湖南黃金洞金礦床白鎢礦Sm-Nd年齡及其地質意義

周岳強, 董國軍, 許德如, 鄧 騰, 吳 俊, 王 翔, 高 磊, 陳孝剛

湖南黃金洞金礦床白鎢礦Sm-Nd年齡及其地質意義

周岳強1,2,3, 董國軍3*, 許德如1,4, 鄧 騰4, 吳 俊3, 王 翔3, 高 磊5, 陳孝剛5

(1. 中國科學院 廣州地球化學研究所 礦物學與成礦學重點實驗室, 廣東 廣州 510640; 2. 中國科學院大學, 北京 100049; 3. 湖南省 地質礦產勘查開發局 四〇二隊, 湖南 長沙 410004; 4. 東華理工大學 核資源與環境國家重點實驗室, 江西 南昌 330013; 5. 湖南黃金洞礦業有限責任公司, 湖南 岳陽 414507)

黃金洞金礦床是江南造山帶上重要的金礦產地之一, 礦體賦存在新元古代的淺變質巖中, 受東西向-北西西向構造的嚴格控制。多年來, 黃金洞金礦床的成礦年齡一直存在著爭議。通過對黃金洞金礦區的白鎢礦開展詳細的野外調查、巖相學觀察和Sm-Nd同位素分析, 在147Sm/144Nd-143Nd/144Nd圖解中獲得白鎢礦的等時線年齡為(129.7±7.4) Ma (MSWD=1.0), 對應的Nd()值為?8.21～ ?8.68。結合黃金洞礦區白鎢礦與含金硫化物的交切關系觀察、以及前人的成礦年代學和礦物學研究成果, 認為白鎢礦的等時線年齡可作為黃金洞金礦床的成礦年齡。白鎢礦的Nd() 值大于賦礦地層新元古界冷家溪群和湘東北早白堊世花崗巖, 但小于新元古界倉溪巖群, 表明白鎢礦中的Nd部分來自新元古界冷家溪群和(或)湘東北早白堊世花崗巖, 部分來自新元古界倉溪巖群。綜合前人的研究, 認為在江南造山帶的金銻鎢成礦作用中, 新元古界為礦源層, 區域變質作用和巖漿作用共同促進了金等成礦物質的活化, 構造活化為含礦熱液的運移和沉淀提供了通道和空間。

金礦床; 白鎢礦; Sm-Nd同位素; 湘東北; 江南造山帶

0 引 言

在對金礦床定年時, 最理想的方式是選取與金同期的礦物進行直接定年[1]。然而, 熱液型金礦床中往往缺少可通過傳統方法直接定年的礦物。因此, 其成礦年齡的確定成為一個難以解決的問題[1–2]。近幾十年來, 人們發現很多金礦床中都有白鎢礦的出現, 且這些白鎢礦與金關系密切, 常被作為重要的找礦標志[3–6]。又由于白鎢礦中的Ca2+與Sm、Nd等稀土元素有著相似的半徑和電子結構[7], 使得白鎢礦具有較高的稀土元素含量和Sm/Nd比值[1,8]。因此, 自20世紀80年代 Fryer.[3]首次成功實現Sm-Nd同位素定年以來, 白鎢礦Sm-Nd同位素定年逐漸被運用于許多金礦床的研究中[1,9–12]。

江南造山帶是華南著名的金銻鎢銅鉛鋅多金屬成礦帶, 帶內分布著數百個金-(銻)-(鎢)礦床(點)。多年來, 前人針對江南造山帶上的金-(銻)-(鎢)礦床的成礦時代進行了大量研究, 但得到的年齡大多為流體包裹體Rb-Sr等時線年齡[13–25]、黃鐵礦和方鉛礦等的Pb-Pb模式年齡[26–27]、石英裂變徑跡年齡[28]等類型。流體包裹體Rb-Sr等時線年齡極易受到次生流體包裹體的影響; Pb-Pb模式年齡則容易因為后期熱液活動導致Pb的丟失而不準確; 由于石英的U含量低且不均勻, 石英裂變徑跡年齡的準確性也不高, 且所測的石英也可能為非成礦期的石英。因此, 這些年齡相互之間差異很大, 在很大程度上已制約著對江南造山帶金銻鎢成礦機理的深入研究。自2003年彭建堂等[11]通過白鎢礦的Sm-Nd同位素測試獲得沃溪金銻鎢礦床的成礦年齡開始, 一些學者[12,29–34]以白鎢礦、含金毒砂以及輝銻礦等與金銻鎢礦床的成礦階段密切相關的礦物為對象, 運用Sm-Nd同位素、Re-Os同位素等可靠程度較高的測年方式, 獲得了江南造山帶西南段沃溪金銻鎢礦床、渣滓溪鎢銻礦床、板溪銻礦床、字溪金礦床、金井金礦床、龍山銻金礦床、平秋金礦床和八克金礦床的成礦年齡。

