興蒙造山帶前中生代構(gòu)造單元?jiǎng)澐殖跆?

徐備　趙盼　鮑慶中　周永恒　王炎陽　羅志文

1.北京大學(xué)造山帶與地殼演化教育部重點(diǎn)實(shí)驗(yàn)室，北京大學(xué)地球與空間科學(xué)學(xué)院,北京　1008712.沈陽地質(zhì)礦產(chǎn)研究所，沈陽　1100341.

1　引言

興蒙造山帶分布于我國內(nèi)蒙古-東北地區(qū)，是東北亞地區(qū)的重要構(gòu)造單元，前人對(duì)它及其周邊地區(qū)已有許多研究成果。例如李春昱等(1982)討論了我國北方的古板塊構(gòu)造及其與歐亞大陸形成的關(guān)系；任紀(jì)舜等(1980，1990，1999)提出和闡述了古亞洲洋構(gòu)造域、古中華陸塊群、親西伯利亞陸塊群、薩彥-額爾古納造山系和天山-興安造山系以及南蒙古-興安、溫都爾廟和吉黑造山帶等各級(jí)構(gòu)造單元；王鴻禎(1981)劃分了額爾古納早加里東褶皺帶、興安海西褶皺帶、內(nèi)蒙晚加里東褶皺帶和松遼中間地塊，并提出西拉木倫河對(duì)接帶的概念。何國琦和邵濟(jì)安(1983)、唐克東等(1983)、唐克東(1992)和邵濟(jì)安(1991)都對(duì)古亞洲洋演化和東亞陸緣構(gòu)造做了詳細(xì)的分析。Xu and Chen (1993,1997)根據(jù)在蘇尼特左旗的1:5萬填圖提出內(nèi)蒙地區(qū)存在早古生代“雙沖造山帶”的認(rèn)識(shí)。Xiaoetal.(2003，2009)認(rèn)為古亞洲洋南部存在多個(gè)古生代加積楔，大洋俯沖一直持續(xù)到晚古生代末。Li(2006)識(shí)別了額爾古納地塊、南戈壁-扎蘭屯地塊和布列亞-佳木斯古板塊，劃分出溫都爾廟-翁牛特早古生代造山帶和索倫山-吉中晚二疊紀(jì)造山帶。張興洲等(2012)主張布列亞-佳木斯古板塊和華北板塊之間在早石炭世之前就連為一體，之后再與額爾古納-興安地塊(含內(nèi)蒙西部)拼合形成東北亞大陸板塊。王成文等(2009)根據(jù)古生物及地層學(xué)研究提出東北地區(qū)曾存在統(tǒng)一的“佳蒙古陸”，并于晚古生代末或早中生代初沿西拉木倫-長春縫合帶與華北板塊拼合。劉永江等(2010)認(rèn)為古亞洲洋向北側(cè)的“佳蒙地塊”俯沖，導(dǎo)致晚古生代的弧花崗巖以及賀根山洋的開合。Zhouetal.(2011,2012)根據(jù)變質(zhì)表殼巖的廣泛出露，提出東北各地塊500Ma時(shí)形成以孔茲巖系為特征的統(tǒng)一地塊。

近年來更精細(xì)的興蒙造山帶構(gòu)造單元研究集中在東、西部構(gòu)造單元的識(shí)別、造山帶結(jié)構(gòu)以及各塊體之間拼合帶的時(shí)空演化等方面。在東部，東北地塊群的具體組成及其相互之間的關(guān)系是研究和爭(zhēng)議的熱點(diǎn)問題。例如關(guān)于佳木斯地塊與松嫩-張廣才嶺地塊在早古生代拼合(Wangetal.,2012; 許文良等,2012)或是中生代拼合(Wuetal.,2011; Zhouetal.,2012; 邵濟(jì)安和唐克東,1995; 邵濟(jì)安等,2013)，已經(jīng)發(fā)表了不同的觀點(diǎn)；興安地塊是否存在及其與額爾古納地塊拼合帶的位置、時(shí)代和結(jié)構(gòu)等重要問題得到進(jìn)一步研究(葛文春等，2007；張麗等，2013)。在西部，一些學(xué)者繼續(xù)闡述索倫-二道井晚古生代加積楔的概念和古亞洲洋晚古生代閉合的觀點(diǎn)(Xiaoetal.,2009)；而早古生代“雙沖造山帶”的構(gòu)造格局也被進(jìn)一步擴(kuò)展(Xuetal.,2013)。

本文根據(jù)已有同位素年齡、巖石建造、地層和古生物學(xué)等方面的研究成果，結(jié)合筆者對(duì)興蒙造山帶前中生代構(gòu)造演化的認(rèn)識(shí)，初步探討其構(gòu)造單元?jiǎng)澐帧?/p>

圖1　興蒙造山帶構(gòu)造單元?jiǎng)澐諪ig.1　Tectonic unit of the Xing-Meng Orogenic Belt

2　中泥盆世之前的構(gòu)造格局

以前寒武紀(jì)微陸塊為基本劃分單位，以它們之間的縫合帶或斷裂帶為界，將興蒙造山帶中泥盆世之前的構(gòu)造格局劃分為“五塊四帶”(圖1)：從北向南依次為(1)額爾古納地塊；(2)興安地塊；(3)艾力格廟-錫林浩特地塊；(4)松遼-渾善達(dá)克地塊；及(5)佳木斯地塊；它們之間的4條邊界為：(1)新林-喜桂圖縫合帶(XXS)；(2)艾力格廟-錫林浩特-黑河縫合帶(AXHS)；(3)溫都爾廟-吉中-延吉縫合帶(WJYS)和(4)牡丹江縫合帶(MS)。

