楊振宇,袁 偉 ,仝亞博,劉 靜,王 艷

1)中國(guó)地質(zhì)科學(xué)院地質(zhì)力學(xué)研究所,國(guó)土資源部古地磁與古構(gòu)造重建重點(diǎn)實(shí)驗(yàn)室,北京 100081;2)中國(guó)石化石油勘探開(kāi)發(fā)研究院無(wú)錫石油地質(zhì)研究所,江蘇無(wú)錫 214126;3)同濟(jì)大學(xué)海洋與地球科學(xué)學(xué)院,上海 200092;4)江蘇省有色金屬華東地質(zhì)勘查局,江蘇南京 210007

通常地質(zhì)學(xué)家認(rèn)為橫貫中國(guó)中部的昆侖—秦嶺—大別造山帶(或中央造山帶)將中國(guó)大陸分為中國(guó)北方地塊和南方地塊(群),南、北方地塊展示了不同的地層組合(王澤九等,2014)。這些地塊群組成一個(gè)復(fù)合大陸(任紀(jì)舜等,1994,1995),北方地塊又通常被認(rèn)為由中朝(—阿拉善)—塔里木板塊構(gòu)成(李春昱等,1982;王鴻禎,1985),阿拉善地塊作為“地腰”連接著華北和塔里木地塊。許效松等(1996)通過(guò)對(duì)中國(guó)主要陸塊的古地理研究,則將界于古亞洲洋以南與岡瓦納陸塊群之間的特提斯洋盆系統(tǒng)中具特提斯暖水動(dòng)物群和華夏植物群的地塊稱(chēng)之為“泛華夏陸塊群”,該群又被分之為“北方陸塊群”包括華北、朝鮮、阿拉善等地塊,而南方型“泛揚(yáng)子陸塊群”包括揚(yáng)子、華夏、塔里木、柴達(dá)木等地塊,也有稱(chēng)之為“西域地塊”(葛肖虹等,1996),這些地塊的顯著特點(diǎn)是具有晉寧構(gòu)造旋回和揚(yáng)子型南華—震旦系蓋層。與前人的認(rèn)識(shí)基本一致,他們認(rèn)為阿拉善地塊一直是華北的一部分,早古生代至早泥盆世初塔里木陸塊和柴達(dá)木陸塊分別與華北(—阿拉善)陸塊及其所圍繞的微陸塊聚合,形成“北方陸塊群”;Xiao等(2009)總結(jié)了阿拉善地塊與祁連山造山帶的構(gòu)造演化,也提出晚泥盆世阿拉善地塊與祁連山造山帶拼合,構(gòu)成柴達(dá)木—祁連山—阿拉善構(gòu)造體。似乎晚泥盆世華北通過(guò)柴達(dá)木—祁連山—阿拉善構(gòu)造體與塔里木連接構(gòu)成北方陸塊群。顯然,泥盆紀(jì)后阿拉善地塊似乎構(gòu)成了塔里木—柴達(dá)木地塊的一部分,這些地質(zhì)方面的認(rèn)識(shí)還存在差異,使我們對(duì)古生代時(shí)期阿拉善地塊究竟是華北地塊的一部分？還是與塔里木地塊親緣產(chǎn)生疑問(wèn),因?yàn)楣诺卮诺难芯勘砻?晚二疊世時(shí)塔里木地塊已與西伯利亞—哈薩克斯坦板塊碰撞、拼合(Zhao et al.,1990;Enkin et al.,1992),而華北與蒙古碰撞并拼合形成了華北—蒙古聯(lián)合地塊,兩者則遠(yuǎn)離西伯利亞板塊,直至晚侏羅世華北—蒙古聯(lián)合地塊和西伯利亞板塊的古地磁極才趨向一致,形成統(tǒng)一整體(朱日祥等,1998)。

