福建平和錦溪銅(鉬)礦床鋯石U-Pb和輝鉬礦Re-Os年齡及其地質(zhì)意義

潘天望,張 達*,倪建輝,陳泉流,袁 遠,狄永軍

(1.中國地質(zhì)大學 地質(zhì)過程與礦產(chǎn)資源國家重點實驗室,北京 100083;2.福建省地質(zhì)礦產(chǎn)勘查開發(fā)局 第八地質(zhì)大隊,福建龍巖 364012)

0 引 言

上杭-云霄火山噴發(fā)帶是福建省重要的多金屬成礦帶之一[1–2],在中生代存在大量的火山盆地以及相應(yīng)的侵入巖漿系統(tǒng),并形成了大量與之相關(guān)的礦床。上杭-云霄構(gòu)造巖漿成礦帶廣泛分布有銅、金、銀、鉬等金屬礦產(chǎn)及其他非金屬礦化和異常點,重要的礦化集中區(qū)包括閩西南上杭紫金山礦集區(qū)、閩中永定山口及大排礦集區(qū)、閩東平和及云霄一帶礦集區(qū)等。近年來前人對紫金山地區(qū)的礦床成因、構(gòu)造及巖漿作用特征以及成巖成礦關(guān)系等進行了大量的研究[3–12],認為紫金山銅金礦田屬于典型的高硫淺成低溫熱液型-中低溫熱液型-斑巖型成礦系統(tǒng)[3,4,6,13,14],該地區(qū)大規(guī)模的成礦作用主要與燕山晚期早白堊世(93～111 Ma)火山-侵入作用相關(guān),且形成于區(qū)域拉張伸展的構(gòu)造環(huán)境[3,5,11,15],如典型的羅卜嶺斑巖型銅(鉬)礦床輝鉬礦樣品 Re-Os同位素等時線年齡為(104.9±1.6) Ma[15],而與成礦關(guān)系密切的羅卜嶺花崗閃長斑巖 LA-ICP-MS鋯石 U-Pb諧和年齡為(103～105) Ma[16–17],成巖成礦時代基本一致。區(qū)域礦產(chǎn)地質(zhì)調(diào)查表明,位于上杭-云霄銅、金、鉬等多金屬成礦帶東端的平和地區(qū)也存在大量晚中生代火山盆地以及相關(guān)的侵入巖漿活動,局部可見與紫金山火山盆地相似的陸相火山機構(gòu)及明礬石次生石英巖化蝕變分帶[18–19]。由于與紫金山火山機構(gòu)處于同一構(gòu)造巖漿成礦帶上,因此平和一帶可能存在與“紫金山”式礦集區(qū)相類似的成巖成礦年代學記錄,也可能成為尋找“紫金山”式銅、金多金屬礦床新的重要找礦靶區(qū)。

平和錦溪銅(鉬)礦床位于NW向上杭-云霄構(gòu)造巖漿巖帶東南部的平和火山盆地內(nèi),并緊鄰鐘騰銅(鉬)礦床[20],為受構(gòu)造控制的中高溫熱液型礦床,銅(鉬)主要賦存于花崗閃長巖斷裂破碎帶中。上杭-云霄構(gòu)造巖漿巖帶上紫金山銅金礦田中四坊巖體的主要圍巖為燕山期的黑云母花崗巖,在巖體內(nèi)及其邊緣常分布有稍晚侵入的淺成斑巖體,如羅卜嶺和紫金山斑巖體,這些斑巖體與四坊巖體呈明顯的侵入接觸關(guān)系,是紫金山地區(qū)高硫淺成低溫熱液型-中低溫熱液型-斑巖型“三位一體”銅礦的主要成礦母巖[14]。錦溪花崗閃長巖體地質(zhì)特征與同屬上杭-云霄成礦帶上的四坊花崗閃長巖體相似,目前鉆孔資料顯示錦溪花崗閃長巖體內(nèi)及其邊緣也具有尋找斑巖體的潛力,且?guī)r體的主要圍巖為燕山期的黑云母花崗巖,這說明錦溪銅(鉬)礦床同樣具有尋找斑巖型銅(鉬)礦床的潛力。但由于其成礦時代及與之相關(guān)的巖體形成時代尚不清楚,一定程度上制約了礦床成因及其形成背景的認識,以及與紫金山礦田典型礦床的對比分析。為此,擬在野外考察的基礎(chǔ)上,對平和錦溪銅(鉬)礦床輝鉬礦及與成礦作用相關(guān)的花崗閃長巖分別開展 Re-Os同位素及鋯石 LA-ICP-MS U-Pb年代學研究,獲得礦區(qū)高精度成巖成礦年齡,在此基礎(chǔ)上,通過對比上杭-云霄成礦帶晚中生代銅、鉬等多金屬礦床成巖成礦時空分布特征,探討平和錦溪銅(鉬)礦床成因及其構(gòu)造背景。

