王嘉瑋，王剛，王宗起，武昱東，王東升，王坤明

1)中國地質(zhì)大學(xué)(北京)，北京，100083； 2)中國地質(zhì)科學(xué)院礦產(chǎn)資源研究所，自然資源部成礦作用與資源評(píng)價(jià)重點(diǎn)實(shí)驗(yàn)室，北京，100037

內(nèi)容提要: 南秦嶺的北大巴山—武當(dāng)山—十堰—隨州一帶發(fā)育大規(guī)模的鎂鐵質(zhì)巖墻群，其巖石學(xué)成因?yàn)榈刭|(zhì)學(xué)家所廣泛關(guān)注。本文對(duì)其中的武當(dāng)山十堰地區(qū)黃龍—方灘一帶發(fā)育的輝長巖體開展了全巖地球化學(xué)、SHRIMP鋯石U-Pb年齡以及LA—MC—ICP—MS鋯石Hf同位素組成研究。結(jié)果表明，輝長巖形成于晚三疊世(221.2±2.5 Ma)；巖石地球化學(xué)組成顯示輝長巖為亞堿性拉斑玄武巖系列，輕稀土富集重稀土虧損，其平滑右傾的稀土配分模式與E—MORB相似；中等Ti、Zr、Hf、Nb含量，虧損Rb、Sr等大離子親石元素，以及結(jié)晶年齡鋯石的εHf(t)值在-13.5至-6.18之間，表明巖石具有古老的兩階段Hf模式年齡(2103～1640 Ma)。綜合分析表明：該套輝長巖巖漿為尖晶石二輝橄欖巖低壓、中等程度部分熔融形成，并且其源區(qū)為虧損地幔與富集地幔組分混合成因；結(jié)合區(qū)域構(gòu)造演化的相關(guān)資料，認(rèn)為該套E—MORB性質(zhì)輝長巖形成于類似匯聚邊緣的構(gòu)造環(huán)境，可能為受勉略洋殼俯沖影響，為俯沖—碰撞造山階段產(chǎn)物。

南秦嶺北大巴山—武當(dāng)山—十堰—隨州一帶近千千米造山帶中發(fā)育大規(guī)模的鎂鐵質(zhì)巖墻群或巖脈(周鼎武等，1997；張成立等，2002；胡健民等，2004；薛懷民等，2011)。綜合分析前人研究發(fā)現(xiàn)，該區(qū)鎂鐵質(zhì)巖石主要集中在：① 新元古代(850～610 Ma)拉斑玄武巖系列和堿性玄武巖系列，部分代表了島弧—弧后伸展構(gòu)造環(huán)境(蘇文等，2013； Xu Yang et al., 2016; 劉嘉威等，2018)，部分代表了地幔柱—裂谷環(huán)境(周鼎武等，1998，1999; 薛懷民等，2011; Wang Lijuan et al., 2013; Zhu Xiyan et al., 2015; Li Qiwei et al., 2016)；② 古生代(470～400 Ma)堿性玄武巖系列具有板內(nèi)洋島玄武巖特征，是區(qū)域伸展構(gòu)造背景下產(chǎn)物，但伸展構(gòu)造機(jī)制存在幔源巖漿底侵(胡健民等，2002，2003，2004)、大陸裂谷(王存智等，2009；鄒先武等，2011；Nie Hu et al., 2016)和弧后伸展等不同認(rèn)識(shí)(王坤明等，2014；Wang Kunming et al., 2015；許光等，2018)；③ 區(qū)域內(nèi)僅有少量中生代的報(bào)道(220 Ma)，前人認(rèn)為其代表了印支期勉略洋閉合后由碰撞擠壓轉(zhuǎn)換為伸展環(huán)境(Nie Hu et al., 2016)。綜上可見，南秦嶺造山帶發(fā)育多期次且構(gòu)造背景復(fù)雜的鎂鐵質(zhì)巖漿，對(duì)武當(dāng)—隨州地區(qū)部分或整體發(fā)育的鎂鐵質(zhì)巖的產(chǎn)出狀態(tài)，仍存在侵入(周鼎武等，1998；胡健民等，2004；薛懷民等，2011)和構(gòu)造侵位(王荃等，2010；王宗起等?)等不同認(rèn)識(shí)。本文對(duì)武當(dāng)山十堰地區(qū)黃龍—方灘一帶發(fā)育的侵入狀輝長巖體進(jìn)行了詳細(xì)的巖石地球化學(xué)、鋯石U-Pb年代學(xué)和Hf同位素研究，闡明其形成時(shí)代和巖石成因，從而為進(jìn)一步認(rèn)識(shí)區(qū)域中生代基性巖墻特征和理解區(qū)域構(gòu)造演化提供新的證據(jù)。