2.1　額爾古納地塊

Wuetal.(2011)查明塔河-新林一線西北的滿歸和碧水等地的侵入巖具有792～927Ma的鋯石年齡，Wuetal.(2012)對(duì)漠河以南約50km的黑云母斜長片麻巖研究表明其形成于794Ma，通過Hf同位素研究認(rèn)為其原巖的模式年齡為中太古代，反映中太古代地殼熔融結(jié)果。同時(shí)在767Ma和1853Ma之間還存在多個(gè)碎屑鋯石峰值。Zhouetal.(2011a)報(bào)道了石榴石夕線石片麻巖496±3Ma的變質(zhì)年齡和從578±8Ma到1373±17Ma的巖漿事件年齡。Wuetal.(2005)還報(bào)道了該地塊北緣的504±8Ma和517±9Ma的巖漿事件。Tangetal.(2013)報(bào)道了地塊中部約737～851Ma的A型花崗巖、輝長巖和輝長-閃長巖，其εHf(t)=+2.5～+8.1，并指出它們產(chǎn)于與Rodinia超大陸裂解有關(guān)的伸展環(huán)境。張麗等(2013)研究了地塊西緣太平林場(chǎng)花崗片麻巖的時(shí)代，表明存在840～830Ma、800～780Ma和730～720Ma等3期巖漿熱事件。上述特征說明額爾古納地塊具有前寒武紀(jì)基底。

2.2　興安地塊

塔河-新林一線東南的前寒武紀(jì)地層應(yīng)屬興安地塊。孫立新等(2013a)在十七站地區(qū)一帶得到花崗質(zhì)片麻巖的年齡為1854±20Ma，εHf(t)=-8.5～-3.9。本文認(rèn)為應(yīng)代表興安地塊存在的古元古代基底。Miaoetal.(2007)報(bào)道了韓家園子一帶興華渡口群碎屑鋯石最小年齡約為1.0Ga；Zhouetal.(2011b)在韓家園子的興華渡口群夕線石榴片麻巖中識(shí)別了496±3Ma的變質(zhì)年齡，其鋯石核部或碎屑鋯石均具有大于6億年的年齡；李仰春等(2013)報(bào)道扎蘭屯以西40km處銅礦溝銅山組頂部的最年輕鋯石年齡峰值為570±4Ma；周建波等(2014)發(fā)現(xiàn)扎蘭屯以東約40km的向陽嶺地區(qū)興華渡口群中碎屑鋯石最小年齡為481±12Ma，并有大量老于530Ma的碎屑鋯石；這些資料暗示興安地塊北部韓家園子和南部扎蘭屯一帶可能有前寒武紀(jì)基底。

2.3　艾力格廟-錫林浩特地塊

該地塊從艾力格廟向東到蘇尼特左旗和錫林浩特地區(qū)，向西與蒙古境內(nèi)的Hutag Uul地塊相連(Badarchetal.,2002)，向北東是否可與興安地塊相連尚不確定。Yarmolyuketal.(2008)在蒙古境內(nèi)的Totoshan地區(qū)得到片麻狀花崗巖中鋯石的上交點(diǎn)年齡為952±8Ma，代表原巖形成時(shí)代。艾力格廟地區(qū)出露的艾力格廟群由石英巖、片麻巖和花崗片麻巖等組成，從石英巖中獲得最年輕的碎屑鋯石年齡為1151±41Ma(徐備等未發(fā)表數(shù)據(jù))。孫立新等(2013b)在蘇尼特左旗東部發(fā)現(xiàn)了年齡為1516±31Ma和1390±17Ma的花崗片麻巖。葛夢(mèng)春等(2011)報(bào)道了錫林浩特地區(qū)錫林郭勒雜巖中的表殼巖，并從中獲得1005～1026Ma的鋯石變質(zhì)核年齡。上述古老巖石露頭東西向斷續(xù)延伸超過300km，它們代表的前寒武紀(jì)地塊構(gòu)成一個(gè)重要構(gòu)造單元。

2.4　松遼-渾善達(dá)克地塊

該地塊代表早古生代AXHS和WJYS兩條縫合帶之間的穩(wěn)定地區(qū)，東部被松遼盆地、西部被渾善達(dá)克沙地所覆蓋，呈東寬西窄的三角形，林西縣以西到蘇尼特左旗南的西半部分急劇變窄。來自松遼盆地東緣的云母片巖顯示757±9Ma、843±10Ma的最小年齡峰值(Wangetal.,2014; 權(quán)京玉等,2013)；而在南部，裴福萍等(2006)從鉆孔巖心中得到的火山角礫巖和變質(zhì)輝長巖年齡分別為1808±21Ma和1873±13Ma；王穎等(2006)也報(bào)道了變質(zhì)閃長巖SHRIMP鋯石年齡為1839±7Ma，這些數(shù)據(jù)表明松遼地塊應(yīng)存在早前寒武紀(jì)基底。在地塊東緣鐵力地區(qū)，Zhouetal.(2012)報(bào)道了變質(zhì)沉積巖約5～23億年的多組碎屑鋯石。在地塊西部蘇尼特左旗南的渾善達(dá)克沙地北緣，溫都爾廟群絹云石英片巖的碎屑鋯石圖譜出現(xiàn)大量5～22億年的數(shù)據(jù)(徐備等未發(fā)表數(shù)據(jù))，提供了地塊西部可能具有前寒武紀(jì)基底的信息。

2.5　佳木斯地塊

目前的研究多限于南部。Wildeetal.(2001,2003)報(bào)道了地塊南部三道溝及西麻山一帶的麻山群具有約500Ma年齡的麻粒巖相變質(zhì)事件，并根據(jù)大量諧合的鋯石數(shù)據(jù)揭示存在1000～1150Ma的重要物源區(qū)。頡頏強(qiáng)等(2008)報(bào)道了地塊南部穆棱地區(qū)麻山群混合巖中的巖漿型鋯石年齡為843～1004Ma，并認(rèn)為這些數(shù)據(jù)指示了新元古代基底的存在。趙海濱等(2009*趙海濱等.2009.佳木斯地塊SHRIMP鋯石U-Pb年齡的發(fā)現(xiàn)及其地質(zhì)意義.2009年全國巖石學(xué)與地球動(dòng)力學(xué)研討會(huì)論文摘要)在黑龍江省太平溝地區(qū)獲得興東群斜長角閃巖及侵入的花崗片麻巖鋯石SHRIMP年齡分別為913Ma和862Ma。這些研究表明佳木斯地塊存在中-新元古代的基底(Zhou and Wilde,2013)。

2.6　新林-喜桂圖縫合帶(XXS)