1 地質(zhì)概況

上杭-云霄構(gòu)造巖漿帶位于華夏板塊的東南部,斜跨于不同的構(gòu)造單元上,自西向東分別為武夷山隆起、粵東閩西南坳陷、浙閩粵坳陷帶及東南沿海斷隆帶,崇安-石城、政和-大埔、長樂-南澳斷裂分別在該帶西側(cè)、中部和東部通過[2](圖 1a)。上杭-云霄斷裂帶主要活動期在早白堊世[1,3],且對燕山晚期巖漿活動及其成礦具有明顯的控制作用[22],其中與北東向構(gòu)造交匯處對成礦尤為有利。兩組斷裂構(gòu)造的復合部位不僅控制著燕山期的巖漿活動,而且次級斷裂及韌性剪切帶往往是后期成礦的有利賦存空間,如紫金山礦集區(qū)、永定山口礦集區(qū)以及平和鐘騰礦集區(qū)等都賦存于該斷裂與北東向各個斷裂交匯處或附近。平和錦溪銅(鉬)礦床位于東南部的平和縣境內(nèi),構(gòu)造上位于華夏板塊閩東燕山期陸內(nèi)造山帶西南部福安-南靖(北東向)深斷裂與上杭-云霄(北西向)深斷裂交匯部位,閩東火山活動亞帶與上杭-云霄火山噴發(fā)亞帶交匯處的東南部。成礦上處于上杭-云霄成礦帶東南段,并緊鄰鐘騰銅(鉬)礦床,表現(xiàn)出良好的成礦地質(zhì)條件(圖1b)。

平和地區(qū)出露地層以侏羅系陸相火山噴發(fā)-沉積巖系為主,主要有下侏羅統(tǒng)梨山組(J1l)內(nèi)陸盆地碎屑巖、細粒砂巖,侏羅系中統(tǒng)長林組(J2c)中細粒石英砂巖、粉砂巖,上侏羅統(tǒng)南園組(J3n)中酸性火山噴發(fā)巖,以及第四系(Q)沖洪積層。區(qū)域構(gòu)造活動十分強烈,以NE向和近EW向構(gòu)造為主。其中近EW向斷裂規(guī)模最大,生成最早,控制鐘騰巖體和平和巖體的產(chǎn)出以及礦化蝕變帶、物化探異常的分布1)中化地質(zhì)礦山總局福建地質(zhì)勘查院,福建省平和縣錦溪礦區(qū)銅礦詳查地質(zhì)報告,2007。;NE向斷裂構(gòu)造形跡清晰,規(guī)模較大,控制著侵入巖、火山巖、礦化蝕變帶和物化探異常的展布,是錦溪礦區(qū)最主要的導礦和容礦構(gòu)造。平和地區(qū)主要出露燕山晚期的平和巖體與鐘騰巖體,呈小巖株狀分別展布于研究區(qū)的東、西部(圖1)。兩巖體均為復式巖體,前者主要由花崗閃長巖、石英閃長巖、(含)黑云母花崗巖組成,后者主要由石英閃長巖和花崗閃長巖等組成。兩者均與Cu、Mo等多金屬成礦關(guān)系較密切。此外,尚有后期侵入的石英斑巖、花崗斑巖等中酸性脈巖。

圖1 福建上杭-云霄成礦帶區(qū)域地質(zhì)簡圖(a)(成礦帶的劃分據(jù)文獻[2]修編;侵入巖的劃分據(jù)文獻[21]修編)及錦溪銅(鉬)礦區(qū)域地質(zhì)簡圖(b)Fig.1 Regional geological map of the Shanghang-Yunxiao mineralization belt(a) and tectonic location of the Jinxi copper(molybdenum) deposit(b)

2 礦床地質(zhì)特征

2.1 礦區(qū)地質(zhì)

錦溪銅(鉬)礦床礦區(qū)除第四系洪積層外,其他地層均未見出露。第四紀洪積層主要分布于礦區(qū)西北部,堆積物由灰-灰黃色黏土、砂質(zhì)黏土、粗砂及砂礫卵石等組成(圖2)。

礦區(qū)主要出露燕山晚期花崗閃長巖,其次為黑云母花崗巖,兩者均為平和復合巖體的組成部分,此外尚有晚期零星侵入的花崗斑巖脈。錦溪花崗閃長巖體在礦區(qū)大面積分布,且?guī)r體的主要圍巖為黑云母花崗巖,黑云母花崗巖時代不明,兩者接觸界線呈漸變關(guān)系,花崗斑巖脈呈透鏡狀侵入于礦區(qū)北部及北東部的花崗閃長巖中1)。錦溪銅(鉬)礦床銅礦化與錦溪花崗閃長巖關(guān)系緊密,而鉬礦化與花崗閃長巖及黑云母花崗巖關(guān)系緊密?；◢忛W長巖體底下、黑云母花崗巖體內(nèi)和邊緣鉬礦化規(guī)模較大,而同樣部位均未見銅礦化,表明黑云母花崗巖可能與銅礦成礦無關(guān)。目前黑云母花崗巖及相關(guān)的輝鉬礦測年工作正在進行中。

礦區(qū)斷裂構(gòu)造以NE向為主,其次為NW向(F5)和近SN向(F4)以及NNE向(F6)。NE向斷裂帶斜貫全區(qū)(F1–3),是區(qū)內(nèi)主要的導礦和容礦構(gòu)造。NW 向和近 SN向斷層形成時間最晚,切割 NE向斷裂帶,剪節(jié)理發(fā)育,常見石英脈充填,地表多為鐵錳質(zhì)充填,顯示正斷層性質(zhì)。