1 區(qū)域地質(zhì)背景

武當(dāng)山是南秦嶺造山帶的重要組成部分(圖1a)，主要發(fā)育武當(dāng)群變沉積巖和基性、中酸性變火山巖組，其上為耀嶺河群變玄武質(zhì)火山巖(熔巖、火山碎屑巖或凝灰?guī)r)夾少量變酸性火山巖和變泥質(zhì)巖基性火山—沉積巖(陳晉鑣等，1991；付建明等，1999；蔡志勇等，2006；祝禧艷等，2008；張永清等，2013)，二者接觸關(guān)系存在整合和構(gòu)造拼合接觸等不同認(rèn)識(shí)(陳晉鑣等，1991；胡健民等，1995；祝禧艷等，2008)。震旦系發(fā)育在武當(dāng)山周緣，為陡山沱組和燈影組次深海相沉積巖。此外，區(qū)域內(nèi)還發(fā)育新元古代、古生代及中生代多期次巖漿活動(dòng)，以鎂鐵質(zhì)—超鎂鐵質(zhì)巖為主，并有少量花崗質(zhì)巖石出露(周鼎武等，1997；胡健民等，2004；凌文黎等，2007；蘇文等，2013；Zhu Xiyan et al., 2015；Li Qiwei et al., 2016；Nie Hu et al., 2016；Wang Ruirui et al., 2016)。區(qū)域上發(fā)育北西向和北東向構(gòu)造，武當(dāng)?shù)貕K被北部的兩鄖斷裂和南部的十堰斷裂(圖1b)分為北部、南部和中部3個(gè)不同的構(gòu)造區(qū)段(趙國春等，2003；胡建民等，2004)，兩條斷裂總體呈北西西向展布，斷面北傾，它們之間發(fā)育武當(dāng)群、耀嶺河群以及鎂鐵質(zhì)的輝綠巖和輝長巖(周鼎武等，1999；胡健民等，2003；Wang Lijuan et al., 2013)，少量超鎂鐵質(zhì)的輝石巖(湖北省地質(zhì)礦產(chǎn)局區(qū)域地質(zhì)礦產(chǎn)調(diào)查所?；湖北省地質(zhì)調(diào)查院?)和花崗質(zhì)侵入巖(Wang Ruirui et al., 2016；圖1b)。研究區(qū)黃龍—方灘一帶位于十堰斷裂北側(cè)，構(gòu)造變形強(qiáng)烈，前人通過地層對(duì)比認(rèn)為該地區(qū)物質(zhì)組成與武當(dāng)?shù)貕K整體一致，主要由武當(dāng)群、耀嶺河群和局部出露的陡山沱組等前寒武系有序地層及少量晉寧期和加里東期鎂鐵質(zhì)巖組成(湖北省地質(zhì)礦產(chǎn)局區(qū)域地質(zhì)礦產(chǎn)調(diào)查所?，圖1c)。王剛等(2018)報(bào)道了該地區(qū)原劃定的前寒武紀(jì)巖石地層中發(fā)現(xiàn)晚古生代沉積組合與火山活動(dòng)物質(zhì)的存在，且為海相沉積特征，后續(xù)又報(bào)道該地區(qū)發(fā)育中二疊世E—MORB型玄武巖塊體，為洋中脊或附近海山環(huán)境(王剛等，2019)。此外，獲得了大量不同時(shí)代年代學(xué)證據(jù)，并結(jié)合野外構(gòu)造解析和室內(nèi)研究提出黃龍—方灘地區(qū)是包含了新元古代—古生代—中生代等若干不同時(shí)代的物質(zhì)組成的混雜巖帶(王宗起等?)。因此，研究區(qū)內(nèi)前人劃歸的前寒武紀(jì)地層以及發(fā)育的鎂鐵質(zhì)巖的時(shí)代等應(yīng)予以重新認(rèn)識(shí)和研究。

圖1 武當(dāng)—十堰地區(qū)大地構(gòu)造位置(a)和武當(dāng)?shù)貐^(qū)地質(zhì)簡圖(b，據(jù)凌文黎等，2007)以及黃龍—方灘一帶地質(zhì)簡圖 (c，據(jù)湖北十堰黃龍—方灘地區(qū)1∶5萬地質(zhì)簡圖，1985)Fig. 1 Location of Wudang Mountain in Qinling—Dabie Orogen(a), geological map of Wudang Mountain(b; modified from Ling Wenli et al., 2007)and geological map of the Huanglong—Fangtan area(c; after 1∶50000 geological map of the Huanglong—Fangtan area, Shiyan City of Hubei Province,1985)

2 樣品和測試方法

2.1 樣品

通過對(duì)武當(dāng)十堰黃龍地區(qū)沉灘溝—文武溝一帶進(jìn)行路線剖面調(diào)查(圖1c)、樣品采集和室內(nèi)測試分析，在研究區(qū)識(shí)別出一套玄武巖、灰?guī)r(大理巖)塊體，與碳硅質(zhì)砂板巖、凝灰質(zhì)砂巖和大理巖互層產(chǎn)出，并呈巖片狀包裹于碎屑砂巖、變凝灰質(zhì)砂巖(片巖)和變質(zhì)泥巖(含石榴石二云母片巖)等巖石中(圖2；王剛等，2018，2019)。本文輝長巖體規(guī)模較大，原1∶5萬地質(zhì)圖中將該部分巖體劃歸為晉寧期輝綠巖體(湖北省地質(zhì)礦產(chǎn)局區(qū)域地質(zhì)礦產(chǎn)調(diào)查所?)，圖巖體東西向延伸近5 km，寬度100～200 m，地質(zhì)圖中巖體北側(cè)與地層呈斷層接觸，野外實(shí)際考察中發(fā)現(xiàn)巖體呈侵入狀切層產(chǎn)出(圖3a)，但未見明顯的冷凝邊和烘烤邊，巖體具有一定巖相變化，自兩側(cè)向中部表現(xiàn)為中細(xì)粒結(jié)構(gòu)輝綠輝長巖逐漸過渡為中粗粒似斑狀結(jié)構(gòu)輝長巖，本文樣品采集于巖體中部輝長巖(圖3b)，采樣點(diǎn)經(jīng)緯度為：N32°42’51.43”，E110°35’22.81”。