黃金洞金礦床位于江南造山帶中段的湘東北地區, 是江南造山帶上最重要的幾個金礦床之一。前人曾獲得黃金洞金礦床的黃鐵礦Pb-Pb模式年齡為552～416 Ma[26], 流體包裹體Rb-Sr等時線年齡為(425±33) Ma[23]和(152±13) Ma[20]。由于這些測年方法存在著較大的局限性, 黃金洞金礦床目前仍缺乏可靠程度高的成礦年齡。在黃金洞金礦床的勘探開采過程中我們發現, 礦區金品位較高的地段往往有白鎢礦出現。基于此, 本次研究擬對黃金洞金礦區的含白鎢礦礦石進行詳細的野外和鏡下觀察, 并對白鎢礦進行Sm-Nd同位素測試, 以獲得黃金洞金礦床的成礦年齡并探討白鎢礦中Nd的來源。在此基礎上, 結合前人的研究成果, 探討江南造山帶上金- (銻)-(鎢)礦床的成因。

1 區域地質

江南造山帶位于揚子陸塊與華夏陸塊的接合部位、揚子陸塊的東南緣, 又被稱為“江南古陸”“江南古島弧”“江南隆起”[35–36](圖1), 以大面積出露元古宇(1.85～0.8 Ga)淺變質火山碎屑巖為特征[20]。此外, 古生代和中生代的淺海相和陸相地層也有少量出露。中生代的陸相沉積多分布于一系列斷陷盆地之中[36,40]。

江南造山帶的構造演化與新元古代以來揚子陸塊與華夏陸塊的活動緊密相關[41]。新元古代, 作為Rodinia大陸聚合的重要組成部分, 揚子陸塊與華夏陸塊發生碰撞, 形成了江南造山帶[42]。之后, 江南造山帶在加里東期、印支期和燕山期經歷了多期的構造作用。早古生代, 南華裂谷盆地閉合, 揚子和華夏陸塊之間再次發生碰撞, 拉開了加里東期陸內造山作用的序幕。這次造山作用在江南造山帶前泥盆紀地層中形成了一系列北西?近東西向的韌性剪切帶、斷裂和褶皺構造[43–44], 形成了大量的花崗巖、花崗閃長巖和少量的火山巖[45], 并使得地層普遍發生綠片巖相?角閃巖相的變質[41]。印支期的造山作用發生于早中生代, 它使得華南最終成為Pangea超大陸的一部分[46]。同時, 它使得華南早三疊世以前的地層大量褶皺變形和形成逆沖推覆構造, 并伴隨著區域變質作用和巖漿活動[47–48]。印支期巖漿巖規模較小, 以S型花崗巖為主。燕山期, 隨著古太平洋板塊向歐亞板塊的俯沖和回撤, 江南造山帶發育了一系列北東向的深大斷裂和斷陷盆地[49], 同時形成了大量的花崗巖、基性?超基性巖脈和基性?酸性火山巖[50–52]。

圖1 湘東北地質及大地構造位置圖

(a) 華南構造劃分圖(據文獻[37]修改); (b) 湘東北地區構造地質圖(據文獻[38,39]修改)。

1–第四系; 2–白堊紀?第三紀砂巖和礫巖; 3–中泥盆世?中三疊世碳酸鹽巖、砂巖和泥巖; 4–震旦紀?志留紀砂巖、頁巖、礫巖和板巖; 5–新元古界板溪群碎屑沉積巖; 6–新元古界冷家溪群淺變質濁積巖; 7–新元古界倉溪巖群片巖, 片麻巖; 8–燕山期花崗巖; 9–印支期花崗巖; 10–加里東期花崗巖; 11–元古宙花崗巖; 12–斷裂; 13–韌性剪切帶; 14–金礦床(點); 15–鈷礦點; 16–錫礦化; 17–鎢礦化; 18–鈹礦化; 19–鈮鉭礦化; 20–銅礦化; 21–鉛鋅礦化; 22–鎢錫礦化; 23–銅多金屬礦床(點)。

(a) Tectonic framework of South China (modified after reference [37]); (b) geological and structural map of northeastern Hunan (modified after references [38,39]).