2.2 礦體特征

錦溪銅(鉬)礦體主要賦存于北東向斷裂破碎帶中,容礦圍巖為錦溪花崗閃長巖。礦體形態(tài)、產(chǎn)狀及規(guī)模主要受NE向F1、F2和F3斷層控制(圖3),已探明鉬礦儲量有望達到中型規(guī)模,銅礦儲量為小型規(guī)模。錦溪礦區(qū)目前共圈定15個礦體,其中銅礦體6個,鉬礦體 9個。銅礦體走向長 65～586 m,厚度2.33～15.55 m;鉬礦體走向長 65～230 m,厚度1.18～8.39 m,各礦體形態(tài)在平面和剖面上均呈脈狀或透鏡狀產(chǎn)出1)。鉬礦體基本分布在銅礦體的上部,主要集中于 F1～F2斷層構(gòu)造破碎帶之間。近礦圍巖和礦體頂板、底板均為礦化、蝕變花崗閃長巖。礦體與頂板、底板接觸界線不清,多為漸變關(guān)系。

2.3 礦石類型及特征

根據(jù)肉眼識辨及物相分析,錦溪礦區(qū)礦石的自然類型以硫化物礦為主。礦石金屬礦物以黃鐵礦、黃銅礦、輝鉬礦為主,次為磁鐵礦、磁黃鐵礦,極少量輝銅礦,偶見閃鋅礦、方鉛礦等;輝鉬礦和黃銅礦集合體常呈細脈狀或星點浸染狀等產(chǎn)于次生石英、鉀長石、黑云母和磁鐵礦等礦物的粒間,輝鉬礦常被黃銅礦細脈切穿或被黃銅礦、黃鐵礦所溶蝕,代表錦溪銅(鉬)礦床至少有兩階段成礦作用(圖4a和4b)。

礦石結(jié)構(gòu)多樣,主要為他形粒狀鑲嵌結(jié)構(gòu),其次為半自形-他形粒狀鑲嵌結(jié)構(gòu),少量自形-半自形他形粒狀結(jié)構(gòu)等;礦石構(gòu)造以不均勻稀疏細脈浸染狀構(gòu)造為主,浸染狀、細脈條帶狀構(gòu)造次之,少量致密塊狀構(gòu)造。脈石礦物以斜長石、鉀長石、石英為主,其次為綠泥石、絹云母、方解石等。

2.4 蝕變類型

礦區(qū)蝕變發(fā)育,且明顯受構(gòu)造控制,構(gòu)造節(jié)理愈發(fā)育,蝕變作用愈強烈,蝕變礦物多沿裂隙充填交代呈脈狀產(chǎn)出,根據(jù)蝕變礦物組合與分布特征,蝕變具有分帶性,大致可分為上、下兩個帶。上帶以硅化為主,伴有絹云母化、鉀長石化、磁鐵礦化、黃鐵礦化等,多呈脈狀與輝鉬礦體相伴生;下帶以鉀長石化為主,伴有硅化、綠泥石化、絹云母化等,往往與黃銅礦體相伴生1)中化地質(zhì)礦山總局福建地質(zhì)勘查院,福建省平和縣錦溪礦區(qū)銅礦詳查地質(zhì)報告,2007。。近礦圍巖蝕變主要為黃鐵礦化、鉀化、硅化和綠泥石化。

3 樣品的采集及測試結(jié)果

3.1 樣品采集及分析方法

本次研究鋯石單礦物樣品選自礦區(qū) 28號勘探線平硐內(nèi)的花崗閃長巖中,巖石樣品新鮮,蝕變污染少。錦溪花崗閃長巖呈灰色或暗灰色,以中細粒花崗結(jié)構(gòu)(粒徑 1～4.5 mm)、塊狀構(gòu)造為主,未見顯微文象結(jié)構(gòu)和晶洞構(gòu)造(圖4c和4d)。組成礦物以斜長石(25.1%～42.9%,An=30～50)和石英(20%～23%)為主,并含有一定量鉀長石,總量在 18.5%～35.5%之間,鐵鎂礦物主要為少量黑云母(7%～8%)和普通角閃石(5%～7%),角閃石多與黑云母共生,未出現(xiàn)堿性鐵鎂礦物;副礦物組合中普遍出現(xiàn)榍石而未見富鋁礦物,以富含F(xiàn)e、Ti、Ca成分的副礦物為特征。

圖2 錦溪銅(鉬)礦礦床地質(zhì)簡圖1) 福建省閩東南地質(zhì)大隊,福建省平和縣鐘騰礦區(qū)深部查證報告,1990。Fig.2 Geological map of the Jinxi copper(molybdenum) deposit

圖3 錦溪礦區(qū)16號勘探線剖面圖示意圖Fig.3 A–B section of the Jinxi mining area

圖4 錦溪礦床測試巖體及礦石樣品照片巖相學特征Fig.4 Photographs showing ore samples and petrographical characteristics of the Jinxi deposit

在 22號勘探線平硐內(nèi)選取一件輝鉬礦含量充足的樣品(X22-b2)進行輝鉬礦 Re-Os同位素模式年齡研究,礦石中輝鉬礦呈鉛灰色,半自形葉片狀或不規(guī)則粒狀集合體,粒徑在0.5～15.0 mm之間,集合體呈脈狀分布于次生石英顆粒間,基本與硅化同時或稍晚晶出,晚期含Cu黃鐵礦化脈將早期含Mo硅化脈所截切,礦脈輝中鉬礦被黃銅礦和黃鐵礦所溶蝕(圖4a和4b),這些特征表明黃銅礦和黃鐵礦形成的時代要比輝鉬礦稍晚。