圖2 湖北十堰黃龍沉灘溝—文武溝信手剖面圖(據(jù)王剛等，2018)Fig. 2 Geological section from Chentangou to Wenwugou of Huanglong area, Shiyan city of Hubei Province (from Wang Gang et al., 2018&)

鏡下觀察得出，所采輝長巖為輝長輝綠結(jié)構(gòu)(圖3c)，局部發(fā)育嵌晶結(jié)構(gòu)(圖3d)。主要礦物為單斜輝石(35%～37%)、斜長石(45%～50%)、角閃石(～5%)、金屬礦物(鈦鐵礦、磁鐵礦; ～8%)；副礦物磷灰石。單斜輝石呈自形—半自形晶產(chǎn)出，粒徑為1～1.5 mm，個(gè)別顆粒綠泥石化；斜長石多呈半自形窄板狀晶體產(chǎn)出，粒徑為1～2 mm，個(gè)別顆粒鈉長石化。鈦鐵礦呈半自形粒狀晶體(圖3c)，磷灰石呈細(xì)小的柱狀體(圖3d)。

2.2 測試方法

樣品磨片、碎樣和鋯石挑選工作由河北省區(qū)域地質(zhì)礦產(chǎn)調(diào)查研究所實(shí)驗(yàn)室完成。全巖主微量及稀土元素測試由中國地質(zhì)科學(xué)院國家地質(zhì)實(shí)驗(yàn)測試中心完成。主量元素采用XRF方法測試，F(xiàn)eO用濕化學(xué)法單獨(dú)分析；微量元素和稀土元素采用等離子質(zhì)譜儀(PE300D)測試。其中Fe2O3、P2O5、TiO2、MnO的檢測準(zhǔn)確度為10%，其余數(shù)據(jù)檢測準(zhǔn)確度為1%；微量和稀土元素含量大于10×10-6的元素分析相對(duì)誤差小于5%，小于10×10-6的元素分析相對(duì)誤差小于10%。用常規(guī)方法將巖石破碎，經(jīng)磁法和密度分選后，經(jīng)淘洗烘干并在雙目鏡下挑選鋯石，鋯石樣品的制靶和陰極發(fā)光圖像工作以及鋯石U-Pb定年測試分析在中國地質(zhì)科學(xué)院地質(zhì)研究所北京離子探針中心完成，詳細(xì)實(shí)驗(yàn)測試過程可參見宋彪等(2002)。鋯石U-Pb年齡測定前，依據(jù)透反射圖像和陰極發(fā)光圖像分析，對(duì)鋯石樣品隨機(jī)圈定裂隙和包裹體不發(fā)育的顆粒。SHRIMP數(shù)據(jù)普通Pb由實(shí)測204Pb校正，鋯石年齡諧和圖等由Isoplot 3.0程序完成(Ludwig，2003)。鋯石Hf同位素測試分析在中國地質(zhì)科學(xué)院礦產(chǎn)資源研究所同位素實(shí)驗(yàn)室完成，所測點(diǎn)位與測年點(diǎn)位一致，使用儀器為Finnigan Neptune型多接收等離子質(zhì)譜儀和Newwave UP 213激光剝蝕系統(tǒng)，采用GJ1作為外標(biāo)，儀器運(yùn)行條件和詳細(xì)實(shí)驗(yàn)測試過程可參見侯可軍等(2009)。

圖3十堰黃龍沉灘溝輝長巖露頭和顯微照片F(xiàn)ig. 3 Outcrops and microscopic texture of mafic rocks in Huanglong—Chentangou area, Shiyan city Cpx—單斜輝石; Pl—斜長石;Ap—磷灰石; Mt—磁鐵礦；Ilm—鈦鐵礦; Cpx—Clinopyroxene; Pl—Plagioclase; Ap—Apatite; Mt—Magnetite; Ilm—Ilmenite