該縫合帶南西段喜桂圖地區(qū)的頭道橋藍(lán)片巖早有報(bào)道(張兆忠等，1986)，最近周建波測(cè)定藍(lán)片巖中鋯石年齡500～490Ma(未發(fā)表資料)，給出了縫合帶形成的下限。北東段新林蛇綠巖自下而上主要由變質(zhì)橄欖巖、層狀堆晶巖、輝綠巖席和變玄武巖等組成(李瑞山，1991)。張麗等(2013)發(fā)現(xiàn)太平林場(chǎng)花崗片麻巖中變質(zhì)鋯石年齡為494±10Ma，并通過對(duì)比額爾古納和興安地塊花崗巖Hf同位素特征的不同，揭示了縫合帶兩側(cè)的地球化學(xué)差異。近年來有學(xué)者據(jù)新資料將額爾古納與興安地塊的邊界置于此縫合帶，而不再采用德爾布干斷裂帶作為兩者的分界線(Zhou and Wilde,2013)。

2.7　艾力格廟-錫林浩特-黑河縫合帶(AXHS)

該縫合帶是分隔北部的額爾古納-興安地塊和南部的松遼-渾善達(dá)克地塊的界線，經(jīng)艾力格廟、蘇尼特左旗南、錫林浩特南和大石寨地區(qū)到黑河一線，以沿線分布的的早古生代巖漿巖、混雜巖和磨拉斯盆地為識(shí)別標(biāo)志。該帶以北發(fā)育早古生代島弧巖漿巖帶，呈北東向延綿1500余千米(圖2)。西段位于艾力格廟-錫林浩特地塊的南緣，其發(fā)育時(shí)間約為490～430Ma(Xu and Chen,1997; Chenetal.,2000; Shietal.,2003; 張炯飛等,2004; 石玉若等,2005; Miaoetal.,2007; Jianetal.,2008; 葛夢(mèng)春等,2011)。中段見于大石寨地區(qū)，以基性火山巖為特征，其形成年齡439±3Ma(Guoetal.,2009)。東段多寶山地區(qū)發(fā)育以銅山組細(xì)碧角斑巖為代表的奧陶紀(jì)島弧火山巖(崔革,1983)和多寶山島弧花崗閃長巖(485±8Ma,葛文春等,2007; 480±5Ma,崔根等,2008)。該帶西段在蘇尼特左旗南和艾力格廟地區(qū)，分布著由溫都爾廟群絹云石英片巖為基質(zhì)的混雜巖帶(Xuetal.,2013; 李瑞彪等,2013)。蘇尼特左旗南的色日巴彥敖包組、二連地區(qū)泥鰍河組及科爾沁右翼中旗大民山組出現(xiàn)中上泥盆統(tǒng)紫紅色粗碎屑巖建造及其與下伏地層的不整合關(guān)系，代表造山帶內(nèi)的磨拉斯盆地(圖3b-e)。同時(shí)這條縫合帶也是重要的生物群界線，其北以分布圖瓦貝(Tuvaella)動(dòng)物群為特色，見于多寶山、額爾古納西、伊爾施和東烏珠穆沁旗等地(內(nèi)蒙古自治區(qū)地質(zhì)礦產(chǎn)局，1991)。

2.8　溫都爾廟-吉中-延吉縫合帶(WJYS)

圖2　沿主要縫合線發(fā)育的早古生代巖漿巖、混雜巖帶和磨拉石建造Fig.2　The Early Paleozoic magmatic rocks,ophiolitic mélange and molassic deposition along the main suture zones

這是一條延長1500km以上的早古生代縫合帶，從西向東沿圖古日格-溫都爾廟-正鑲白旗-敖漢旗-吉中-延吉一線分布。西段以發(fā)育混雜巖和藍(lán)片巖為標(biāo)志，如在烏拉特中旗以北的圖古日格、達(dá)爾罕茂明安聯(lián)合旗北的紅旗牧場(chǎng)地區(qū)以及著名的溫都爾廟地區(qū)(唐克東等,1983; 唐克東,1992; 胡驍?shù)?1990; 邵濟(jì)安,1991; Xuetal.,2013; Shietal.,2013)，藍(lán)閃石和多硅白云母所獲39Ar/40Ar年齡為445.6±15Ma，453.2±1.8Ma和449.4±1.8Ma(唐克東,1992; De Jongetal.,2006)?？p合帶以南的華北板塊北緣發(fā)育早古生代島弧火山巖和深成巖帶，從西向東包括圖古日格地區(qū)包爾漢圖群及侵入巖(453～425Ma,Xuetal.,2013)、達(dá)茂旗北部(452～446Ma，張維和簡(jiǎn)平，2008)、溫都爾廟地區(qū)白乃廟群及侵入巖(474～437Ma,Jianetal.,2008; Zhangetal.,2013)、正鑲白旗二長花崗巖(457±11Ma，秦亞等，2013)、敖漢旗地區(qū)八當(dāng)山群火山巖、吉中地區(qū)放牛溝火山巖(黃德薰等，1992；476～444Ma，裴福萍等，2011*裴福萍等.2011.華北克拉通北緣東段早古生代陸緣增生帶：火成巖年代學(xué)與地球化學(xué)證據(jù).2011年全國巖石學(xué)與地球動(dòng)力學(xué)研討會(huì)摘要集)、張家屯英云閃長巖(443±5Ma，裴福萍等，2014)和延吉地區(qū)巖漿巖(裴福萍等未發(fā)表資料)。沿縫合帶發(fā)育晚志留世徐尼烏蘇組復(fù)理石建造和西別河組砂礫巖，不整合覆于奧陶紀(jì)地層或巖漿巖之上(張?jiān)势降龋?010)，代表早古生代造山帶的前陸盆地沉積。

2.9　牡丹江縫合帶(MS)