鋯石與輝鉬礦的分選由河北省廊坊市地科勘探技術(shù)服務(wù)有限公司完成。鋯石樣品的挑選、制靶和陰極發(fā)光(CL)成像在北京鋯石領(lǐng)航科技有限公司實驗室完成。挑選出的輝鉬礦質(zhì)純,無包體,無污染且純度達98%以上。鋯石U-Pb測年分析在天津礦產(chǎn)研究所實驗室利用LA-ICP-MS方法完成,具體測試原理及儀器配置和實驗流程詳見文獻[23–24]。采用Andersen[23]方法對普通Pb進行校正。采用TE-MORA作為外部鋯石年齡標準,數(shù)據(jù)處理采用 ICP-MS Data Cal 4.3程序[25],加權(quán)平均年齡計算及處理采用Isoplot軟件完成[26]。利用NIST612玻璃標樣作為外標計算鋯石樣品的Pb、U、Th含量。測試結(jié)果見表1。

由于地球樣品自約0.8 Ga以來放射性衰變引起的207Pb/235U比值的增幅較小,年輕鋯石的207Pb豐度較低而難以測量,并且由于該類鋯石中常含有低的、不等量的普通 Pb,這就使得年輕鋯石在常規(guī)的206Pb/238U-207Pb/235U 諧和曲線上常常出現(xiàn)偏離諧和線的情況[27],造成這種常規(guī)的諧和曲線難以判斷諧和年齡與存在不同放射成因 Pb丟失年齡之間的區(qū)別[28],且目前 LA-ICP-MS方法尚無法準確獲得204Pb的含量,因此,為了評價207Pb/206Pb組成和普通 Pb的相對比例[29],同位素年齡的確定使用 Tera-Wasserburg諧和圖解[30],圖解的橫坐標和縱坐標分別為238U/206Pb和207Pb/206Pb,將所有測試結(jié)果不進行普通Pb扣除而直接投圖,形成一條不一致線,不一致線與諧和線的下交點即代表樣品的形成年齡,圖解的生成及處理亦采用Isoplot軟件完成。

3.2 鋯石U-Pb年代學

對錦溪花崗閃長巖體選取 2件代表性樣品,進行LA-ICP-MS鋯石U-Pb測年。所選鋯石呈自形長柱狀或短柱狀,粒徑一般在 80～200 μm 之間,長寬為 1∶1～3∶1之間(圖 5)。CL圖像顯示大部分鋯石內(nèi)部可見較清晰的韻律環(huán)帶和條帶結(jié)構(gòu),表現(xiàn)出典型巖漿鋯石特征。少量鋯石具有繼承鋯石的核,鋯石內(nèi)部顯示其核部震蕩環(huán)帶較寬,呈現(xiàn)亮白色-灰白色,而邊部呈暗灰色,振蕩環(huán)帶較窄而密,是巖漿鋯石早期處于高溫下結(jié)晶而成的[31]。在分析過程中,避開裂隙和包裹體發(fā)育的鋯石或微區(qū),選擇環(huán)帶發(fā)育的鋯石邊部打點,兩件樣品鋯石U、Th、Pb同位素成分數(shù)據(jù)及諧和年齡見表1。

LA-ICP-MS 鋯石 U-Pb同位素測年結(jié)果顯示,可能受到蛻晶化作用的影響[32],兩個花崗閃長巖樣品大部分測點都偏離協(xié)和線。樣品JX28-b1中除了2個測點(測點 7和測點 8)顯示較大的鋯石206Pb/238U年齡(126±1) Ma和(138±2) Ma,其余17個測點則顯示了較為一致的206Pb/238U年齡(104～114 Ma)。19個鋯石測試點在 Tera-Wasserburg圖解中給出了(104.5±1.0) Ma(MSWD=1.8)的下交點年齡(圖 6a)。樣品JX14-b2的Tera-Wasserburg圖解顯示,17個測試點中除了測試點 10顯示出較高206Pb /238U年齡((122±2) Ma)外,剩余16個測點206Pb/238U年齡集中于107～112 Ma之間,所有測試點在Tera-Wasserburg圖解中給出了(106.8±0.8) Ma(MSWD=0.89)的下交點年齡(圖6b)。

上述兩件樣品鋯石 Th/U比值變化于0.32～0.59(Th/U ＞ 0.1)之間,表明了鋯石為典型的巖漿鋯石[33]。由于錦溪花崗閃長巖體形成時代較新,且鋯石樣品中常含有低的、不等量的普通Pb,因此兩個花崗閃長巖均未能獲得206Pb/238U加權(quán)平均年齡,但2件樣品下交點年齡代表了錦溪花崗閃長巖體的侵入年齡,表明該巖體形成于105～107 Ma之間。

圖5 錦溪礦床錦溪花崗閃長巖部分鋯石陰極發(fā)光圖Fig.5 Cathodoluminescence(CL) images of some zircons from the Jinxi granodiorite in the Jinxi deposit