3 測試結(jié)果

3.1 鋯石U-Pb年齡

輝長巖樣品中的鋯石顆粒呈無色透明自形、半自形結(jié)構(gòu)，CL圖像顯示大部分呈灰黑色均質(zhì)結(jié)構(gòu)，部分發(fā)育生長振蕩環(huán)帶。鋯石粒徑為40～180 μm，長短軸比值為4∶1～2∶1。本文對(duì)16顆單顆粒鋯石進(jìn)行SHRIMP方法測試，數(shù)據(jù)見表1。獲得了8顆時(shí)代分散于古元古代(2485 Ma)、中元古代(1019 Ma)、新元古代(825 Ma，747 Ma，639 Ma，625 Ma)、古生代(528 Ma，427 Ma)等的繼承或捕獲鋯石年齡，其余8顆鋯石年齡集中在215～233 Ma(圖4a、b)。鋯石形態(tài)和Th/U值(0.16～0.82，均大于0.1)表明這些鋯石為巖漿成因，其中6顆鋯石加權(quán)平均年齡為221.2±2.5 Ma(MSWD = 3.2)，代表了輝長巖結(jié)晶年齡。

圖4 十堰黃龍—方灘地區(qū)輝長巖鋯石U-Pb年齡及CL圖像(紅色圓圈為鋯石測年點(diǎn)，綠色圓圈為Hf同位素測試點(diǎn))Fig. 4 U-Pb age and CL images of zricon from gabbro in Huanglong—Fangtan area, Shiyan(red circles represent zircon dating spots, and the green one represent Hf isotope testing spot inFig. 4a)

3.2 巖石地球化學(xué)組成

本次選取了5件樣品進(jìn)行巖石地球化學(xué)測試分析，測試數(shù)據(jù)見表格2。樣品SiO2變化范圍介于43.71%～49.99%(均值47.78%)；TiO2含量介于1.27%～2.65%(均值1.84%)；其余主要元素含量的變化范圍均不大，其中Al2O3和Fe2O3T分別介于13.94%～15.32%(均值14.7%)和9.24%～16.21%(均值12.90%)；CaO含量在8.27%～11.35%(均值9.66%)；Na2O含量介于2.37%～4.03%(均值3.34%)；MgO含量6.03%～7.30%，Mg#值介于42～61；全堿含量介于2.67%～4.69%。在TAS分類圖解中(圖5a)，大部分樣品都落在亞堿性系列輝長巖區(qū)域。在10000 Zr/TiO2—Nb/Y分類圖解上(圖5b)，所有樣品都落于亞堿性系列輝長巖區(qū)域。在K2O—SiO2圖解和Y—Zr圖解上(圖6a、b)進(jìn)一步劃分為拉斑玄武巖系列。與Nie Hu等(2016)報(bào)道的武當(dāng)山南部發(fā)育的中生代(～220 Ma)鎂鐵質(zhì)巖具有相似的巖漿系列特征。

圖5 十堰黃龍—方灘地區(qū)輝長巖TAS圖解(a，底圖據(jù)Middlemost, 1994)和10000Zr/TiO2 — Nb/Y圖解 (b，底圖據(jù)Pearce at al., 1996)Fig. 5 Classification diagrams of TAS and 10000Zr/TiO2 versus Nb/Y for gabbro in Huanglong—Fangtan area. Shiyan City (a，after Middlemost, 1994; b，after Pearce at al., 1996)

圖6 十堰黃龍—方灘地區(qū)輝長巖K2O—SiO2圖解(a，底圖據(jù)Rickwood, 1989)和Y—Zr圖解 (b，底圖據(jù)Barrett, 1999；圖例同圖5)Fig. 6 Magma series diagrams of K2O versus SiO2 and Y versus Zr for gabbro in Huanglong—Fangtan area, Shiyan City (a，after Rickwood, 1989; b，after Barrett, 1999; Legends are the same to those inFig. 5)

輝長巖樣品∑REE值介于54.4×10-6～111×10-6，其中∑LREE集中在43.2×10-6～91.7×10-6，∑HREE值介于11.2×10-6～19.7×10-6；輕重稀土比值介于3.77～4.65，(La/Yb)N=3.47～4.85，所有樣品均顯示輕稀土富集重稀土虧損的特征；(La/Sm)N=1.71～2.11，輕稀土輕微分異；(Gd/Lu)N=1.66～1.95，說明重稀土亦輕微分異；在球粒隕石標(biāo)準(zhǔn)化的稀土分配模式圖中大部分樣品呈平坦微右斜模式，類似于E—MORB稀土配分曲線，輕重稀土分異程度低于OIB和土耳其地區(qū)造山帶后碰撞階段堿性玄武巖(圖7a)。樣品δEu=0.95～1.18，平均為1.01，Eu異常不明顯；樣品δCe=1.04～1.05，平均為1.05，無明顯異常。Nie Hu等(2016) 報(bào)道的武當(dāng)山南部發(fā)育的中生代鎂鐵質(zhì)巖顯示出N—MORB和E—MORB兩種稀土配分曲線特征，三組樣品從空間展布上看，自南向北表現(xiàn)為N—MORB向E—MORB過渡的特征。