該縫合帶位于松遼-渾善達(dá)克地塊與佳木斯地塊之間，盡管目前尚缺乏與碰撞有關(guān)的直接證據(jù)，但一些學(xué)者已經(jīng)從巖漿作用和沉積作用方面研究了其形成背景和演化過程。許文良等(2012)指出沿松嫩-張廣才嶺東緣存在南北向展布的早古生代花崗巖，有485Ma、450Ma和425Ma等三個(gè)峰期。Wangetal.(2012)識(shí)別出縫合帶以西存在晚奧陶閃長巖(443～451Ma)、英云閃長巖、流紋巖和中志留世二長花崗巖(424～430Ma)，并據(jù)此提出它們可能代表早古生代佳木斯地塊向西的俯沖。魏連喜等(2013)報(bào)道了晨明地區(qū)花崗閃長巖(433±1Ma)和二長花崗巖(432±2Ma)，認(rèn)為其產(chǎn)生于陸殼加厚環(huán)境，與俯沖后的地殼加厚有關(guān)。Mengetal.(2010)對(duì)松嫩-張廣才嶺地塊湯原地區(qū)和佳木斯地塊寶清地區(qū)下泥盆統(tǒng)碎屑巖的研究也表明，兩個(gè)地塊在413Ma(早泥盆世)之前已經(jīng)拼合。

根據(jù)上述資料，興蒙造山帶各構(gòu)造單元之間及其與華北板塊之間的演化過程有三個(gè)重要事件即：500～490Ma時(shí)期，由額爾古納與興安地塊碰撞形成新林-喜桂圖縫合帶；440～410Ma時(shí)期，由松遼-渾善達(dá)克地塊、華北板塊和佳木斯地塊碰撞形成溫都爾廟-吉中-延吉縫合帶和牡丹江縫合帶；385～375Ma時(shí)期，由松遼-渾善達(dá)克地塊與額爾古納-興安地塊碰撞形成艾力格廟-錫林浩特-黑河縫合帶。這一過程導(dǎo)致古亞洲洋的消失和興蒙造山帶的形成。

圖3　興蒙造山帶泥盆紀(jì)沉積盆地及植物化石分布(a)-中晚泥盆世沉積盆地和古植物化石及賀根山蛇綠巖的分布；(b)-泥鰍河組下部巨厚的磨拉斯沉積；(c)-對(duì)孤山組復(fù)理石地層；(d)-大民山組礫巖；(e)-上泥盆統(tǒng)色日巴彥敖包組礫巖不整合在混雜巖之上；(f)-大民山組植物化石Fig.3　The Devonian sedimentary basins and plant fossils in the Xing-Meng Orogenic Belt(a)-distribution of the Middle-Late Devonian sedimentary basins,plant fossils and Hegenshan ophiolites; (b)-the Niqiuhe Formation molass conglomerate; (c)-the Duigushan Formation flysch; (d)-the Daminshan Formation conglomerate; (e)-the Upper Devonian Seribayanaobao Formation conglomerate overlying mélange; (f)-plant fossil in the Daminshan Formation

3　中泥盆世-石炭紀(jì)(400～300Ma)的構(gòu)造單元

中-晚泥盆世之后，內(nèi)蒙古及東北地區(qū)完成了由古亞洲洋到興蒙造山帶的構(gòu)造格局轉(zhuǎn)變，開始出現(xiàn)多處陸相及海陸交互相沉積，以含植物化石為標(biāo)志。石炭紀(jì)則廣泛分布陸相及濱淺海相碎屑巖和碳酸鹽建造，同時(shí)發(fā)育蛇綠巖、輝長巖、花崗巖及雙峰式火山巖等建造，構(gòu)成多條不同類型的巖漿巖帶。根據(jù)上述基本特征，可劃分陸相盆地、陸表海盆地、蛇綠巖帶、侵入巖帶等構(gòu)造單元。

3.1　中晚泥盆世陸相盆地

此類盆地以含植物化石的中-上泥盆統(tǒng)碎屑巖為標(biāo)志，見于興蒙造山帶西部蘇尼特左旗、中部東烏珠穆沁旗、扎魯特旗、北部海拉爾市、黑河縣及東部延壽縣及密山縣等地。它們雖出露零星，但分布廣泛，具重要的構(gòu)造古地理意義，除前述的色日巴彥敖包組(圖3b)、泥鰍河組(圖3c)、大民山組(圖3d)、那清組之外，還有東烏珠穆沁旗的哈諾敖包組、安格爾音烏拉組、延壽地區(qū)的福興屯組、黑河地區(qū)小河里河組等(圖3a，內(nèi)蒙古自治區(qū)地質(zhì)礦產(chǎn)局，1991；黑龍江省地質(zhì)礦產(chǎn)局，1993)，沉積地層由陸相或海陸交互相礫巖或砂巖組成，含晚泥盆世法門階植物化石(表1)，向上過渡為濱淺海相。例如在伊敏地區(qū)，泥盆系顯示紫紅色復(fù)理石特征(圖3f)。在中段科爾沁右翼中旗以北的造山帶腹地，大民山組砂巖中新發(fā)現(xiàn)了晚泥盆世的植物化石(圖3e，王弢等，2012)。

表1興蒙造山帶內(nèi)晚泥盆世古植物及其分布位置
Table 1Late Devonian plant fossils and their position in the Xing-Meng Orogenic Belt

地區(qū)代表性植物分子地層位置時(shí)代資料來源蘇尼特左旗南①LeptophloeumrhombicumDaw 色日巴彥敖包組晚泥盆世內(nèi)蒙古區(qū)測(cè)一隊(duì)，1965①東烏珠穆沁旗北②Lepidodendropsissp 安格爾音烏拉組晚泥盆世內(nèi)蒙古區(qū)測(cè)一隊(duì)，1973②扎魯特旗北③Archaeocalamitessp 色日巴彥敖包組晚泥盆世?早石炭世王弢等，2012延壽縣馬鞍山④Protoleptidodendronyanshouense福興屯組中泥盆世黑龍江省地質(zhì)礦產(chǎn)局，1993密山縣新中⑤Granulatisporitessp 新中組早泥盆世黑龍江省地質(zhì)礦產(chǎn)局，1993黑河市小河里河⑥Archaeopterissp 小河里河組晚泥盆世黑龍江省地質(zhì)礦產(chǎn)局，1993鄂溫克族自治旗伊敏東⑦Lepidodendropsiscyclostigmatoides對(duì)孤山組晚泥盆世黑龍江地質(zhì)二隊(duì)，1981③海拉爾市大民山⑧未詳細(xì)介紹大民山組晚泥盆世內(nèi)蒙古自治區(qū)地質(zhì)礦產(chǎn)局，1991①②③內(nèi)蒙古自治區(qū)地質(zhì)局第一區(qū)域地質(zhì)測(cè)量隊(duì)(內(nèi)蒙古區(qū)測(cè)一隊(duì))．1965．1 20萬蘇尼特左旗幅區(qū)域地質(zhì)調(diào)查報(bào)告內(nèi)蒙古自治區(qū)地質(zhì)局第一區(qū)域地質(zhì)測(cè)量隊(duì)(內(nèi)蒙古區(qū)測(cè)一隊(duì))．1973．1 20萬東烏珠穆沁旗幅區(qū)域地質(zhì)調(diào)查報(bào)告黑龍江省區(qū)域地質(zhì)調(diào)查第二隊(duì)(黑龍江地質(zhì)二隊(duì))．1981．1 20萬塔爾其幅區(qū)域地質(zhì)調(diào)查報(bào)告