圖6 錦溪花崗閃長巖中鋯石LA-ICP-MS U-Pb定年結(jié)果Fig.6 LA-ICP-MS U-Pb ages of zircon from the Jinxi granodiorite

3.3 輝鉬礦Re-Os測定

輝鉬礦單礦物的挑選在室內(nèi)無污染環(huán)境下進行,挑選出符合測試要求的輝鉬礦,Re-Os同位素年齡測試由中國地質(zhì)科學院國家地質(zhì)實驗測試中心完成,采用電感耦合等離子質(zhì)譜儀TJA X-erie ICP-MS進行測量,樣品的化學處理流程和分析方法見文獻[34–35],模式年齡t按以下式計算:

式中:λ(187Re 衰變常數(shù))=1.666×10–11a–1。

本次工作在錦溪礦區(qū)22號勘探線平硐內(nèi)選取1件具有代表性且含量充足的輝鉬礦樣品(JX22-b2)進行樣品的Re-Os同位素測試,結(jié)果表明輝鉬礦的模式年齡為(105.7±1.7) Ma。輝鉬礦的Re含量為2.058 μg/g,187Re含量為 1.576 μg/g,187Os含量為2.778 ng/g,而普Os含量為0.001 ng/g(表2),遠低于樣品的187Os含量,反映出187Os都是187Re的衰變產(chǎn)物,符合計算模式年齡的條件,也說明所獲得的模式年齡是有效的。

4 討 論

4.1 成巖成礦時代約束

本文獲得的錦溪花崗閃長巖 LA-ICP-MS鋯石U-Pb年齡在105～107 Ma之間,代表了錦溪花崗閃長巖的侵位年齡區(qū)間。閩西南紫金山盆地白堊世(94～128 Ma)火山-侵入巖分布主要受NW向上杭-云霄深斷裂的控制[3],平和火山盆地與之相似,所以該地區(qū)近年來成為尋找“紫金山式”銅金礦床的重點區(qū)域[18–19]。平和錦溪銅(鉬)礦床與羅卜嶺斑巖型銅(鉬)礦床同屬NW向上杭-云霄銅、金、鉬等多金屬成礦帶,鉬礦床的成礦年齡((105.7±1.7) Ma)與羅卜嶺銅(鉬)礦床((104.9±1.6) Ma)以及相鄰鐘騰斑巖型銅(鉬)礦床((109.0 ± 2.8) Ma)(輝鉬礦 Re-Os)[36]的成礦年齡在誤差范圍內(nèi)較為一致,錦溪花崗閃長巖的侵位年齡(105～107 Ma)與四坊花崗閃長巖的侵位年齡(鋯石 U-Pb 年齡,104～107 Ma)[14,37]近乎一致,且與四坊巖體呈明顯的侵入接觸關(guān)系的羅卜嶺花崗閃長斑巖的侵位年齡(103～105 Ma)亦非常接近,同時羅卜嶺花崗閃長斑巖是“羅卜嶺”式斑巖型銅(鉬)多金屬礦床的成礦母巖。因此,平和錦溪地區(qū)也可能為尋找斑巖型銅(鉬)多金屬礦床新的找礦靶區(qū)。

輝鉬礦封閉溫度較高(約 500 ℃),冷卻速度較慢的且不易受后期蝕變和構(gòu)造事件的影響[38]。因此,對礦石中分離出的輝鉬礦進行Re-Os同位素定年是目前確定成礦時代的最好方法,輝鉬礦的 Re-Os同位素定年結(jié)果也是精確厘定礦床成礦時代的最好證據(jù)[39–40]。本次工作在錦溪礦區(qū)22號勘探線平硐內(nèi)獲得的含輝鉬礦石樣品(JX22-b2)中,含輝鉬礦硅化脈常被含黃銅礦細脈切穿,輝鉬礦常被黃銅礦、黃鐵礦所溶蝕,代表錦溪銅(鉬)礦床至少存在兩階段成礦作用,銅礦的形成普遍比輝鉬礦要略晚。本文首次對樣品中的輝鉬礦進行 Re-Os同位素定年,獲得輝鉬礦Re-Os同位素模式年齡為(105.7±1.7) Ma,該年齡與銅(鉬)礦含礦圍巖錦溪花崗閃長巖的侵位年齡(105～107 Ma)在誤差范圍內(nèi)基本一致,因此認為該礦床鉬礦成礦年齡在105～107 Ma年之間。

4.2 成礦物質(zhì)來源

Re-Os同位素體系不但可以精確測定硫化物礦床的成礦時代,而且金屬硫化物礦床中輝鉬礦Re含量對成礦物質(zhì)來源有一定的示蹤作用[41–43]。Maoet al.[44–45]通過對中國各種成因類型鉬礦床中輝鉬礦Re含量統(tǒng)計與分析后指出,從幔源到殼幔混源再到殼源,輝鉬礦中的Re含量從n×10～n×103μg/g →n×10 μg/g →nμg/g呈數(shù)量級逐次降低。此次測得的錦溪銅(鉬)礦床中輝鉬礦187Re為(1.576 ± 0.011) μg/g,相當于殼源巖漿礦床的Re含量,指示錦溪銅(鉬)礦床的鉬礦成礦物質(zhì)來源以殼源為主。