樣品Zr、Hf和Nb豐度變化范圍分別為65.4×10-6～143×10-6，1.82×10-6～3.76×10-6，5.11×10-6～10.3×10-6，5件樣品的元素豐度值與中等Zr、Hf和Nb豐度的E—MORB(73.0×10-6，2.03×10-6，8.30×10-6)較相近，其中相容元素Ni、Cr和Co含量相對(duì)較低，Ni=48.4×10-6～105×10-6，Cr變化范圍較大，介于7.38×10-6～736×10-6，Co=40.5×10-6～60.4×10-6。樣品原始地幔標(biāo)準(zhǔn)化微量元素配分曲線整體與E—MORB配分曲線相似，呈平坦微右傾型分配模式(圖7b)。其中Rb、Sr等大離子親石元素表現(xiàn)為虧損，而Pb元素富集成峰。

表2 湖北十堰黃龍—方灘地區(qū)輝長巖主量元素(%)、微量(×10-6)和稀土元素(×10-6)組成Table 2 Analyses and ratios of major element(%), rare earth element(×10-6) and trace element(×10-6) for gabbro samples from the Huanglong—Fangtan area, Shiyan City of Hubei Province

圖7十堰黃龍—方灘地區(qū)輝長巖稀土配分曲線(a)和微量元素蛛網(wǎng)圖(b)Fig. 7 Chondrite-normalized rare earth element patterns(a)and primitive mantle-normalized spidergrams (b)for gabbro in Huanglong—Fangtan area, Shiyan City

3.3 鋯石Hf同位素組成

鋯石Hf同位素測試分析點(diǎn)位和U-Pb點(diǎn)相對(duì)應(yīng)，測試結(jié)果見表3。代表輝長巖巖漿結(jié)晶年齡的鋯石n(176Yb)/n(177Hf)值范圍為0.097167～0.241165，n(176Lu)/n(177Hf)值變化范圍為0.001523～0.004431，n(176Hf)/n(177Hf)值范圍為0.282354～0.282479。根據(jù)鋯石結(jié)晶年齡計(jì)算，獲得εHf(t)值在-10.27至-6.18，峰值為-9.29；鋯石Hf模式年齡TDM1=1202～1332 Ma，TDM2=1640～1895 Ma(圖8)，fLu/Hf=-0.95～-0.87，明顯小于下地殼值(-0.34)和上地殼值(-0.72)，其兩階段模式年齡更能反映源區(qū)物質(zhì)從虧損地幔被抽取的時(shí)間或源區(qū)物質(zhì)在地殼的平均存留年齡(Amelin et al., 1999)。

表3 十堰黃龍—方灘地區(qū)輝長巖鋯石Lu—Hf同位素組成

圖8 十堰黃龍—方灘地區(qū)輝長巖鋯石Hf和模式年齡組成Fig. 8 Zricon Hf and model age for gabbro from the Huanglong—Fangtan area, Shiyan City (a) 鋯石Hf組成；(b) 鋯石Hf單階段模式年齡組成；(c) 鋯石Hf兩階段模式年齡組成 (a) Zircon Hf isotope composition; (b) Zircon Hf single-stage model age composition; (c) Zircon Hf two-stage model age composition

4 巖石成因

4.1 巖漿演化

分析結(jié)果顯示，輝長巖樣品Eu具有弱負(fù)異常，Mg#=42～61，Ni=48.4×10-6～105×10-6，二者均低于原始巖漿值(Mg#值>65，Ni含量>235×10-6；Hess,1992；鄧晉福等，2004)，說明母巖漿在巖漿房內(nèi)或上升至地表的過程中曾發(fā)生明顯的分離結(jié)晶作用。在La/Sm—La圖解上(圖9a)輝長巖樣品表現(xiàn)出部分熔融的特點(diǎn)，指示初始巖漿先后經(jīng)歷了部分熔融作用和分離結(jié)晶作用(鄧晉福等，2015)。基性巖中，大離子親石元素如Rb、Ba、Sr等更容易受到后期蝕變與變質(zhì)作用改造，而V、Cr等過渡元素和Zr、Hf、Nb、Ta、Ti等高場強(qiáng)元素以及稀土元素的活動(dòng)性不會(huì)改變，常用來分析巖漿演化過程(Pearce and Cann, 1973；Riley et al., 2001)。樣品集中投影在Nb/U—Nb圖解中的MORB區(qū)域附近(圖9b)，(La/Sm)N<4.5，且Nb、Ta也并未出現(xiàn)虧損，反而Ta相對(duì)富集，這都表明巖漿演化過程中同化混染作用是有限的(Keppler, 1996)。因此本文測試樣品先后經(jīng)歷了源巖部分熔融和母巖漿分離結(jié)晶作用，巖漿上升過程中未受到地殼物質(zhì)明顯的同化混染作用。

圖9 十堰黃龍—方灘地區(qū)輝長巖La/Sm—La圖解(a，據(jù)Geng Hongyan et al., 2009)和Nb/U—Nb圖解 (b，據(jù)Hofmann et al., 1986; 圖例同圖5)Fig. 9 The binary diagram of La/Sm—La and Nb/U—Nb for gabbro from the Huanglong—Fangtan area, Shiyan City (a，after Geng Hongyan et al., 2009; b，after Hofmann et al., 1986; Legends are the same to those inFig. 5)

4.2 巖漿源區(qū)