1–Quaternary; 2–Tertiary-Cretaceous sandstone and conglomerate; 3–Middle Triassic-Middle Devonian carbonate, sandstone and siltstone; 4–Silurian-Sinian sandstone, shale, conglomerate and slate; 5–clastic sediments of the Neoproterozoic Banxi Group; 6–low-grade metamorphosed turbidites of the Neoproterozoic Lengjiaxi Group; 7–schist and gneiss of the Neoproterozoic Lengjiaxi Group; 8–Yanshanian granitoids; 9–Indosinian granitoids; 10–Caledonian granitoids; 11–Proterozoic granit0ids; 12–fault; 13–ductile shear zone; 14–Au deposit or occurrence; 15–Co deposit; 16–Sn mineralization; 17–W mineralization; 18–Be mineralization; 19–Ni-Ta mineralization; 20–Cu mineralization; 21–Pb-Zn mineralization; 22–W-Sn mineralization; 23–Cu polymetallic deposit or occurrence

湘東北地區位于江南造山帶的中段(圖1a)。區內出露的地層主要為新元古界、中生界白堊系及新生界第四系。新元古界主要分布于斷隆帶上, 由倉溪巖群、冷家溪群和板溪群組成。倉溪巖群主要由云母片巖和黑云母斜長片麻巖組成。冷家溪群和板溪群為一套具有復理石建造的淺變質火山碎屑巖和黏土巖。冷家溪群主要由板巖、(粉)砂質板巖和變質雜砂巖組成, 由老至新依次為雷神廟組、黃滸洞組、小木坪組和大藥姑組。冷家溪群與上覆板溪群呈角度不整合接觸[53]。新元古界的冷家溪群和板溪群富含Au、Sb和W等元素[54], 是金銻鎢礦床的主要賦礦地層[36]。其中, 冷家溪群含Au 0.5～44.2 ng/g, 是地殼克拉克值的1～8倍[38]; 含鎢5～15 μg/g, 局部高達0.18%[54]。白堊系和第四系主要分布于斷陷盆地。除此以外, 震旦紀至三疊紀的地層在區內也有少量出露(圖1b)。

湘東北地區北東向深大斷裂發育。以這些斷裂為界, 湘東北被劃分為一系列相間分布的斷隆和斷陷盆地, 被稱為“盆?嶺式構造”[41]。此外, 2004年肖擁軍等[55]根據構造形跡和地球物理資料認為, 湘東北地區還存在著三條近東西向的韌性剪切帶。新元古代、加里東期、印支期和燕山期巖漿巖在湘東北地區都有出露[56]。新元古代巖漿巖包括長三背、葛藤嶺、大圍山和張邦源等巖體, 主要為S型花崗巖, 成巖年齡大多分布于833～816 Ma之間, 形成于同碰撞的構造環境[35,57–61]。加里東期巖體包括張坊、板杉鋪和宏夏橋等, 成巖年齡為434～432 Ma,為I型花崗巖, 為加厚的中下地殼發生部分熔融而成[62–63]。印支期巖漿巖僅在湘東北的西南部有出露, 成巖年齡分布于250～233 Ma之間, 目前相關研究較少[64]。燕山期巖漿巖出露面積最大, 主要為S型花崗巖, 是伸展環境下加厚下地殼發生部分熔融的產物[65], 代表性巖體有連云山巖體、望湘巖體及金井巖體(圖1b)。其中, 連云山巖體主要由中細粒二云母花崗巖和中粗粒斑狀黑云母花崗巖組成, 為強過鋁質S型花崗巖[39], 其成巖年齡分布于 155～130 Ma之間[49,56],常見綠泥石化、綠簾石化、高嶺土化及絹云母化。在連云山巖體周圍, 由近到遠依次出現W-Sn-Nb- Ta-Be礦化帶、Cu-Pb-Zn礦化帶和Au礦化帶(圖1b)[38,39]。

湘東北地區是江南造山帶重要的金礦產地之一。區內產出有大萬(大洞和萬古)、黃金洞和雁林寺等多個金礦床(點), 它們均分布于北東向深大斷裂長平斷裂帶兩側新元古代冷家溪群的板巖之中(圖1b)。其中, 大萬和黃金洞金礦床均為大型?超大型金礦床。

