group; 6-Beiya group; 7-Qingtianbao group; 8-Emeishan basalt; 9-quartz orthophyre; 10-sampling location

區(qū)內(nèi)富堿斑巖主要沿近EW向隱伏基底斷裂、馬鞍山斷裂及其次級斷裂分布;前者影響著南大坪、干海子、小干海、馬頭灣、桅桿坡、白沙井等富堿斑巖體(脈),后者控制著SN向展布的鋪臺山、獅子山、萬硐山、紅泥塘、焦石硐、老馬澗等富堿斑巖體(脈)⑥。

2 礦床地質(zhì)特征

北衙金多金屬礦床位于區(qū)內(nèi)中部偏南,與萬硐山、紅泥塘(石英)正長斑巖一起分布于松桂-北衙復(fù)式向斜南部翹起端的北衙向斜核部及兩翼部位,受斜切北衙向斜西翼的馬鞍山斷裂及其次級斷裂控制,并與兩條近EW向隱伏基底斷裂交匯的萬硐山、紅泥塘處成巖成礦,且產(chǎn)于斑巖體邊部及圍巖裂隙、層間破碎帶內(nèi)。受區(qū)域上構(gòu)造影響,區(qū)內(nèi)主要發(fā)育近SN向弧形控礦斷裂和近EW向的破礦斷裂,并多沿EW向斷裂穿插充填有黑云正長斑巖脈。

圍巖主要有青天堡組(T1q)黃褐、灰綠色巖屑石英砂巖夾黃綠、紫紅色頁巖層,北衙組中下部(T2b1+2)灰色、淺灰色,中厚層瘤狀、蠕蟲狀(生物碎屑)灰?guī)r及泥質(zhì)灰?guī)r,局部夾砂泥質(zhì)碎屑巖薄層,以及向上漸變?yōu)榛赢a(chǎn)出的灰色、深灰色粒屑白云巖和微晶白云巖(T2b3);北衙組上部(T2b4)則為灰白色微晶白云巖與淺灰色含粒屑白云巖。其中,白云巖(T2b3、T2b4)普遍存在強(qiáng)烈的碳酸鹽化蝕變、褐鐵礦化特征,而灰?guī)r(T2b1+2)局部發(fā)育矽卡巖蝕變(圖3)及磁鐵礦化現(xiàn)象;部分碎屑巖(T1q)存在熱液接觸、交代成礦作用,呈角巖或角巖化產(chǎn)出,伴隨著黃鐵礦、黃銅礦等硫化礦物發(fā)育,并首次發(fā)現(xiàn)團(tuán)狀、條帶狀磁鐵礦化現(xiàn)象(圖4),具有較大的成礦潛力。

圖2 北衙金多金屬礦床地質(zhì)及采樣位置圖(據(jù)①,③修改)Fig.2 Geological map and sampling position map of the Beiya Au-polymetallic deposit①,③ 1-第四系;2-北衙組四段;3-北衙組三段;4-北衙組一、二段;5-青天堡組;6-峨眉山玄武巖;7-石英正長斑巖;8-煌斑巖脈;9-產(chǎn)狀;10-實(shí)測及推測界線;11-實(shí)測及推測斷層;12-礦體及其編號;13-采樣位置;14-隱伏基底斷 裂大致位置1-Quaternary ; 2-4th section of the Beiya group; 3-3th section of the Beiya group; 4-1th and 2th sections of the Beiya group; 5-Qingtianbao group; 6-Emeishan Basalt; 7-quarta orthophyre; 8-lamprophyre vein; 9-attitude; 10-measured and inferred geological bounderies; 11-measured and inferred faults; 12-ore bodies and their number; 13-sampling location; 14-location of concealed basement faults