①內(nèi)蒙古自治區(qū)地質(zhì)局第一區(qū)域地質(zhì)測(cè)量隊(duì)(內(nèi)蒙古區(qū)測(cè)一隊(duì))．1965．1∶20萬蘇尼特左旗幅區(qū)域地質(zhì)調(diào)查報(bào)告
②內(nèi)蒙古自治區(qū)地質(zhì)局第一區(qū)域地質(zhì)測(cè)量隊(duì)(內(nèi)蒙古區(qū)測(cè)一隊(duì))．1973．1∶20萬東烏珠穆沁旗幅區(qū)域地質(zhì)調(diào)查報(bào)告
③黑龍江省區(qū)域地質(zhì)調(diào)查第二隊(duì)(黑龍江地質(zhì)二隊(duì))．1981．1∶20萬塔爾其幅區(qū)域地質(zhì)調(diào)查報(bào)告
④內(nèi)蒙古自治區(qū)地質(zhì)調(diào)查院．2004．1∶25萬滿都拉幅區(qū)域地質(zhì)調(diào)查報(bào)告

3.2　石炭紀(jì)陸相及陸表海盆地

早石炭世興蒙造山帶的錫林郭勒盟北部及興安盟西北部普遍隆起，其南發(fā)育陸相及海陸交互相沉積，見于陳巴爾虎旗-喜貴圖旗-額爾古納右旗一帶(如紅水泉組)和敖漢旗北部(如朝吐溝組)，局部含礫巖和火山巖，并含植物化石。陸表海盆地分布于蘇尼特左旗南部、敖漢旗北部、塔河-沐河地區(qū)和吉林省北部，發(fā)育陸緣碎屑沉積建造，含大量腕足及珊瑚類化石，沉積不整合覆蓋于早古生代造山帶之上。晚石炭世興蒙造山帶北部發(fā)育陸相盆地，在二連浩特北-白音烏拉-東烏珠穆沁旗-科爾沁右翼中旗一線，以寶力高廟組陸相沉積-火山巖系為代表，向東北延伸至額爾古納右旗及黑龍江省大部，以類磨拉斯建造不整合超覆在前寒武紀(jì)變質(zhì)基底、早古生代沉積地層及蛇綠巖之上(鮑慶中等，2006)，并出現(xiàn)華夏植物群與安加拉植物群的混生現(xiàn)象(辛后田等，2011)。晚石炭世興蒙造山帶中部則仍發(fā)育陸表海盆地，沉積建造以淺海相碳酸鹽巖和碎屑巖為主(如本巴圖組和阿木山組)，其范圍從烏拉特中旗經(jīng)蘇尼特右旗、西烏旗、烏蘭浩特等地延伸到吉林省北部。在造山帶西緣滿都拉地區(qū)、南緣敖漢旗至吉林南部一線，發(fā)育海陸交互相或陸相盆地，局部出現(xiàn)含煤巖系(如酒局子組)，含華夏植物群化石Calamites(內(nèi)蒙古自治區(qū)地質(zhì)調(diào)查院，2004*內(nèi)蒙古自治區(qū)地質(zhì)調(diào)查院.2004.1:25萬滿都拉幅區(qū)域地質(zhì)調(diào)查報(bào)告)。

晚石炭世盆地內(nèi)火山巖多與局部陸內(nèi)伸展作用有關(guān)，如嫩江地區(qū)寶力高廟組中流紋巖為307±2Ma，大石寨組中晶屑凝灰?guī)r為308±2Ma， 并被認(rèn)為處于陸相伸展背景 (趙芝等，2010a)；曾維順等(2011)獲得大石寨地區(qū)大石寨組火山巖年齡為314±1Ma，據(jù)此提出晚石炭世應(yīng)為裂陷盆地；辛后田等(2011)將東烏珠穆沁旗寶力高廟組厘定為320～303Ma的陸相火山-碎屑巖建造；湯文豪等(2011)在蘇尼特右旗本巴圖組中識(shí)別了313～308Ma的雙峰式火山巖，并認(rèn)為研究區(qū)應(yīng)處于裂谷構(gòu)造環(huán)境。在蒙古南部，Yarmolyuketal.(2008)已報(bào)道同時(shí)代的雙峰式火山巖和堿性花崗巖帶，可向東延入內(nèi)蒙古西部地區(qū)。

總之，石炭紀(jì)地層發(fā)育于更為廣闊的陸相-海陸交互相-濱海相沉積盆地(內(nèi)蒙古自治區(qū)地質(zhì)礦產(chǎn)局，1991；黑龍江省地質(zhì)礦產(chǎn)局，1993)，這類盆地不整合于早古生代造山帶之上，屬上疊型沉積古地理單元(圖4)。

3.3　早石炭世蛇綠巖

見于二連東、賀根山和迪彥廟等地，形成時(shí)代為356～333Ma(Jianetal.,2010; 張志誠、宋述光待發(fā)表資料)。地球化學(xué)分析表明賀根山蛇綠巖形成與軟流圈上涌和巖石圈伸展有關(guān)的構(gòu)造背景(Jianetal.,2010)。需要指出的是，早在晚泥盆世，這些蛇綠巖附近已經(jīng)出現(xiàn)陸相磨拉斯建造，如二連以北的泥鰍河組和蘇左旗、阿巴嘎旗一帶含植物化石的色日巴彥敖包組(圖3)，暗示晚泥盆世之后出現(xiàn)的陸相環(huán)境。因此，區(qū)域地質(zhì)背景限定賀根山等地的早石炭世蛇綠巖應(yīng)發(fā)育在陸殼基底之上，代表造山后的一次伸展過程。