2 礦床地質

黃金洞金礦床位于湘東北地區北東向長沙?平江深大斷裂帶(簡稱長平斷裂帶)的SE側(圖1b)。區內出露的地層主要為新元古界冷家溪群大藥姑組, 局部被第四系覆蓋。大藥姑組主要由粉砂質板巖、砂質板巖和絹云母板巖組成。巖石普遍經受了區域淺變質作用, 產生的蝕變主要為絹云母化, 其次為弱硅化及少量綠泥石化、黃鐵礦化和碳酸鹽化。礦區內褶皺和斷裂都很發育。褶皺主要為倒轉背向斜, 褶皺樞紐呈北西(西)走向。區內發育兩組斷裂, 分別為東西向?北西西向和北東向。東西向?北西西向斷裂的走向與褶皺樞紐方向大致平行。北東向斷裂主要為泥灣斷裂和許多近平行的次級斷裂。這些斷裂走向北北東, 傾向北西西, 傾角通常大于50°。礦區內尚未發現有火成巖出露(圖2)。

截至2018年, 黃金洞金礦區已探明的金資源量(保有資源量+已開采資源量)達82 t, 平均品位約5 g/t[66]。礦區共發現19條金礦脈, 走向東西向至北西西向, 受東西向?北西西向斷裂控制。其中, 1號脈和3號脈的金資源量占整個礦區金資源量的50%以上。1號脈傾向北, 傾角20°～40°, 沿走向延伸長約3200 m, 礦體厚0.46～2.16 m。3號脈傾向南, 傾角45°～70°, 沿走向延伸長約3300 m, 礦體厚約0.74～ 3.65 m。礦石類型主要為石英脈型和蝕變巖型, 少量為構造角礫巖型(圖3a～3c)。礦石礦物主要為毒砂和黃鐵礦, 少量為白鎢礦、輝銻礦、方鉛礦、閃鋅礦、黃銅礦和自然金等。脈石礦物主要為石英和方解石, 少量為綠泥石、絹云母和白云石等。金呈自然金、晶格金和納米級金顆粒三種形式存在。其中, 晶格金和納米級金顆粒主要賦存于毒砂和含砷黃鐵礦中[56,67,68]。近礦圍巖的蝕變類型多樣, 主要蝕變類型為硅化、黃鐵礦化和毒砂化, 可見少量的絹云母化和綠泥石化。局部圍巖可見輝銻礦化和葉臘石化。

根據野外和鏡下觀察到的穿插關系, 可將黃金洞金礦床的熱液作用劃分為四個階段(圖4): 第一階段以無礦石英(Qz1)為特征, 石英顆粒較大(圖3c); 第二階段以白鎢礦和石英(Qz2)為特征(圖3e); 第三階段為金多金屬硫化物階段, 形成石英(Qz3)、毒砂、黃鐵礦、方鉛礦和自然金礦物組合(圖3f); 第四階段由方解石、石英(Qz4)和少量黃鐵礦組成(圖3g～3h)。其中, 第三階段與金成礦有關。局部可觀察到第二階段的白鎢礦細脈切穿了第一階段形成的無礦石英(Qz1) (圖3c～3e), 同時又被第三階段形成的金多金屬硫化物細脈切穿(圖3c、3e和3f)。

3 樣品采集及分析測試方法

本次研究的含白鎢礦礦石均采自3號礦脈(圖2), 詳細采樣位置見表1。礦區的白鎢礦通常為乳白色, 油脂光澤, 呈細脈狀、團塊狀產出。

在詳細進行野外和室內觀察的基礎上, 首先將樣品碎至粒徑約0.25 mm (60目)。然后, 在雙目鏡下借助熒光燈挑選白鎢礦。在挑選過程中, 將混晶和雜質剔除, 使白鎢礦的純度達到99%以上。最后, 將挑選出來的白鎢礦碎至粒徑約0.075 mm (200目)。白鎢礦Sm-Nd同位素的測定工作在中國地質調查局武漢地質調查中心的Triton熱電離質譜儀上完成。詳細的操作流程參考李華芹[69]。樣品分析測試在超凈化實驗室完成。通過同位素稀釋法得到Sm和Nd含量, 直接對提純的樣品分析得到Nd同位素比值, 質譜分析過程中產生的質量分餾采用146Nd/144Nd=0.7219進行冪定律校正。在分析過程中,采用GBW04419、BCR-2和GSW標準物質對全流程和儀器進行監控。GBW04419的測定結果為Sm=3.028 μg/g, Nd=10.08 μg/g,143Nd/144Nd= 0.512720±0.000005(1σ), 與其證書值(3.03±0.04、10.10±0.12、0.512725±0.000005(2σ))在誤差范圍內一致; BCR-2的測定結果為Sm=6.54 μg/g, Nd=28.85 μg/g,143Nd/144Nd=0.512636±0.000008 (1σ), 與其推薦值(6.41～6.73、27.62～28.97、0.512618～0.512650)在誤差范圍內一致; GSW的測定結果為143Nd/144Nd = 0.512433±0.000005(1σ), 與推薦值0.512438±6(2σ)在誤差范圍內完全一致。標準全流程Sm、Nd空白分別為3.0×10?11g和2.0×10?11g, 對樣品分析結果的影響可忽略不計。Sm和Nd含量的分析誤差優于1%,147Sm/144Nd的分析誤差為0.005%。Sm-Nd同位素年齡通過Isoplot程序分析處理[70]。計算時采用的147Sm衰變常數為6.54×10?12a?1, 球粒隕石均一儲庫(CHUR)現代的147Sm/144Nd和143Nd/144Nd值分別采用0.1967和0.512638[71]。