與成礦關(guān)系密切的富堿斑巖主要為(石英)正長斑巖;巖性表現(xiàn)為角斑結(jié)構(gòu),斑晶(>50%)主要為鉀長石,少見石英、斜長石斑晶;基質(zhì)(<50%)主要為微粒狀長英質(zhì)礦物,以鉀長石為主,石英次之,常發(fā)育弱絹云母化蝕變。此外,沿順層及切層斷裂多穿插發(fā)育有云母煌斑巖脈及黑云母正長斑巖脈,時(shí)代上與(石英)正長斑巖相似具有多期次活動特征(Xuetal.,2007a, 2007b, 2007c ),并且早期云煌巖脈多具有褪色蝕變和較高的金含量,顯示可能與成礦作用有著內(nèi)在的聯(lián)系(楊金永,2010),或指示著多類型巖脈產(chǎn)出區(qū)具有較好的成礦前景③。

從礦體(原生)產(chǎn)出特征上看,區(qū)內(nèi)礦化類型可分為3類:Ⅰ.產(chǎn)于斑巖與北衙組灰?guī)r段接觸帶圍巖內(nèi)的條帶狀(似層狀)交代型鐵金礦體(脈),似接觸交代作用的矽卡巖型礦床(和文言等,2012);其中,青天堡組(T1q)粉砂質(zhì)泥(板)巖中普遍存在的團(tuán)狀、條帶狀磁鐵礦化(圖3)亦屬此類型;Ⅱ.產(chǎn)于斑巖、圍巖內(nèi)及其間并沿節(jié)理、裂隙及層間破碎帶、溶蝕坑洞穿插充填的脈狀及囊狀鐵金礦體(脈)(圖3),屬熱液成礦作用的熱液礦床類型(和文言等,2012);Ⅲ.產(chǎn)于斑巖及圍巖之間受后期壓扭性逆沖構(gòu)造作用的鐵金角礫巖型礦體,包括主要的磁-赤鐵礦及部分碳酸鹽巖角礫,后經(jīng)熱液作用,發(fā)生強(qiáng)烈的褐鐵礦化及綠簾-綠泥石化蝕變及礦質(zhì)進(jìn)一步富集作用,屬熱液疊加成礦類型(圖3)。其中,產(chǎn)于斑巖體與圍巖之間,且圍繞萬硐山石英正長斑巖體呈弧形不閉合環(huán)帶狀展布的K52礦體是北衙鐵金礦床最主要的礦體,發(fā)育Ⅱ、Ⅲ兩種成礦類型。

圖3 北衙金多金屬礦床礦化與蝕變特征Fig.3 Mineral alteration characters of the Beiya Au-polymetallic deposit a-砂巖內(nèi)的磁鐵礦脈(采自55ZK30-B3,T1q);b-矽卡巖內(nèi)共生的磁鐵礦、黃鐵礦(采自60ZK7_304 m,T2b1+2);c-磁鐵礦交代石榴子石形成殘余結(jié)構(gòu)(單偏光,采自60ZK7_293.20 m);d-黃鐵礦交代磁鐵礦形成殘余結(jié)構(gòu)(反光,采自55ZK30-B3);e-壓扭性逆沖構(gòu)造及熱液疊加改造的鐵金礦體;f-綠簾石化及硅孔雀石銅礦化現(xiàn)象;礦物代號(Kretz R,1983):Mag-磁鐵礦;Py-黃鐵礦; Ccl-硅孔雀石;Grt-石榴子石;Ep-綠簾石;Chl-綠泥石;Qtz-石英a-magnet Vein in sandstone(from the 55ZK30-B3, T1q); b-paragenetic magnets and pyrites in the skarn(from the 60ZK7_304 m, T2b1+2 ); c-relic structures by magnets replacing garnets(polarizing microscope, from the 60ZK7_293.20 m ); d-relic structures by pyrites replacing magnets(reflecting microscope, from the55ZK30-B3); e-Fe and Au ore body of compresso-shear overthrust tectonic and hydrothermal superimposition and reformation; mineral abbreviations(from Kretz R,1983): Mag-magnet; Py-pyrite; Ccl-chrysocolla; Grt -garnet; Ep-epidote; Chl-chlorite; Qtz-quartz