3.4　石炭紀(jì)侵入巖

這類侵入巖呈面狀分布(圖4)，包括花崗巖、花崗閃長巖、輝長巖等，其同位素年代約300～330Ma。例如佘宏全等(2012)報(bào)道了大興安嶺中北段廣布于龍鎮(zhèn)、扎蘭屯以西和原林以西的二長花崗巖、正長花崗巖、石英閃長巖和黑云母花崗巖等多個(gè)巖體。類似的還包括牙克石花崗閃長巖(331±4Ma，趙芝等，2010b)、塔源輝長巖和花崗巖(331～329Ma，馮志強(qiáng)等，2014)、塔河輝長巖(333±8Ma，周長勇等，2005)、內(nèi)蒙東部錫林浩特地區(qū)白音高勒石英閃長巖(313～323Ma，鮑慶中等，2007)、石榴石花崗巖(316±3Ma，施光海等，2003)、內(nèi)蒙蘇尼特左旗巴音寶力道石英閃長巖(309±8Ma,Chenetal.,2000)以及內(nèi)蒙西部四子王旗輝長巖(331±4Ma，周志廣等，2009)等。有些學(xué)者已經(jīng)提出它們產(chǎn)于張性構(gòu)造環(huán)境(鮑慶中等，2007；馮志強(qiáng)等，2014)。根據(jù)本文對(duì)泥盆-石炭紀(jì)古構(gòu)造格局的認(rèn)識(shí)，它們應(yīng)與造山后的伸展作用有關(guān)。

圖4　興蒙造山帶晚古生代巖石-構(gòu)造單元示意圖Fig.4　Late Paleozoic litho-tectonic units of the Xing-Meng Orogenic Belt

4　二疊紀(jì)(300～250Ma)的巖石-構(gòu)造單元

在興蒙造山帶范圍內(nèi)，二疊紀(jì)伸展作用形成了多種巖石-構(gòu)造單元，包括被動(dòng)裂谷帶、主動(dòng)裂谷帶、蛇綠巖帶和堿性巖帶等。

4.1　早-中二疊世被動(dòng)裂谷帶

早-中二疊世陸內(nèi)裂谷建造具有三個(gè)鮮明特點(diǎn)，一是沉積類型多變，同時(shí)期可出現(xiàn)陸相、海相和海陸交互相沉積巖系，二是普遍含植物化石和濱淺海相動(dòng)物化石，暗示沉積基底具有明顯的深度變化、陸相或陸源沉積物豐富和不存在大范圍洋殼；三是具有大量雙峰式火山巖，說明與伸展背景有關(guān)(圖4)。據(jù)此可將這種沉積建造與火山巖建造均發(fā)育的組合歸為被動(dòng)裂谷。

作為該時(shí)期火山巖的典型代表，大石寨組(290～270Ma)火山巖廣泛分布，從西向東見于西部滿都拉、中部林西到東部大石寨等地，構(gòu)成3條火山-沉積巖帶(邵濟(jì)安等，2014)，其中火山巖顯示為雙峰式。例如在滿都拉地區(qū)(圖5)，早二疊世火山巖呈近東西向分布，基性巖見于滿都拉南部呼吉爾特以北和查干哈達(dá)廟，其年齡為279±3Ma和274±1Ma，19個(gè)樣品SiO2為47%～55%(晨辰等，2012)；酸性巖見于行格寶木太以東，8個(gè)樣品SiO2為64%～76%(Jianetal.,2010)。鮑慶中等(2006)報(bào)道了西烏珠穆沁旗大石寨組的雙峰式火山巖并認(rèn)為與裂谷環(huán)境有關(guān)。Zhangetal.(2011)根據(jù)地球化學(xué)研究確定蘇尼特左旗西北部的大石寨組為雙峰式火山巖并具有高鉀鈣堿性巖漿特征。

圖5　索倫山-滿都拉地區(qū)地質(zhì)圖(據(jù)內(nèi)蒙古自治區(qū)區(qū)域地質(zhì)調(diào)查院，2004)Fig.5　Geological map of Suolunshan-Mandula area

沉積環(huán)境分析表明該時(shí)期陸相沉積和海相沉積交替出現(xiàn)，組成同期異相的古地理面貌。例如晚石炭世-早二疊世寶力高廟組、格根敖包組為陸相地層且均含安加拉植物化石(李文國等，1996; Shenetal.,2006)；而吉林北部發(fā)育壽山溝組濱淺海相碎屑-碳酸鹽巖沉積，出現(xiàn)北方冷水型和南方暖水型化石的共生(吉林省地質(zhì)礦產(chǎn)局，1988)。又如內(nèi)蒙古中部早二疊世額里圖組和哲斯組，前者為含植物及淡水動(dòng)物化石的湖湘沉積，后者則為含“哲斯動(dòng)物群”的濱淺海相碳酸鹽-碎屑巖系(內(nèi)蒙古自治區(qū)地質(zhì)礦產(chǎn)局，1991；李文國等，1996)。

值得注意的是，在東烏珠穆沁旗東北滿都胡寶拉格地區(qū)最新發(fā)現(xiàn)早-中二疊世華夏植物群分子(周志廣等，2010)，這不但暗示此時(shí)該區(qū)為陸相沉積，而且證實(shí)了晚石炭世華夏植物群在該區(qū)的衍生(辛后田等，2011)，說明從晚石炭世以來興蒙造山帶北部已經(jīng)出現(xiàn)華夏植物群與安加拉植物群的混生。