4.3 成巖地質(zhì)意義

華南中生代大規(guī)模構(gòu)造巖漿作用被認為與特提斯構(gòu)造域向環(huán)太平洋構(gòu)造域的轉(zhuǎn)換有關(guān)[46–48]。已有研究表明,華南在中生代至少存在 3期擠壓構(gòu)造運動,印支期擠壓構(gòu)造變形表現(xiàn)為近東西向褶皺和北東向斷裂發(fā)生右旋走滑運動(239～230) Ma[49],造成了早-中三疊世與晚三疊世的不整合[50–51],這指示華南早中生代遭受南北向擠壓作用,其動力來源為印支陸塊與華南陸塊南緣之間發(fā)生的碰撞以及華北陸塊與華南陸塊北緣之間的碰撞[52–53],而晚三疊世以后,受古太平洋板塊北西向俯沖影響,中國東部大陸邊緣逐漸成為活動大陸邊緣[54–58];175～150 Ma是古太平洋板塊斜向俯沖占主導的陸內(nèi)造山時期[59–60],而特提斯構(gòu)造體系向環(huán)太平洋活動邊緣構(gòu)造體系轉(zhuǎn)換的開始時間約為(165±5) Ma[61],這一時期古太平洋板塊向歐亞板塊俯沖,表現(xiàn)為大規(guī)模陸內(nèi)擠壓,在中侏羅世(169～161 Ma)擠壓達到高潮,中國東南部發(fā)育了大規(guī)模的S型過鋁一弱過鋁質(zhì)花崗巖和二長花崗巖[62],晚期高分異巖株顯示出鋁質(zhì)A型花崗巖的地球化學特征,例如閩西南地區(qū)以帶內(nèi)雙峰式火山巖、拉斑質(zhì)玄武巖和同時代A型-I型花崗巖、橄欖輝長巖為特征[63],其中以湯泉富鈉埃達克質(zhì)花崗閃長巖(157 Ma)[64]和高Sr初始值S型花崗巖(才溪巖體和紫金山巖體(164～150 Ma)[5,37,65]為代表,這類花崗巖形成對應(yīng)于古太平洋俯沖所導致的活動大陸邊緣環(huán)境,同時表明在164～155 Ma時期,古太平洋板塊可能俯沖到紫金山地區(qū)[66];在150～100 Ma,中國東南部在古太平洋動力學體系的影響下,造成沿海地區(qū)拉張伸展,巖石圈減薄,地幔上隆,地幔來源玄武巖質(zhì)巖漿底侵[67–72],并使下部地殼部分熔融形成花崗質(zhì)巖漿,形成了中國東南部地質(zhì)歷史上規(guī)模最大的花崗質(zhì)火山-侵入雜巖[59,67,73,74]。紫金山地區(qū)的四坊花崗閃長巖體、羅卜嶺花崗閃長斑巖體、浸銅湖石英正長斑巖體即形成于這種拉張伸展構(gòu)造背景之下[14–15]。

表2 錦溪礦床輝鉬礦Re-Os同位素年齡測試結(jié)果Table 2 Re-Os isotopic results of the molybdenite form the Jinxi deposit

綜合以上研究成果,錦溪花崗閃長巖體不但與四坊花崗閃長巖體和羅卜嶺巖花崗閃長斑體成巖成礦年齡基本一致,而且這些巖體的分布主要受 NW向上杭-云霄構(gòu)造巖漿巖帶控制。因此,本文推測平和錦溪花崗閃長巖體可能與紫金山四坊巖體和羅卜嶺巖體一樣形成于拉張伸展構(gòu)造背景之下。

4.4 成礦地質(zhì)意義

東南沿海成礦帶構(gòu)造-巖漿活動以及相應(yīng)的成礦作用與華夏古陸的形成演化、特提斯向環(huán)太平洋構(gòu)造成礦域的轉(zhuǎn)換及中新生代中國東部大陸邊緣構(gòu)造活動關(guān)系密切[47,48,61]。NW 向上杭-云霄成礦帶作為東南沿海成礦帶的重要組成部分,成礦作用時代的分布與區(qū)域構(gòu)造演化、巖漿作用、沉積作用及變質(zhì)作用有關(guān)(表3),不同類型礦床的分布格局是該成礦帶長期構(gòu)造巖漿成礦演化的結(jié)果。上杭-云霄成礦帶中生代成礦作用積極響應(yīng)了中侏羅世(175±5 Ma)以來華夏古陸地質(zhì)作用的全過程,但仍以燕山期成礦作用占主導地位,目前還未發(fā)現(xiàn)印支期前(包括印支期)相應(yīng)的巖漿-成礦活動。