圖4 北衙金多金屬礦床輝鉬礦賦存特征Fig.4 Occurrence characters of molybdenite from the Beiya Au-polymetallic deposit a-石榴子石矽卡巖內(nèi)團(tuán)斑狀、浸染狀輝鉬礦(采自萬硐山礦段,T2b1+2); b-矽卡巖內(nèi)與黃鐵礦、黃銅礦共生的輝鉬礦(采自萬硐山礦段,T2b1+2);c-磁鐵礦化粉砂質(zhì)泥巖內(nèi)脈狀輝鉬礦(采自55ZK30_640 m,T1q); d-菱鐵礦內(nèi)的黃鐵礦、黃銅礦及輝鉬礦(采自79ZK6_240 m);礦物代號(Kretz R,1983):Mag-磁鐵礦;Py-黃鐵礦;Gn-方鉛礦;Ccp-黃銅礦;Mo-輝鉬礦;Sd-菱鐵礦;Grt -石榴子石;Qtz-石英a-porphyritic and disseminated molybdenites in garnet skar(from Wangdongshan ore block, T2b1+2); b-molybdenites with pyrites and chalcopyrites(from Wangdongshan ore block, T2b1+2); c-veined molybdenites in silty mudstone with magnetites(from 55ZK30_640 m, T1q); d-pyrites, chalcopyrites and molybdenites within siderites(from 79ZK6_240 m);Mineral abbreviations(from Kretz R,1983): Mag -magnet; Py-pyrite; Gn-gelenite; Ccp-chalcopyrite; Mo-molybdenite; Sd-siderite; Grt-garnet; Qtz-quartz

圍巖蝕變及礦化大體上可劃分兩個階段;Ⅰ.矽卡巖、角巖(化)及鐵成礦階段:伴隨著石榴子石、透輝石、陽起石、硅灰石等矽卡巖礦物和角巖(化)形成過程,以形成條帶狀、團(tuán)狀交代型磁鐵礦、磁-赤鐵礦和脈狀、囊狀充填型磁鐵礦為主(圖3);Ⅱ.熱液疊加及金屬硫化物階段:以石英、方解石等脈石礦物和黃鐵礦、黃銅礦、方鉛礦、輝鉬礦等金屬硫化物形成為主,呈脈狀、團(tuán)斑狀、浸染狀等形式疊加于早期階段礦化之上(圖3)。磁鐵礦多于后一階段氧化成褐鐵礦,而金主要以自然金狀態(tài)以裂隙、包裹形式賦存于褐鐵礦石內(nèi)①。

3 樣品采集與測試結(jié)果

為進(jìn)行精確確定和對比研究礦床成礦年齡及富堿斑巖成巖年齡,本次工作采集北衙礦區(qū)2件萬硐山礦段及3件紅泥塘礦段的含輝鉬礦接觸交代型的硫化物礦石及脈狀礦石。其中,輝鉬礦呈團(tuán)斑狀、浸染狀產(chǎn)于石榴子石矽卡巖內(nèi),與黃鐵礦、黃銅礦等硫化物礦物緊密共生(圖4),或呈細(xì)脈狀產(chǎn)于浸染狀或團(tuán)狀磁鐵礦化的粉砂質(zhì)泥(板)巖,與石英細(xì)脈緊密共生(圖4);該產(chǎn)出及共生特征指示輝鉬礦與區(qū)內(nèi)金屬硫化物成礦同期(張世銘等,2013),基本可代表萬硐山、紅泥塘全礦段金屬硫化物成礦年齡。

輝鉬礦的分選工作在河北省廊坊區(qū)域地質(zhì)礦產(chǎn)調(diào)查研究所實(shí)驗(yàn)室完成。用常規(guī)方法將巖石樣品粉碎至300 μm左右,經(jīng)淘洗、重選富集,再經(jīng)磁選和密度分選后,在雙目鏡下進(jìn)一步分離、挑純鋯石和輝鉬礦單礦物。輝鉬礦質(zhì)純,無包體,無污染,純度達(dá)98%以上。