李達是中共一大的發起者、籌備者、召集者和組織者，他和夫人王會悟也是同時參加黨的一大的唯一一對夫妻。在中國共產黨早期領導人中，“還很少有像李達同志這樣勤奮、這樣有豐富的卓越的成就，這樣在任何困難危險的環境下生命不息、戰斗不止的馬克思主義宣傳家、教育家，這樣堅定勇敢而不斷追求進步，力求達到當代的最高水平的馬克思主義理論戰士”。他為中國共產黨的創立，為馬克思主義在中國的傳播，為豐富毛澤東哲學思想作出了重要貢獻。

圖2 黃金洞礦區地質圖(據文獻[36]修改)

圖3 黃金洞礦區礦脈野外、手標本及顯微鏡下照片

(a) 蝕變巖型礦石; (b) 構造角礫巖型礦石; (c) 石英脈型礦石手標本; (d) 紫外熒光燈照射下的石英脈型礦石手標本; (e) 白鎢礦細脈切穿了無礦石英, 又被黃鐵礦、毒砂細脈切穿(正交偏光); (f) 金多金屬硫化物細脈切穿白鎢礦(反射光); (g) 和 (h) 石英和方解石的礦物組合(正交偏光)。Apy–毒砂; Au–自然金; Cal–方解石; Gn–方鉛礦; Py–黃鐵礦; Qz–石英; Sch–白鎢礦。

(a) Altered rock type ore; (b) tectonic breccia type ore; (c) quartz vein type ore; (d) quartz vein type ore irradiated by the ultraviolet fluorescent lamp; (e) vein of scheelite crosscutting barren quartz and crosscutted by vein of pyrite and arsenopyrite (cross-polarized light); (f) vein of Au polymetallic sulfide crosscutting vein of scheelite (reflected-light); (g) and (h) quartz and calcite (cross-polarized light). Apy–arsenopyrite; Au–native gold; Cal–calcite; Gn–galena; Py–pyrite; Qz–quartz; Sch–scheelite

圖4 黃金洞金礦床的成礦階段和礦物組合

4 分析測試結果

黃金洞礦區3號脈采集的5件樣品中白鎢礦的Sm和Nd含量以及同位素組成如表1所示。白鎢礦Sm和Nd的含量分別為0.5517～5.1330 μg/g和0.5854～ 3.5100 μg/g,147Sm/144Nd比值分布于0.5702～1.1130之間,143Nd/144Nd比值分布于0.512521～0.512979之間。在143Nd/144Nd-147Sm/144Nd圖解中, 5個白鎢礦樣品表現出良好的線性關系(圖5)。運用Isoplot程序求得白鎢礦的等時線年齡(129.7±7.4) Ma, MSWD為1.0, (143Nd/144Nd)i值為0.512040±0.000038 (圖5), 對應的Nd()值為?8.21 ～ ?8.68 (表1)。由于所有樣品均采自黃金洞礦區3號礦脈, 是同源同期熱液活動的產物, 本次獲得的年齡(129.7±7.4) Ma可代表白鎢礦的真實形成年齡。

5 討 論

5.1 黃金洞金礦床的成礦時代

白鎢礦在江南造山帶以及世界上其他地區的很多金礦床中都有產出[36,72]。這些白鎢礦與自然金同時形成或形成于自然金之前[36,72–75], 大多與金有著成因上的聯系[75–76]。因此, 白鎢礦Sm-Nd同位素定年被廣泛用于金礦床的成礦年齡限定[1,9–12]。