在(175±5) Ma,古太平洋板塊向歐亞大陸斜向俯沖已占主導[52,59,60],引發(fā)路塊間的強烈擠壓,華南發(fā)生了大規(guī)?；◢徺|(zhì)巖漿-成礦活動(170～150 Ma)[54,55,75],作為華南陸塊重要組成部分之一的華夏地塊也一起轉(zhuǎn)入古太平洋斜向俯沖占主導的陸內(nèi)造山體系,處于華夏地塊西南緣上杭-云霄成礦帶也有相應(yīng)的巖漿-成礦活動。以永定山口鉬礦床為例,其輝鉬礦樣品Re-Os同位素等時線年齡為(165.3±3.5) Ma[76],才溪巖體和紫金山巖體的成巖年齡在(164～150 Ma)之間[5,37,65];晚侏羅世(約150 Ma)以后,中國東南大陸在古太平洋板塊斜向俯沖構(gòu)造背景下,受到華南陸內(nèi)多塊體之間從擠壓到伸張一系列構(gòu)造運動以及深斷裂再活化影響,發(fā)生大規(guī)模陸內(nèi)火山-侵入活動,其中 135 Ma是個重要的由擠壓向伸展的轉(zhuǎn)換時間[57,77,78]。該時期NW向上杭-云霄深斷裂再次活化,形成了武平十二排為代表巖漿-熱液型鉬礦床,其輝鉬礦樣品 Re-Os同位素等時線年齡出現(xiàn)(150.8±1.3) Ma[22]和(143.9± 2.1) Ma[79]兩期成礦年齡,與成礦關(guān)系密切的武平十二排巖體晚期黑云母花崗巖鋯石 U-Pb諧和年齡為(143.47±0.42)Ma[79],同時紫金山礦田在該時期則發(fā)生了金龍橋巖體細?；◢弾r和五龍寺巖體中細?；◢弾r(SHRIMP鋯石 U-Pb年齡均為(149±2) Ma[65])的侵入活動。

早白堊世(135 Ma)以后中國東南大陸邊緣進入了拉張伸展階段,形成了一系列北西向的橫張斷裂和斷陷盆地[80],同時出現(xiàn)大規(guī)模的巖漿作用與伸展空間而成礦,在 130 Ma左右,北西向上杭-云霄大斷裂也從擠壓向伸展機制轉(zhuǎn)變[81],該斷裂再次活化誘發(fā)深部中酸性巖漿向上運移,形成廣泛的燕山晚期花崗巖和次火山巖。侵入的花崗巖以含幔源物質(zhì)較少且為殼源型為主要特征。多階段侵入的花崗巖不但為成礦提供了充足的熱源、流體來源及絕大部分的鐵質(zhì)來源,而且大量含礦流體進入早期沉積的富含F(xiàn)e、Cu、Mo、Pb、Zn的一套碎屑巖和碳酸鹽巖之間的層間斷裂,并發(fā)生了強烈的夕卡巖化交代作用,形成層控夕卡巖型鐵、鉛、鋅、鉬礦床,如永定火山盆地中大排鐵多金屬礦床((133±2) Ma,輝鉬礦Re-Os同位素等時線年齡)以及相應(yīng)的大排礦區(qū)成礦相關(guān)的似斑狀花崗巖(132.7～132.5 Ma,鋯石 U-Pb法諧和年齡)[82],盆地外圍的大洋-莒州巖體(LAMC-ICPMS鋯石U-Pb年齡為136～125 Ma)正是在擠壓向伸展轉(zhuǎn)變的構(gòu)造背景下(約135 Ma)形成的[82–83];約125 Ma以后,中國東部轉(zhuǎn)入了太平洋板塊正向俯沖構(gòu)造體系[67,69,84–86],其中太平洋板塊俯沖方向、俯沖速率、俯沖角度等的變化可能是東南沿海地區(qū)能形成晚中生代寬廣火山-侵入巖帶的重要動力學原因[69,87–89]。該時期中國東南部擠壓構(gòu)造的表現(xiàn)形式以下白堊統(tǒng)地層翹傾和長樂-南澳大型左旋走滑韌性剪切帶的形成(121～117 Ma)[58]為代表,而東南沿海結(jié)合帶的上火山巖系和寧鎮(zhèn)山脈則有從擠壓到伸展構(gòu)造的巖漿巖記錄[89],該階段紫金山地區(qū)發(fā)生較大規(guī)模早白堊世火山噴發(fā)與巖漿超淺層就位,形成石帽山群下段的英安玢巖及紫金山次火山巖(全巖Rb-Sr等時線年齡為(125～118 Ma)[3,90],平和長崎后地區(qū)也有Pb-Zn礦床的成礦記錄(Pb-Pb同位素年齡為133 Ma)[2]。

表3 福建上杭-云霄成礦帶部分礦床和巖體同位素年齡Table 3 Isotopic ages of some igneous rocks and related ore deposits in the Shanghang-Yunxiao mineralization belt,Fujian Province