4.2　堿性巖帶

已有研究表明，興蒙造山帶內(nèi)發(fā)育南、北兩條二疊紀(jì)堿性巖帶(圖4)。北帶從額爾古納地區(qū)沿中蒙邊界向西到二連浩特北部，由大量早二疊世堿性花崗巖(洪大衛(wèi)等,1994; Wuetal.,2002)和雙峰式火山巖(Zhangetal.,2011)組成。該帶向西延至蒙古國南部，與Yarmolyuketal.(2008)所劃分的裂谷巖漿巖帶連通。南帶位于達(dá)茂旗-溫都爾廟-鑲黃旗一線，已報(bào)道達(dá)茂旗北部花崗巖時(shí)代為270～257Ma(范宏瑞等，2009)；鑲黃旗南部畢力赫鉀長花崗巖時(shí)代為264Ma(路彥明等，2012)；克什克騰旗南部堿性巖時(shí)代為264～263Ma(江小均等，2011)。另外該帶包含大量中二疊世花崗巖、花崗閃長巖及輝長-輝綠巖，共同組成興蒙造山帶南部中二疊世巖漿巖帶(圖4; Liuetal.,2010; 章永梅等,2009; 王子進(jìn)等,2013; Caoetal.,2013)。

4.3　索倫山Ligurian型蛇綠巖

索倫山蛇綠巖沿中蒙邊界線分布，在我國境內(nèi)東西向延伸約百余千米，被夾持于早古生代南造山帶與北造山帶之間的晚石炭世濱海相沉積層序內(nèi)，變形及變質(zhì)程度低，未見蛇綠混雜帶或高壓低溫變質(zhì)帶。筆者的地質(zhì)填圖工作顯示，索倫山地區(qū)的上古生界是一個(gè)總體向北推覆的逆沖體系(圖5)，由石炭紀(jì)本巴圖組濱海相碎屑巖巖片(圖6a)、二疊及滑塌堆積和濁積巖片及蛇綠巖巖片等組成。蛇綠巖巖片有三類：(1)超基性巖巖片，呈黃褐色外表，碳酸鹽化和硅化強(qiáng)烈；(2)玄武巖巖片，見于烏珠爾少布特，具有連續(xù)層序，并常被輝長巖脈所穿插(圖6b)；(3)含放射蟲硅質(zhì)巖巖片，內(nèi)部具連續(xù)層序，有粗砂巖和玄武巖夾層(圖6c)，放射蟲化石的時(shí)代為中二疊世早期(王惠等，2005)。這些巖片與本巴圖組濱海相或晚二疊世濁積巖呈斷層關(guān)系(圖6d)。上述成分、層序和構(gòu)造侵位特征與西阿爾卑斯的Ligurian型蛇綠巖非常相似(Bernoullietal.,2003)，而后者緣于Adriatic-Iberian大陸板塊的伸展作用(Borsietal.,1996)，屬陸緣型蛇綠巖，其構(gòu)造就位與推覆過程有關(guān)而與洋殼俯沖無關(guān)(Dilek,2003; Dilek and Furnes,2011; Furnesetal.,2013)。綜上，索倫山蛇綠巖應(yīng)代表中二疊世的伸展環(huán)境，反映了繼早二疊世大石寨期伸展過程之后的又一次巖漿作用。

圖6　索倫蛇綠巖及其與圍巖關(guān)系(a)-石炭紀(jì)本巴圖組紫紅色厚層粗砂巖；(b)-玄武巖被輝長巖脈所侵入；(c)-硅質(zhì)巖中的砂巖夾層；(d)-蛇綠巖與本巴圖組斷層接觸Fig.6　Suolun ophiolites and relationship with country rocks(a)-the Benbatu Fm.red thick sandstone; (b)-basalt intruded by gabbro vein; (c)-sandstone band in siliceous rock; (d)-fault between the Benbatu Fm.and ophiolite

4.4　晚二疊世主動(dòng)裂谷帶

近年來陸續(xù)發(fā)現(xiàn)興蒙造山帶內(nèi)存在246～260Ma的基性巖層序，例如Miaoetal.(2007)報(bào)道了造山帶西段溫都爾廟附近約260Ma的枕狀玄武巖和林西地區(qū)半拉山256±3Ma的輝長巖；初航等(2013)從溫都爾廟以北烏蘭溝枕狀玄武巖中獲得246～261Ma的鋯石年齡。從已發(fā)表的數(shù)據(jù)看，基性火山巖的地球化學(xué)特征接近E-MORB，并且有向OIB演化的趨勢(shì)(張晉瑞等，2014)；同時(shí)這類基性巖具有較多的繼承性鋯石，其時(shí)代從400Ma到元古代，表明鋯石可能源于陸殼基底或早古生代造山帶的混染(初航等,2013)。王子進(jìn)等(2013)報(bào)道了造山帶東段263～246Ma的鎂鐵質(zhì)侵入巖，指出其原始巖漿在巖漿源區(qū)或巖漿演化過程中遭受了古老陸殼物質(zhì)的混染，并與同時(shí)代的花崗巖組成雙峰式火成巖組合，反映伸展環(huán)境。綜上，在晚二疊世興蒙造山帶已轉(zhuǎn)為陸相為主的背景下，這些以火成巖組合為主的建造可能代表軟流圈上涌形成的主動(dòng)裂谷帶。

綜上所述，二疊紀(jì)時(shí)期興蒙造山帶具有伸展作用多次發(fā)生、伸展構(gòu)造復(fù)雜多樣的特征，這與更大范圍的構(gòu)造背景一致，例如Jahnetal.(2009)在中亞造山帶范圍內(nèi)劃分了3條巨型巖漿巖帶，橫跨新疆、蒙古南部、內(nèi)蒙古和東北地區(qū)，由約300～260Ma的花崗巖及雙峰式火山巖組成，用以描述早-中二疊世廣泛的伸展作用。