本次輝鉬礦Re-Os測試是在國家地質(zhì)測試中心Re-Os同位素實(shí)驗(yàn)室進(jìn)行?;瘜W(xué)分離過程和分析方法見文獻(xiàn)(Du Andaoetal., 2004;杜安道等,2001;屈文俊等2003;Shireyetal.,1995)。輝鉬礦Re-Os同位素模式年齡t計(jì)算公式如下:

187Os——現(xiàn)在礦物中187Os含量(mol/g),分析中采用質(zhì)量濃度(ng/g);

187Re——現(xiàn)在礦物中187Re含量(mol/g),分析中采用質(zhì)量濃度(μg/g);

λ——187Re衰變常數(shù)1.666×10-11a-1(1.02%);

t礦物形成后的年齡,在公式中單位為百萬年(Ma)表示(Smolar M Ietal.,1996;Shen J Jetal.,1996)。

北衙金多金屬礦床5件輝鉬礦樣品經(jīng)上述方法測定,得到模式年齡為(37.46±0.57)~(39.44±0.79)Ma。采用Isoplot軟件作等時(shí)線和加權(quán)平均值(圖5),得到等時(shí)線年齡為(37.9±2.5)Ma,加權(quán)平均年齡為(38.48±0.54)Ma,兩者在誤差范圍內(nèi)一致。

圖5 北衙金多金屬礦床輝鉬礦Re-Os同位素 等時(shí)線及模式年齡加權(quán)平均值Fig.5 Re-Os isochron age and weighted average age for molybdenite from the Beiya Au-polymetallic deposit

4 討論

4.1 成礦年齡限定

西南三江富堿斑巖帶是新生代以來印度-亞歐板塊碰撞過程中的重要響應(yīng)(張玉泉等,1998a,1998b),并伴隨著與富堿斑巖活動有關(guān)的Cu、Mo、Au、Ag、Pb等多大規(guī)模金屬成礦作用(侯增謙等,2004;曾普勝等,2006;薛傳東等,2008;鄧軍等,2010;鄧軍等,2011),時(shí)代集中于38~33 Ma(鄧軍等,2011)。

北衙金多金屬礦床是此富堿斑巖成礦帶中南段的典型礦床之一(薛傳東等,2008),與形成于37.93~31.3 Ma的富堿斑巖密切相關(guān)(徐受民等,2006;李勇等,2011;和文言等,2012)。斑巖成礦通常出現(xiàn)在最晚期次含礦斑巖侵入前1~3 Ma(侯增謙等,2003),或晚于主成礦斑巖0.5~3 Ma(侯增謙等,2004;王登紅等,2004)。和文言等(2013)在北衙金多金屬礦床紅泥塘礦段取得1件輝鉬礦Re-Os年齡36.87±0.76 Ma和斑巖鋯石LA-ICP-MS U-Pb年齡36.48±0.26 Ma,與萬硐山巖體及區(qū)域上新生代富堿斑巖帶成巖作用峰期一致(和文言等,2013)。

為更全面精確研究北衙金多金屬礦床全礦段成礦時(shí)代,本次就整個北衙金多金屬礦床采得5件含輝鉬礦巖石樣品,輝鉬礦呈團(tuán)斑狀、浸染狀與硫化物礦物緊密共生產(chǎn)于交代蝕變巖或矽卡巖內(nèi),或呈細(xì)脈狀與石英細(xì)脈緊密共生產(chǎn)于浸染狀或團(tuán)狀磁鐵礦化的粉砂質(zhì)泥(板)巖內(nèi),指示著其為同期成礦作用產(chǎn)物;由于輝鉬礦較云母、長石等蝕變礦物K-Ar及40Ar-39Ar具有封閉溫度高(~500℃)的優(yōu)點(diǎn),可以更直接準(zhǔn)確測得硫化物成礦年齡(Minsteretal.,1979;Ishiharaetal.,1989;Suzukietal.,1996;Steinetal.,1997,2001;Selbyetal.,2002);本次測得Re-Os同位素等時(shí)線年齡37.9±2.5Ma,加權(quán)平均年齡為38.48±0.54Ma,與已有萬硐山、紅泥塘含礦斑巖鋯石LA-ICP-MS U-Pb同位素年齡大致在同一范圍,可以代表北衙金多金屬礦床大規(guī)模成礦年齡。