在黃金洞金礦區, 白鎢礦出現的地段金的品位往往較高, 甚至有明金出現。根據黃金洞金礦床的階段劃分結果, 金形成于第三階段。這一階段的含金硫化物細脈切穿了第二階段的白鎢礦(圖3f), 且白鎢礦的Sm-Nd等時線年齡為(129.7±7.4) Ma。因此, 推測黃金洞金成礦的年齡晚于(129.7±7.4) Ma。而目前尚未在白堊系中發現金礦化的現象表明(圖1b), 黃金洞金礦床的成礦年齡應早于白堊系的沉積年齡。此外, 長平斷裂帶通常被認為是黃金洞等金礦床的導礦構造[56,77]。長平斷裂帶上產出的大巖金礦化點(圖1b)與黃金洞金礦床相鄰, 礦物組合石英?毒砂?黃鐵礦與黃金洞金礦床成礦階段(第三階段)的礦物組合類似, 這表明大巖金礦化點和黃金洞金礦床可能為同一期金成礦事件的產物。前人[56]已通過鋯石U-Pb定年和白云母Ar-Ar定年得到大巖金礦化點的成礦年齡為(142～130) Ma。根據以上論述, 黃金洞金礦床的成礦年齡應為130 Ma左右, 與白鎢礦的Sm-Nd等時線年齡近似。白鎢礦的年齡(129.7±7.4) Ma可大致作為成礦年齡。

表1 黃金洞金礦床中白鎢礦的Sm-Nd同位素組成

圖5 湖南黃金洞金礦床白鎢礦Sm-Nd等時線圖

5.2 黃金洞金礦床白鎢礦中Nd的來源

由于白鎢礦從流體中結晶時, Nd同位素不會受到影響[78], 白鎢礦的Nd同位素被廣泛運用于源區示蹤的工作[1,11,30,78,79]。本次測得黃金洞金礦床中白鎢礦的Nd()值位于?8.21～?8.68之間, 表明Nd同位素為殼源。根據毛景文等[38]的Sm-Nd同位素數據, 重新計算得賦礦地層冷家溪群的Nd(129.7 Ma)值分布于?10.30 ～ ?13.86之間, 小于白鎢礦的Nd()值。礦區外圍出露的時代更老的倉溪巖群的Nd(129.7 Ma)值分布于?5.80 ～ ?8.06之間[80], 大于白鎢礦的Nd()值。同時, 湘東北地區早白堊世的S型花崗巖的Nd(129 Ma)值分布于?10.02 ～ ?10.36之間(中南大學未發表數據) (圖6)。這表明, 白鎢礦中的Nd可能部分來自于冷家溪群和(或)湘東北早白堊世的花崗巖, 部分來自于新元古界倉溪巖群。

5.3 黃金洞金礦床的成因

在黃金洞金礦區, 切穿第一階段無礦石英的白云母的Ar-Ar年齡為397～399 Ma[81], 表明東西向?北西西向的賦礦構造形成于加里東期或更早。同樣賦存于東西向?北西西向賦礦構造中的第二階段白鎢礦的Sm-Nd等時線年齡為(129.7±7.4) Ma, 表明賦礦構造在燕山期發生了活化。前人研究表明, 向華南板塊俯沖的古太平洋板塊發生后撤, 進而導致整個華南地區的應力體系由擠壓向伸展轉換的時間也為130 Ma左右[52,82], 與黃金洞金礦床的成礦年齡在誤差范圍內一致。因此, 可能是這次構造事件導致了湘東北地區構造的活化, 從而為黃金洞金礦床的成礦流體提供了運移的通道和成礦的空間。

圖6 黃金洞金礦區白鎢礦與湘東北各地質體εNd(t)值對比圖

新元古界倉溪巖群的Nd() (=129.7 Ma)根據文獻[80]重新計算; 新元古界冷家溪群的Nd() (=129.7 Ma)根據文獻[38]重新計算; 湘東北早白堊世花崗巖的Nd() (=129 Ma)數據引自中南大學未發表數據

Nd() (=129.7 Ma) for the Neoproterozoic Cangxiyan Group was calculated according to reference [80];Nd() (=129.7 Ma) for the Neoproterozoic Lengjiaxi Group was calculated according to reference [38], whileNd() (=129 Ma) for early Cretaceous granites in northeastern Hunan was cited from unreleased data of Central South University