輝長巖樣品的巖石稀土元素∑LREE/∑HREE和(La/Yb)N顯示輕稀土富集重稀土虧損的特征，具有類似于E—MORB稀土配分曲線。在(Tb/Yb)N—(La/Sm)N圖解上(圖10a)，樣品投影在尖晶石穩(wěn)定域內(nèi)表明其巖漿熔融深度小于80 km。在SiO2—Nb/Y圖解上(圖10b)，樣品均投影在低壓、高度部分熔融的拉斑玄武巖漿區(qū)域，指示巖漿可能經(jīng)過較高程度部分熔融形成。Sm/Yb—Sm圖解顯示樣品源區(qū)具有尖晶石二輝橄欖巖和石榴子石二輝橄欖巖混合特征，巖漿為二者發(fā)生20%～30%的部分熔融形成(圖10c)，結(jié)合圖10b，筆者等認(rèn)為該巖漿為尖晶石二輝橄欖巖低壓、中等程度部分熔融形成。在Th/Yb—Nb/Yb圖解上(圖10d)，樣品主要分布在E—MORB序列附近，表明巖漿源區(qū)來自于虧損地幔部分熔融，并受富集地幔組分影響(Pearce et al., 1984；Choe et al., 2007)。Nie Hu等(2016)報(bào)道的武當(dāng)山南部發(fā)育的中生代鎂鐵質(zhì)巖與本文測試樣品具有相似特征，但其巖漿源區(qū)來源于以尖晶石二輝橄欖巖部分熔融為主，且主要來源于虧損地幔端元，富集地幔組分影響較少?？傮w來講，三組樣品體現(xiàn)出自南向北，受富集地幔組分影響越來越大趨勢特征。

圖10 十堰黃龍—方灘地區(qū)輝長巖源區(qū)(Tb/Yb)N —(La/Sm)N , SiO2—Nb/Y, Sm/Yb—Sm和Th/Yb — Nb/Yb判別圖解 (a，據(jù)Furman et al., 2004; b，據(jù)Greenough et al., 2005; c，據(jù)Aldanmaz et al., 2000; d，據(jù)Pearce, 2008修改；圖例同圖5)Fig. 10 The binary diagrams of(Tb/Yb)N versus(La/Sm)N , SiO2—Nb/Y, Sm/Yb versus Sm and Dy/Yb versus La/Yb for gabbro from the Huanglong—Fangtan area, Shiyan City(a，after Furman et al., 2004; b，after Greenough et al., 2005; c，after Aldanmaz et al., 2000; d，after Pearce, 2008; Legends are the same to those inFig. 5)

鋯石的Hf同位素組成很少受到后期地質(zhì)作用影響，是探討巖漿源區(qū)屬性的重要證據(jù)。本文樣品鋯石同位素εHf(0)和εHf(t)<0，暗示源區(qū)可能是古老地殼或有古老地殼物質(zhì)加入，或者源區(qū)來源于富集巖石圈地幔；樣品兩階段模式年齡更能反映源區(qū)物質(zhì)從虧損地幔被抽取的時(shí)間或源區(qū)物質(zhì)在地殼的平均存留年齡，而巖體結(jié)晶年齡的鋯石Hf兩階段模式年齡(2103～1640 Ma)遠(yuǎn)大于鋯石結(jié)晶年齡(220 Ma)，表明巖漿受到地殼混染或來源于富集地幔(吳福元等，2007)。鋯石的Hf同位素值與前人報(bào)道的十堰—丹江口地區(qū)新元古代武當(dāng)群和耀嶺河群火山巖鋯石Hf同位素組成具有相似性(圖11)，且與其兩階段模式年齡一致(Wang Lijuan et al., 2013)，指示本文輝長巖可能與新元古代火山巖來自同一巖漿源區(qū)。而區(qū)域上武當(dāng)群和耀嶺河群火山巖Nd—Hf同位素反映二者巖石成因可能存在差異，大部分以幔源物質(zhì)占主導(dǎo)，小部分來自地殼物質(zhì)重熔成因(祝禧艷等，2009；Wang Lijuan et al., 2013)。因此本文輝長巖樣品巖漿源區(qū)也可能以幔源物質(zhì)成分為主，而非地殼混染，這與前文全巖地球化學(xué)數(shù)據(jù)特征相吻合。綜上，該套輝長巖的可能來源于源區(qū)發(fā)生了改造的幔源巖漿，為虧損地幔與富集地幔組分混合的源區(qū)性質(zhì)。

圖11 十堰黃龍—方灘地區(qū)輝長巖鋯石εHf(t)與 年齡關(guān)系圖Fig. 11 Plot of εHf(t) and U-Pb age of zircon for gabbro from the Huanglong—Fangtan area, Shiyan City 武當(dāng)群和耀嶺河群火山巖和沉積巖εHf(t)組成區(qū)域據(jù)Wang Lijuan et al., 2013數(shù)據(jù)換算(t=220 Ma) Date εHf(t) of The Wudang Group and The Yaolinghe Group from Wang Lijuan et al, 2013&.(t=220 Ma)