4.2 成礦動力學(xué)背景

本區(qū)位于西南三江的“蜂腰”地段,處于多島弧盆與揚(yáng)子陸塊碰撞結(jié)合處(潘桂堂等,2003)。自始新世以來,該區(qū)經(jīng)歷了主碰撞陸陸匯聚階段(65~41 Ma)、晚碰撞構(gòu)造轉(zhuǎn)換階段(40~26 Ma)及后碰撞地殼伸展階段(25~0 Ma)(侯增謙等,2006;鄧軍等,2011),并伴隨近SN向的褶皺推覆、壓扭性及張扭性走滑、近EW向伸展等構(gòu)造作用和相應(yīng)期次的富堿巖漿活動(侯增謙等,2004)。西南三江富堿斑巖帶中的江達(dá)-鶴慶-大理含礦斑巖亞帶(侯增謙等,2004)主要形成于37.93~31.3Ma(徐受民等,2006;李勇等,2011;和文言等,2012),與構(gòu)造轉(zhuǎn)換時(shí)期一致,受SN走滑斷裂及其次級斷裂構(gòu)造控制;同時(shí)該斑巖帶內(nèi)的玉龍(輝鉬礦Re-Os:41.2±0.3 Ma)、北衙(輝鉬礦Re-Os:37.9±2.5 Ma)、馬廠箐(輝鉬礦Re-Os:35.8±1.6 Ma)等超大型多金屬礦床(曾普勝等,2006),均與其各斑巖巖漿活動同期,表現(xiàn)出與其存在著密切成生關(guān)系,具有相似的成礦動力學(xué)背景及條件。也由此,金屬礦物和含礦斑巖的相關(guān)示蹤、對比研究可直接反映成礦源區(qū)及動力學(xué)背景等方面的信息。

表1 北衙金多金屬礦床Re-Os同位素分析測試數(shù)據(jù)

前人研究顯示,Re-Os同位素體系內(nèi)Re含量可以示蹤金屬硫化物源區(qū),衡量地殼物質(zhì)混然程度(Foster, J Getal.,1996),且從幔源-幔殼混源-殼源,輝鉬礦內(nèi)Re含量呈n×10-4-n×10-5-n×10-6數(shù)量級降低(Steinetal.,1997;Mao Jinwenetal.,1999)。如表1,區(qū)內(nèi)Re含量在2.719~43.15×10-6之間變化,僅有1件樣品Re含量為2.719×10-6,顯示地殼物質(zhì)混染程度較高,其余為2.684~4.315×10-5區(qū)間,與和文言等(2013)所測的1件輝鉬礦Re含量(2.027±0.16)×10-5保持一致,均指示著金屬硫化物成礦物質(zhì)主要為幔殼混合來源。這也與已有的含礦斑巖及礦物質(zhì)示蹤、對比研究認(rèn)識相一致。