5.4 對江南造山帶金銻鎢成礦作用的啟示

在江南造山帶上, 絕大多數金銻鎢礦床賦存于新元古界地層之中[36,77]。S和Pb同位素分析結果表明, 這些礦床的成礦物質主要來源于賦礦的新元古界(文獻[36]及其參考文獻)。同時, 元素含量分析結果表明, 新元古界(尤其是冷家溪群)的Au、Sb和W的含量高于地殼豐度值[38,54]。因此, 江南造山帶上絕大多數金銻鎢礦床的礦源層應為新元古界, 各個礦床成礦時代不一致可能是因為成礦物質被活化、遷移、沉淀成礦的時間不同所導致的。

關于引起礦源層中成礦元素活化的因素, 有學者認為是大規模的造山作用[25,93–96]和(或)區域變質作用[97–100]。針對江南造山帶金銻鎢礦床的成礦年代學研究結果顯示, 不論是加里東期、印支期還是燕山期, 在江南造山帶的西南段、中段和北東段通常都有相近的年齡(不論是成礦年齡還是無礦的熱液活動年齡)出現(表2, 圖7)。因此, 大規模的造山作用和(或)區域變質作用在引發江南造山帶熱液活動方面發揮了重要作用。江南造山帶大部分金銻鎢礦床的成礦流體主要為變質水[25,95,99,101–109]的現象也支持這個觀點。

表2 江南造山帶已報道和本文中的金銻鎢礦床年齡統計表

(續表2)

粗體的年齡數據為“較可靠”的年齡; 其余為“較不可靠”的年齡。“較可靠”的年齡和“較不可靠”的年齡的定義見圖7的說明。

圖7 江南造山帶北東段、中段、西南段年齡對比圖(年齡數據來自表2)

圖中“較可靠”的年齡指對應的定年礦物的成因明確, 且與成礦階段/無礦階段的關系明確的年齡; “較不可靠”的年齡指對應的定年礦物成因不明, 或與成礦階段/無礦階段的關系不明的年齡。

Robust ages in the figure represent ages that were dated by minerals with specific genesis and relationship with ore-forming stage/barren stage;Less robust ages represent ages that were dated by minerals without specific genesis or relationship with ore-forming stage/barren stage.

同時, 江南造山帶上的金銻鎢礦床大多在空間上與巖漿巖相聯系。部分礦區有巖體或巖脈出露(如龍山金銻礦床[12]); 部分礦區盡管沒有巖體露頭, 但被認為深部存在隱伏巖體(如大萬金礦床[110]), 或其附近的北東向深大斷裂沿線有巖體產出(如大萬金礦床、黃金洞金礦床(圖1b)和沃溪金銻鎢礦床)。金銻鎢礦床的成礦年齡通常與這些鄰近巖體的年齡相近或稍晚。例如, 黃金洞金礦床的年齡((129.7±7.4) Ma)、大巖金礦化點的年齡(130 Ma)[56]略晚于長平斷裂帶沿線燕山期巖體的年齡(155～130 Ma)[49,56]; 龍山金銻礦床的年齡((210±2) Ma)[12]和渣滓溪銻鎢礦床的年齡((227.3±6.2) Ma)[30]與附近晚三疊世巖體的年齡(228～201 Ma)[111]大致相等。氫氧同位素分析結果顯示, 江南造山帶金銻鎢礦床的成礦流體中除了變質水外, 通常還有少量巖漿水的參與[102,104,106,107]。在湘東北地區, 還可觀察到以連云山巖體為中心, 由近到遠依次出現高溫、中溫和低溫的成礦元素分帶[38,39](圖1)。以上這些證據表明, 巖漿作用也在成礦物質的活化過程中發揮了重要作用, 可能其提供的熱能或帶來的某些流體或物質有利于礦源層中成礦物質的活化。

此外,江南造山帶上的金銻鎢礦床大多受構造的控制, 產出于北東向深大斷裂兩側的次級斷裂中[41,77]。平秋[29,31]、金井[29,34]和黃金洞[81]等礦床同時存在著兩個或多個年齡(表2)的現象表明, 控礦構造在形成后可能再次活化[36], 構造的活化可能為含礦流體的運移和沉淀成礦提供了通道和空間。

綜上所述, 礦源層中金等成礦物質的活化可能是造山作用及其相關的區域變質作用和巖漿作用共同作用的結果, 而構造活化可能為含礦流體的運移和沉淀成礦提供了通道和空間。在某個特定的時期, 之所以部分地區成礦而部分地區不成礦, 一方面可能是不成礦地區區域變質作用和(或)巖漿作用的影響程度較低導致礦源層中的成礦物質沒有被活化, 另一方面可能是不成礦地區缺乏構造活化提供的成礦流體運移的通道和沉淀成礦的空間。