5　討論

5.1　放射蟲代表的沉積環(huán)境

該區(qū)一個(gè)值得澄清的問題是放射蟲所代表的古地理環(huán)境。有學(xué)者把興蒙造山帶內(nèi)放射蟲的出現(xiàn)作為二疊紀(jì)古亞洲洋存在的關(guān)鍵性證據(jù)(王玉凈和樊志勇，1997；尚慶華，2004；王惠等，2005)，例如用毛登牧場(chǎng)和哲斯敖包地區(qū)的放射蟲化石推測(cè)內(nèi)蒙古中、東部中二疊世仍存在古亞洲洋。這種認(rèn)識(shí)得到廣泛引用。但最近方俊欽等(2014)在毛登牧場(chǎng)地區(qū)原放射蟲化石賦存層位找到宏體螺類化石，而且《內(nèi)蒙古自治區(qū)地質(zhì)志》(第195頁)早已報(bào)道過毛登牧場(chǎng)下二疊統(tǒng)有Paracalamitessp.,Noeggerathiopsissp.等安哥拉植物群化石(內(nèi)蒙古自治區(qū)地質(zhì)礦產(chǎn)局，1991)。在哲斯敖包地區(qū)，以豐富的腕足、珊瑚和化石為特色的哲斯生物群產(chǎn)于厚層生物碎屑灰?guī)r中，顯然代表生物產(chǎn)率極高的濱海環(huán)境。因此，興蒙造山帶二疊紀(jì)放射蟲化石并非代表深海遠(yuǎn)洋環(huán)境，不能作為早-中二疊世古亞洲洋存在的證據(jù)。在世界范圍內(nèi)，論述放射蟲化石產(chǎn)于濱淺海相的研究實(shí)例屢見不鮮(見方俊欽等,2014的文章及其參考文獻(xiàn))。

5.2　古地磁研究成果的啟示

在研究古亞洲洋閉合、興蒙造山帶形成過程中，華北板塊與古亞洲洋內(nèi)各微板塊的位置關(guān)系顯得尤為重要，一些學(xué)者的研究成果給出了新的啟示。Xuetal.(1997)通過對(duì)俄羅斯赤塔地區(qū)石炭-二疊系地層的古地磁研究，認(rèn)為在石炭-二疊紀(jì)赤塔地區(qū)與華北板塊具有相似的緯度，而距離西伯利亞板塊很遠(yuǎn)。Pruner (1987)通過對(duì)蒙古國中部的古地磁研究，認(rèn)為蒙古國中部地區(qū)在二疊紀(jì)已成為華北板塊一部分。Chenetal.(1997)通過對(duì)東烏旗地區(qū)上石炭統(tǒng)地層的古地磁研究，認(rèn)為晚石炭世烏里雅斯臺(tái)大陸邊緣非常接近華北板塊。李朋武等(2012)對(duì)蘇尼特左旗北部白音烏拉及敖漢旗安慶溝鄉(xiāng)晚石炭世地層的古地磁研究顯示二者具有相似的古地磁方向，據(jù)此認(rèn)為內(nèi)蒙古中部在晚石炭世-早二疊世可能已屬華北地塊。根據(jù)Zhaoetal.(2013)對(duì)內(nèi)蒙古中部地區(qū)泥盆紀(jì)-二疊紀(jì)地層的最新研究，該區(qū)自晚泥盆世之后已與華北板塊處于同一緯度，可能說明二者此時(shí)非常接近。以上古地磁研究結(jié)果說明：華北板塊與古亞洲洋內(nèi)的幾個(gè)陸塊最晚在晚石炭世已成為統(tǒng)一塊體，代表古亞洲洋的閉合。

6　結(jié)論

(1)中泥盆世之前興蒙造山帶的構(gòu)造單元可劃分為“五塊四帶”：從北向南依次為額爾古納地塊、興安地塊、艾力格廟-錫林浩特地塊、松遼-渾善達(dá)克地塊及佳木斯地塊；它們之間的4條邊界為：新林-喜桂圖縫合帶、艾力格廟-錫林浩特-黑河縫合帶、溫都爾廟-吉中-延吉縫合帶和牡丹江縫合帶。

(2)中-晚泥盆世內(nèi)蒙古及東北地區(qū)完成了由古亞洲洋到興蒙造山帶的構(gòu)造格局轉(zhuǎn)變，開始出現(xiàn)多處陸相及海陸交互相沉積。石炭紀(jì)則廣泛分布陸相及濱淺海相碎屑巖和碳酸鹽建造，同時(shí)發(fā)育蛇綠巖、輝長巖、花崗巖及雙峰式火山巖等建造，可劃分陸相盆地、陸表海盆地、蛇綠巖帶、侵入巖帶等構(gòu)造單元。

(3)二疊紀(jì)時(shí)期興蒙造山帶具有伸展作用多次發(fā)生、伸展構(gòu)造復(fù)雜多樣的特征，形成了多種巖石-構(gòu)造單元，包括被動(dòng)裂谷帶、主動(dòng)裂谷帶、索倫山Ligurian型蛇綠巖帶和堿性巖帶等。早-中二疊世沉積類型多變，普遍含植物化石和濱淺海相動(dòng)物化石，有大量雙峰式火山巖，這類沉積建造與火山巖建造均發(fā)育的組合應(yīng)屬被動(dòng)裂谷，而晚二疊世發(fā)育的以火成巖組合為主的建造可稱為主動(dòng)裂谷。

7　結(jié)語

目前關(guān)于興蒙造山帶的研究存在多個(gè)尚待解決的重要問題，例如東部地區(qū)有幾個(gè)地塊？它們之間的構(gòu)造關(guān)系如何？興蒙造山帶東、西部如何對(duì)比與銜接？晚古生代巖漿活動(dòng)的構(gòu)造背景及其意義？古亞洲洋最終閉合的位置、時(shí)代及過程？蒙古-鄂霍茨克洋和古太平洋俯沖過程對(duì)古亞洲洋構(gòu)造域的影響等。顯然，解決這些問題需要進(jìn)行長期的、大量的工作。興蒙造山帶構(gòu)造單元的劃分爭(zhēng)議頗多，雖然本文按照古亞洲洋早古生代閉合、晚古生代伸展的觀點(diǎn)初步建立了興蒙造山帶早、晚古生代的構(gòu)造單元，但限于篇幅，未能對(duì)不同觀點(diǎn)展開討論，對(duì)已有研究資料的閱讀和引用也難免掛一漏萬。另外，雖然本文提出了晚古生代伸展構(gòu)造的類型和實(shí)例，但據(jù)目前的研究程度還不能在興蒙造山帶范圍內(nèi)進(jìn)行完整劃分，也沒有討論伸展作用之后的擠壓過程。

致謝在成文過程中，與任紀(jì)舜、何國琦、邵濟(jì)安、韓寶福、魏春景、宋述光、邵積東、許文良、劉永江、周建波、葛文春、孫立新等同行進(jìn)行了有益的討論，特此致謝！

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