5 討論

秦嶺造山帶經(jīng)歷了新元古代—中生代的俯沖—增生造山、碰撞造山以及陸內(nèi)造山等多個(gè)構(gòu)造演化階段(張國偉等，2001；Ratschbacher et al., 2003; 王宗起等，2009；楊經(jīng)綏等，2010；Bader et al., 2013; Dong Yunpeng et al., 2015; 張國偉等，2019)。以商丹斷裂為界，將秦嶺劃分為南秦嶺和北秦嶺(李春昱等，1978；許志琴等，1988；張國偉，1991)，勉略斷裂帶則將揚(yáng)子板塊與南秦嶺分隔(李春昱等，1978)。王宗起等(2009)將增生造山的理論應(yīng)用于秦嶺造山帶，認(rèn)為勉略帶及附近相關(guān)構(gòu)造—巖石單元為一條增生雜巖帶(王濤等，2011；Yan Zhen et al., 2012；許志琴等，2015)。不同構(gòu)造演化觀點(diǎn)的爭議在于南秦嶺勉略洋盆的性質(zhì)和形成時(shí)限(Wang Gang et al., 2017；王剛等，2019)，然而大量同碰撞和后碰撞花崗巖的發(fā)育(Qin Jiangfeng et al., 2013)和變火山巖記錄的變質(zhì)時(shí)代(李曙光等，1996)等證據(jù)表明勉略洋已于晚三疊世閉合并導(dǎo)致華北板塊與揚(yáng)子板塊全面碰撞，這一觀點(diǎn)在地學(xué)界已達(dá)成共識(shí)(張國偉等，1995；王宗起等，2009；Dong Yunpeng et al., 2011；Li Sanzhong et al., 2018)。

本次研究的輝長巖樣品巖石地球化學(xué)、稀土配分曲線和微量元素蛛網(wǎng)圖顯示樣品具有E—MORB特征，樣品在Nb/U—Nb, Sm/Yb—Sm和Th/Yb—Nb/Yb圖中均投影在MORB附近；在Hf/3—Th—Nb/16判別圖解中大部分落入E—MORB區(qū)域內(nèi)(圖12a)；在Agrawal等(2008)基于已知基性和超基性玄武巖的不活躍微量元素創(chuàng)建的判別圖解中，亦落在MORB區(qū)域(圖12b)。結(jié)合空間展布，與Nie Hu等(2016)報(bào)道的鎂鐵質(zhì)巖共同代表了N—MORB向E—MORB過渡的線性演化特征。

圖12 十堰黃龍—方灘地區(qū)輝長巖Hf/3—Th—Nb/16和DF1—DF2構(gòu)造判別圖解(a，據(jù)Metzger et al., 2002; b，據(jù)Agrawal et al., 2008修改；圖例同圖5)Fig. 12 Plots of Hf/3—Th—Nb/16 and DF1—DF2 for gabbro from the Huanglong—Fangtan area, Shiyan City (a，after Metzger et al., 2002; b，after Agrawal et al., 2008；Legends are the same to those inFig. 5) MORB—洋中脊玄武巖；IAB—島弧玄武巖；OIB—洋島玄武巖；CRB—大陸裂谷玄武巖 MORB—mid-ocean ridge basalt; IAB—island arc basalt; OIB—ocean island basalt; CRB—continental rift basalt; DF1=0.3518ln(La/Th)+0.6013ln(Sm/Th)-1.3450ln(Yb/Th)+2.1056ln(Nb/Th)-5.4763; DF2=-0.3050ln(La/Th)-1.1801ln(Sm/Th)+1.6189ln(Yb/Th)+1.2260ln(Nb/Th)-0.9944