區(qū)域上,與成礦緊密相關(guān)的富堿斑巖存在如下特征:SiO2飽和或過飽和、高K2O、低N2O,143Nd/144Nd值0.512317~0.512597,εNd(t)值-6.75-~1.28,εSr值21.1~42.3,而208Pb/204Pb、207Pb/204Pb、206Pb/204Pb分別為38.442~38.676、15.541~15.615、18.49~18.603;這些特征顯示幔源特征,為其經(jīng)地殼不同程度混染的產(chǎn)物(曾普勝等,2002)。另一方面,富堿斑巖中常見有包體巖石,其富鐵玻璃組成和富鐵熔漿獨(dú)立包體中存在著碳硅石、含鉻自然鐵、鈦鐵礦及含鈦鏡鐵礦等地幔標(biāo)志型礦物,且富鐵熔漿包體硅同位素呈現(xiàn)出未經(jīng)動力分餾低負(fù)值(34Si=-0.8‰),也均表明富堿斑巖來源于地幔(劉顯凡等,2010)。本區(qū)富堿斑巖微量分析也證實(shí)源于加厚的下地殼底部或“殼幔混合層”(鐘大賚等,2000),具有低Cr、低Ni,富集LILE、LREE,虧損HFSE、HREE的特征,特別是富集Ba、Rb、Th、K和虧損Nb、Ta、P、Ti等元素(徐受民等,2006);而代表著同期成礦流體的含礦斑巖內(nèi)石英斑晶流體包裹體,其與斑巖全巖具有一致的稀土配分模式,與礦體內(nèi)石英、方解石脈內(nèi)流體包裹體溫度、鹽度測定結(jié)果基本相同(肖曉牛等,2011),表明含礦質(zhì)流體與富堿斑巖同源,是富堿斑巖巖漿深部結(jié)晶分異產(chǎn)物或結(jié)晶分異后期殘余巖漿出溶產(chǎn)物(肖曉牛,2009),具有深部幔源特征。礦石內(nèi)黃鐵礦、黃銅礦、方鉛礦的34S值在-2.4~4.5‰,均值1.18‰,接近幔源硫的(34S值(0‰);而208Pb/204Pb、207Pb/204Pb、206Pb/204Pb分別變化在38.256~39.0394、15.457~15.703、18.380~18.587之間,與區(qū)域上富堿斑巖Pb同位素組成保持一致(肖曉牛等,2011)。再者,劉顯凡等通過對富堿斑巖、硅化石英、蝕變礦化斑巖、圍巖等進(jìn)行的34Si研究顯示,非礦化斑巖與次生石英34Si為0.0~0.4‰,而蝕變礦化斑巖及代表成礦流體的硅化石英(34Si為-0.1‰~-2.4‰,存在著明顯的原始地幔低負(fù)值特征,為成礦流體作用的結(jié)果(劉顯凡,2006;趙普峰等,2011)。以上均與本次輝鉬礦Re-Os同位素研究認(rèn)識相同,均指示成礦物質(zhì)為幔殼混合來源,以富硅的、不混溶含礦流體形式受一定程度的地殼混染或交代蝕變作用而于適當(dāng)部位成礦。

綜上,北衙金多金屬礦床及礦集區(qū)成礦是在構(gòu)造轉(zhuǎn)換時(shí)期(40~26Ma)出現(xiàn)的幕式應(yīng)力松弛、下地殼減薄的背景下,形成了大規(guī)模SN向馬鞍山深大斷裂及其次級斷裂構(gòu)造,以及近EW向隱伏基底斷裂;同時(shí),幔源區(qū)或下地殼發(fā)生減壓熔融,富硅、含礦質(zhì)流體與富堿巖漿于深部發(fā)生成份分異作用,呈不混溶狀沿同生斷裂上涌,并受地殼物質(zhì)混染或交代蝕變作用至淺表層次合適部位就位成礦;循環(huán)往復(fù),造就了始新世-漸新世(38~33Ma)時(shí)期大規(guī)模成礦作用的發(fā)生(鄧軍等,2011)。因此,北衙金多金屬成礦受構(gòu)造體制轉(zhuǎn)換階段的深部幔殼相互作用和淺表構(gòu)造、蝕變過程控制,并伴隨著富堿斑巖的就位,形成具代表性的超大型金多金屬礦床。