5.5 對找礦工作的啟示

本次研究表明, 在江南造山帶的金銻鎢成礦作用中, 新元古界地層是礦源層, 區域變質作用、巖漿作用和構造活化在成礦物質的活化、遷移和沉淀過程中起到了重要作用。因此, 在江南造山帶的找礦工作中, 可將新元古界地層、火成巖和活化的構造作為重要的預測要素。

6 結 論

(1) 黃金洞金礦床的成礦年齡為(129.7±7.4) Ma;

(2) 黃金洞金礦床白鎢礦中的Nd部分來自新元古界冷家溪群和(或)湘東北早白堊世的花崗巖, 部分來自新元古界倉溪巖群;

(3) 在江南造山帶上, 新元古界地層為金銻鎢礦床的礦源層, 區域變質作用和巖漿作用的綜合作用可能為新元古界地層中金等成礦物質的活化提供了必要條件, 構造的活化可能為含礦熱液提供了運移通道的和沉淀成礦的空間。

中國地質大學(武漢)蔣少涌教授和中國地質科學院地質研究所周利敏副研究員對本文的初稿提出了寶貴的修稿意見, 在此表示衷心的感謝！

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Scheelite Sm-Nd age of the Huangjindong Au deposit in Hunan and its geological significance

ZHOU Yue-qiang1,2,3, DONG Guo-jun3*, XU De-ru1,4, DENG Teng4, WU Jun3, WANG Xiang3, GAO Lei5and CHEN Xiao-gang5

1. Key Laboratory of Mineral and Metallogeny, Guangzhou Institute of Geochemistry, Chinese Academy of Sciences, Guangzhou 510640,China;2. University of Chinese Academy of Sciences, Beijing 100049, China; 3. Team 402, Hunan Geology and Mineral Resources Exploration and Development Bureau, Changsha 410014, China; 4. State Key Laboratory of Nuclear Resources and Environment, East China University of Technology, Nanchang 330013, China; 5. Huangjindong Mining Industry Limited Company of Hunan, Yueyang 414507, China

The Huangjindong gold deposit is one of the most important Au reserve in the Jiangnan Orogenic Belt. Its orebodies are strictly controlled by a series of E- to WNW-trending faults developed in low-grade metamorphic Neoproterozoic strata. However, the mineralization age of the Huangjindong deposit has not been constrained. Detailed field surveys, petrographic observations and Sm-Nd isotopic analyses have been carried out on scheelites in the Huangjindong deposit area. The scheelites yield an isochron age of 129.7±7.4 Ma (MSWD=1.0) on the143Nd/144Nd versus147Sm/144Nd plot, with correspondingNd() values varying from ?8.21 to ?8.68. Based on the crosscutting relationship of the scheelite vein and Au-bearing sulfide vein in the Huangjindong deposit, and the previous studies on geochronology and mineralogy, the isochron age of scheelites is considered to be the mineralization age of the Huangjindong gold deposit. TheNd() values of scheelites are higher than those of the ore-bearing Neoproterozoic Lengjiaxi Group and early Cretaceous granitoids in northeastern Hunan but lower than those of the Neoproterozoic Cangxiyan Group, indicating that Nd in the scheelites partly originate from the Neoproterozoic Lengjiaxi Group and/or the early Cretaceous granitoids in northeastern Hunan, and partly from the Neoproterozoic Cangxiyan Group. Combined with previous research, ore materials of the Au-Sb-W deposits in the Jiangnan Orogenic belt are interpreted to be sourced from the Neoproterozoic strata owing to regional metamorphism and magmatic activities are interpreted to have facilitated the reactivation of ore-forming materials such as Au. Structural reactivation was interpreted as the source of channels and space for ore-fluids during the Au-Sb-W ore-forming process in the Jiangnan Orogenic Belt.

Au deposit; scheelite; Sm-Nd isotope; northeastern Hunan; Jiangnan Orogenic Belt

P597.1; P619.51

A

0379-1726(2021)04-0381-17

10.19700/j.0379-1726.2021.04.005

2019-11-15;

2020-04-15;

2020-07-21

國家自然科學基金項目(41930428, 42002090)、湖南省自然資源廳科技項目(2020-13)、湖南省礦產資源深部探測研究中心(DK402–2019–PT01)和國家重點研發計劃(2016YFC0600401, 2017YFC0602302)

周岳強(1985–), 男, 博士, 高級工程師, 構造地質學專業。E-mail: 271164104@qq.com

DONG Guo-jun, E-mail: dgj402@163.com; Tel: +86-731-85596782