前人研究表明，E—MORB型巖漿主要發(fā)育于大洋中脊及附近的海山(Niu Yaoling et al., 1999；Hemond et al., 2006)、現(xiàn)代大洋弧后盆地也有少量發(fā)育，如Mariana和Lau Basin(Gribble et al., 1996; Hawkins, 2003)，此外匯聚大陸邊緣如環(huán)太平洋造山帶也出現(xiàn)具有E—MORB特征的巖石，主要受洋脊(擴(kuò)張脊)俯沖影響(Cole et al., 2006)，但這些巖石只是具有E—MORB特征，并非真正大洋性質(zhì)巖石。前文述及，印支期勉略洋盆開始關(guān)閉，經(jīng)過俯沖—增生造山過程至晚三疊世閉合，結(jié)合本文巖石成因探討，該套E—MORB型輝長巖樣品以及Nie Hu等(2016)報(bào)道的武當(dāng)山南部發(fā)育的中生代N—MORB鎂鐵質(zhì)巖并非產(chǎn)生于大洋脊環(huán)境，亦不符合弧后擴(kuò)張的構(gòu)造背景。Nie Hu等(2016)將武當(dāng)山南部發(fā)育的中生代鎂鐵質(zhì)巖解釋為勉略洋閉合后由碰撞擠壓轉(zhuǎn)換為伸展的構(gòu)造環(huán)境，這與傳統(tǒng)觀點(diǎn)認(rèn)為武當(dāng)山為前寒武紀(jì)基底，經(jīng)歷了印支期陸內(nèi)構(gòu)造作用的認(rèn)識(shí)較一致。然而，有學(xué)者認(rèn)為武當(dāng)山整體或局部是混雜帶。如周鼎武等(1998)認(rèn)為武當(dāng)群由不同時(shí)代、不同古構(gòu)造環(huán)境的地質(zhì)體以構(gòu)造關(guān)系組合在一起、時(shí)間跨度大的復(fù)雜構(gòu)造組合體；或認(rèn)為兩鄖—隨棗或丹江口—隨州一帶(王荃等，2010)存在俯沖帶和增生混雜帶。近年來，黃龍—方灘地區(qū)先后報(bào)道了中晚泥盆世海相沉積組合與火山物質(zhì)巖片(王剛等，2018)和中二疊世火山作用產(chǎn)物(王剛等，2019)以及大量新元古代不同巖性及成因的塊體(～640 Ma的OIB型輝綠巖塊，沉積時(shí)代晚于～612 Ma的含石英大理巖塊)和碎屑鋯石時(shí)代(最年輕峰值220 Ma；王宗起等?)，表明該地區(qū)存在中生代構(gòu)造混雜巖帶，王東升等(2019)結(jié)合前人大量中生代變質(zhì)和變形年代學(xué)證據(jù)及變質(zhì)溫壓條件認(rèn)為，黃龍地區(qū)巖石為中低級(jí)變質(zhì)且表現(xiàn)出不均衡特征，是受控于該地區(qū)晚古生代—中生代俯沖增生過程。基于上述研究成果，晚古生代—中生代武當(dāng)山可能并非統(tǒng)一結(jié)晶基底，武當(dāng)南緣以及十堰—兩鄖斷裂之間構(gòu)造混雜巖帶的識(shí)別(王宗起等?；湖北省地質(zhì)調(diào)查院?；王剛等，2018，2019；許光等，2018；王東升等，2019)，表明武當(dāng)山內(nèi)部或整體在晚古生代—中生代可能經(jīng)歷了勉略洋盆關(guān)閉導(dǎo)致的俯沖—碰撞造山作用，因此本文樣品形成的構(gòu)造環(huán)境類似于環(huán)太平洋造山帶等匯聚大陸邊緣，并形成了具有E—MORB特征的巖石，且受到勉略洋殼俯沖的影響，為俯沖—碰撞造山階段產(chǎn)物。

6 結(jié)論

(1)十堰黃龍—方灘構(gòu)造混雜帶內(nèi)侵入發(fā)育的輝長巖的SHRIMP鋯石U-Pb年齡為221.2±2.5 Ma，表明其形成于晚三疊世。

(2)該套輝長巖具有輕稀土元素富集重稀土虧損特征，Zr、Hf、Nb等高場強(qiáng)元素豐度為中高等，Rb、Sr等大離子親石元素表現(xiàn)為虧損，結(jié)晶年齡鋯εHf(t)值相對(duì)均一在-13.5至-6.18之間，指示巖漿為尖晶石二輝橄欖巖低壓、中等程度部分熔融形成，來源于虧損地幔和富集組分混合的地幔源區(qū)。

(3)研究區(qū)中生代鎂鐵質(zhì)巖MORB性質(zhì)的巖石形成的構(gòu)造環(huán)境可能類似于匯聚邊緣環(huán)境，且受到勉略洋殼俯沖的影響，為俯沖—碰撞造山階段產(chǎn)物。

致謝:在成文過程中，楊經(jīng)綏院士、陳雷研究員、馮光英副研究員和劉飛博士提出了許多建設(shè)性意見和建議并給予筆者等悉心的幫助，在此表示衷心的感謝!

注 釋／Notes

? 湖北省地質(zhì)礦產(chǎn)局區(qū)域地質(zhì)礦產(chǎn)調(diào)查所. 1985. 竹山幅1∶20萬區(qū)域地質(zhì)調(diào)查報(bào)告. 武漢:湖北地礦局區(qū)域地質(zhì)礦產(chǎn)調(diào)查所.

? 湖北省地質(zhì)礦產(chǎn)局區(qū)域地質(zhì)礦產(chǎn)調(diào)查所. 1990. 黃龍灘幅1∶5萬區(qū)域地質(zhì)調(diào)查報(bào)告. 武漢:湖北地礦局區(qū)域地質(zhì)礦產(chǎn)調(diào)查所.

? 湖北省地質(zhì)調(diào)查院. 2009. 十堰市幅1∶25萬區(qū)域地質(zhì)調(diào)查報(bào)告. 武漢: 湖北省地質(zhì)調(diào)查院.

? 王宗起, 武昱東, 王剛, 張晗, 王濤, 王東升, 賈少華, 張玉濤. 2016. 武當(dāng)—桐柏—大別關(guān)鍵地區(qū)區(qū)域地質(zhì)調(diào)查成果報(bào)告.北京: 中國地質(zhì)科學(xué)院礦產(chǎn)資源研究所.

? 湖北省地質(zhì)調(diào)查院. 2016. 水坪幅、竹山縣幅、蔡家壩幅、峪口幅1∶5萬區(qū)域地質(zhì)礦產(chǎn)調(diào)查報(bào)告. 武漢:湖北省地質(zhì)調(diào)查院.

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