5 結(jié)論

(1) 通過對北衙金多金屬礦床萬硐山及紅泥塘礦段地表及鉆孔內(nèi)的5件輝鉬礦Re-Os同位素精確測年,得到模式年齡(37.46±0.57)~(39.44±0.79)Ma,加權(quán)平均年齡為38.48±0.54 Ma,等時(shí)線年齡為37.9±2.5 Ma,精確限定了本區(qū)金屬硫化物主成礦年齡,與富堿巖漿活動高峰期一致。

(2) 北衙金多金屬礦床內(nèi)輝鉬礦Re含量主體在26.84~43.15×10-6之間,與殼?;旌显磶r漿礦床的輝鉬礦Re含量相當(dāng);結(jié)合已有巖石、礦床地球化學(xué)研究成果,進(jìn)一步證明了該礦床成礦物質(zhì)來源為殼幔混合源。

(3) 北衙金多金屬礦床輝鉬礦Re-Os同位素研究也進(jìn)一步證實(shí),在構(gòu)造轉(zhuǎn)換時(shí)期,隨著下地殼減薄、深大斷裂及其次級斷裂的形成,幔源區(qū)或下地殼發(fā)生減壓熔融,且幔源流體或含礦質(zhì)流體與幔殼混合源巖漿發(fā)生成份分異作用,而呈不混溶狀沿同生斷裂上涌,并受地殼物質(zhì)混染或交代蝕變作用至淺表層次合適部位就位成礦。

致謝: 野外期間得到了云南黃金礦業(yè)集團(tuán)北衙項(xiàng)目部各位領(lǐng)導(dǎo)、同仁的大力支持和熱心幫助;輝鉬礦樣品測試得到了國家地質(zhì)測試中心屈文俊研究員和李超博士的幫助,在此表示由衷感謝!

[注釋]

① 云南黃金礦業(yè)集團(tuán)股份有限公司.2011.北衙鐵金礦區(qū)詳查報(bào)告[R]

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Re-Os Isotope Age of Molybdenite in the Beiya Au-Polymetallic Deposit, Western Yunnan Province and its Geological Implications

NIU Hao-bin1,HU Wen-yi2,DING Jun1,LI Jun1,NING Kuo-bu1,WANG Peng1,REN Fei1,DONG Li-yang1

(1.ChengduInstituteofGeologyandMineralResources,Chengdu,Sichuan610081; 2.Keyuan,SichuanEngineeringTechnicalTest,Chengdu,Sichuan610091)

The Beiya Au-polymetallic deposit lies in the alkali-rich porphyry polymetallic metallogenic belt of northwestern Yunnan Province. The deposit is well controlled by the alkali-rich porphyry and deep genetic faults, simultaneously developing thermal contact and contact metasomatic-hydrothermal alteration, where exist ore types of metasomatite and filling veins in the host rocks, forming a mineralization system of porphyry and skarn that is a super large-size Au-polymetallic deposit. This work firstly applied Re-Os isotopic dating technique to all ore sections. Five model ages of molybdenite obtained are from 37.46 Ma to 39.44 Ma, with the weighted average age 38.48±0.54 Ma and the isochron age 37.9±2.5 Ma, which are within the error range and consistent with the Zircon U-Pb ages of the alkali-rich porphyries in the area. The Re content of the molybdenite is mostly in the range 26.84×10-6to 43.15×10-6, suggesting that the metallogenic material originated from the upper mantle or lower crust, and should be a mixed source of the mantle and crust. Both of the results show that the gold polymetallic metallogeny was related to alkali-rich porphyry that was derived from the mixed source of the mantle and crust.

geochemistry, Re-Os isotopic dating, metallogenic age, geodynamic background, Beiya, western Yunnan

2014-06-25;

2014-08-21;[責(zé)任編輯]郝情情。

中國地質(zhì)調(diào)查局工作項(xiàng)目(編號:1212011220249)、12120113094500和12120114013501資助。

牛浩斌(1984年-),男,主要從事礦物學(xué)、巖石學(xué)、礦床學(xué)研究。E-mail:aibornew@126.com。

P597.3, P618.51

A

0495-5331(2015)01-0001-12

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