早白堊世晚期(約 105 Ma),沿一系列北西向的斷裂帶和斷陷盆地內(nèi)的較大規(guī)模的陸相火山噴發(fā)和巖漿-成礦活動,標志著 105 Ma左右華夏板塊已全面處于伸展構(gòu)造環(huán)境[91],此時NW向上杭-云霄深斷裂廣泛分布的基性巖墻群說明該斷裂一定程度的聯(lián)通或該斷裂連接了古俯沖帶或(和)古拼接帶等板塊邊界構(gòu)造,而沿深斷裂上升侵入的新生鈣堿性花崗閃長巖-花崗閃長斑巖漿因則繼承了早先形成的與俯沖或和碰撞有關(guān)的幔源物質(zhì)[92],地幔組分逐漸增多,形成了諸如閩西南四坊巖體(104～107 Ma)、羅卜嶺巖體(103～105 Ma)和悅洋花崗閃長斑巖體((105.0±7.2) Ma)等,以及各盆地典型火山機構(gòu)中的英安玢巖(如紫金山英安玢巖鋯石 U-Pb法年齡為(105.0±0.7) Ma)、隱爆角礫巖和凝灰熔巖(如包圍山凝灰熔巖((104.6±1.1) Ma))等。在巖漿活動過程中,巖漿氣液所攜帶的成礦物質(zhì)沿次火山通道、NW 向構(gòu)造帶向淺部遷移,在接觸帶、隱爆角礫巖帶、裂隙帶等有利的位置沉淀成礦,形成了以平和包圍山鉬礦床((95.2±1.5) Ma)等受火山機構(gòu)控制為代表的火山熱液型鉬礦床,以及紫金山礦田中一套典型的斑巖型-高硫淺成低溫熱液型成礦系統(tǒng)。同時平和火山盆地以錦溪花崗閃長巖(105～107 Ma)、鐘騰花崗閃長斑巖(101.9 Ma)等為代表的成礦母巖就位,形成以錦溪中高溫熱液脈型銅(鉬)礦床((105.7± 1.7) Ma)和鐘騰斑巖型銅(鉬)礦床((109.0±2.8) Ma)等為代表的礦床。隨后92 Ma左右東南大陸巖石圈則進入伸展-地殼減薄(伸展作用加強)階段[91,93],該時期上杭-云霄深斷裂中火山再度活化,發(fā)生較大規(guī)模的陸相火山噴發(fā)和巖漿-成礦活動,形成以紫金山盆地中悅洋低硫型銀多金屬礦床(冰長石40Ar-39Ar年齡為((91.5±0.4)～(94.7±2.3) Ma)[94]以及浸銅湖斑巖型銅鉬礦床(含礦圍巖石英閃長斑巖(LA-MC-ICPMS鋯石U-Pb年齡為(95.3±0.9) Ma 和(96.7±0.9) Ma)[15]等為代表的礦床,同時形成紫金山石帽山群流紋巖(SHRIMP鋯石U-Pb年齡為(94.0±7.7) Ma)[65]、石英斑巖和花崗斑巖(SHRIMP鋯石U-Pb年齡分別為((96±2) Ma和(93±2) Ma[65])等無礦次火山巖脈。

綜合以上研究資料成果,受古太平洋構(gòu)板塊俯沖作用影響,上杭-云霄構(gòu)造巖漿成礦帶構(gòu)造環(huán)境經(jīng)歷了170～150 Ma持續(xù)擠壓階段、150～125 Ma擠壓向伸展轉(zhuǎn)換階段、125～92 Ma持續(xù)伸展階段以及隨后92 Ma左右伸展作用加強階段過程。早白堊世晚期-晚白堊世早期(125～92 Ma)東南沿海地區(qū)在古太平洋板塊俯沖作用機制影響下,巖石圈拉張伸展構(gòu)造背景下下地殼部分熔融所誘發(fā)NW向上杭-云霄深斷裂發(fā)生的構(gòu)造-巖漿-成礦事件是導致錦溪銅(鉬)礦床和錦溪花崗閃長巖體形成的主導因素。錦溪銅(鉬)礦床與紫金山羅卜嶺銅(鉬)礦床同處于上杭-云霄構(gòu)造巖漿成礦帶上,與羅卜嶺銅(鉬)礦床形成背景相似,兩者相關(guān)巖漿-成礦活動年齡非常相近。因此錦溪地區(qū)可能為尋找“羅卜嶺”式銅、金多金屬礦床新的重要找礦靶區(qū),具有尋找斑巖型銅(鉬)礦床的潛力。

5 結(jié) 論

鋯石 LA-ICP-MS U-Pb定年結(jié)果表明,錦溪花崗閃長巖體成巖年齡為105～107 Ma;通過對礦體中輝鉬礦的 Re-Os同位素年齡分析,獲得其模式年齡為(105.7±1.7) Ma,與巖體成巖年齡非常相近。礦體中輝鉬礦的Re含量指示鉬礦成礦物質(zhì)來源于地殼。研究結(jié)果指示錦溪銅(鉬)礦床在早白堊世晚期至少存在2個階段較大規(guī)模的成礦作用。根據(jù)錦溪銅(鉬)礦床輝鉬礦 Re-Os同位素年齡和成礦圍巖鋯石LA-ICP-MS U-Pb定年結(jié)果,結(jié)合中生代上杭-云霄成礦帶成巖成礦的大地構(gòu)造背景,認為早白堊世中-晚期(125～92 Ma)東南沿海地區(qū)在古太平洋板塊俯沖作用機制影響下,巖石圈拉張伸展構(gòu)造背景之下導致下地殼部分熔融所誘發(fā)上杭-云霄構(gòu)造巖漿帶發(fā)生的構(gòu)造-巖漿-成礦事件是導致錦溪銅(鉬)礦床和錦溪花崗閃長巖體形成的主導因素。

輝鉬礦樣品測試得到了國家地質(zhì)實驗測試中心屈文俊研究員和李超博士的幫助;鋯石 U-Pb測年實驗過程中得到了天津地質(zhì)礦產(chǎn)研究所袁海帆老師的熱情幫助;匿名審稿人的建設(shè)性意見對完善本文很有價值,在此謹致感謝！

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