阿拉善地塊前寒武紀(jì)地質(zhì)研究表明,其基底由新太古代迭布斯格巖群下部依肯烏蘇巖組(2700 Ma)和古元古代的巴彥烏拉山巖群(2500—2264 Ma)組成(耿元生等,2007;Dan et al.,2012),并經(jīng)歷了早古生代(480—446 Ma)和晚古生代(281—266 Ma)兩次構(gòu)造熱事件。近年來(lái),在阿拉善北部發(fā)現(xiàn)的多條蛇綠巖帶,恩格爾烏蘇蛇綠巖帶的發(fā)現(xiàn)表明塔里木陸塊和華北陸塊在早古生代也是分離的(王廷印等,1992),詳細(xì)的年代學(xué)研究表明,蛇綠巖的年齡可晚至晚二 疊 世 ((274±3) Ma (MSWD=0.35)和(262±5) Ma(MSWD=1.2),Feng et al.,2013)。阿拉善地塊與華北及塔里木地塊的構(gòu)造關(guān)系長(zhǎng)期受到關(guān)注,但由于騰格里沙漠的覆蓋,阿拉善地塊的構(gòu)造屬性和構(gòu)造演化一直懸而未決,對(duì)其深入研究應(yīng)是理解中國(guó)北方大陸構(gòu)造演化的一個(gè)重要課題。

圖1 中國(guó)大陸(A)及阿拉善地塊東南緣(B)地質(zhì)簡(jiǎn)圖Fig.1 Simplified geological map of China’s mainland(A) and southeastern Alxa Block(B)

1 中—晚泥盆世砂巖碎屑鋯石 U-Pb年齡及Hf同位素結(jié)果

本次研究對(duì)河西走廊帶—阿拉善地塊東部牛首山地區(qū)中—晚泥盆世砂巖中碎屑鋯石開(kāi)展了 U-Pb年代學(xué)與Hf同位素的詳細(xì)研究(Yuan et al.,2014a)(圖1),鋯石U-Pb年齡譜主要集中在0.4—0.7 Ga、1.0—1.3 Ga、1.5—1.8 Ga、2.4—2.7 Ga 和＞3.0 Ga五個(gè)年齡區(qū)間(圖2d,g)。研究表明華北板塊西部前寒武紀(jì)—晚中生代地層中碎屑鋯石 U-Pb年齡譜,主要集中在1.8—2.1 Ga和2.4—2.7 Ga(圖2e)。而本次研究中獲得牛首山地區(qū)明顯有別于華北的鋯石年齡譜,其年齡譜中并未出現(xiàn)華北板塊典型的 1.85—2.1 Ga峰值。鄂爾多斯盆地西北部桌子山地區(qū)的新元古代—早古生代沉積巖中碎屑鋯石 U-Pb年齡譜存在1.85—2.1 Ga和2.4—2.6 Ga兩個(gè)明顯峰值(圖2f),它具有典型的華北板塊特征。桌子山(華北板塊西緣)與牛首山(阿拉善地塊南緣)相距很近,卻具有截然不同的碎屑物質(zhì)來(lái)源,這也暗示著二者的古地理位置可能是彼此分開(kāi)。

目前 Gondwana大陸各主要板塊均有碎屑鋯石U-Pb年齡峰值為～2.5 Ga的報(bào)道,但是單從U-Pb年齡的峰值已經(jīng)很難判斷碎屑物質(zhì)的來(lái)源。而鋯石Hf同位素?cái)?shù)據(jù)則被認(rèn)為是判斷碎屑物源的一個(gè)很好的輔助工具(Hoskin et al.,2000;Fedo et al.,2003)。阿拉善地塊東部牛首山地區(qū)中—晚泥盆世砂巖中的～2.5 Ga碎屑鋯石Hf同位素研究結(jié)果表明,其εHf(t)值在+4.9 ～ –23.7之間,對(duì)應(yīng)的地殼模式年齡分布在2689—4501 Ma,其峰值為3010 Ma。然而,目前報(bào)道的華北板塊峰值在～2.5 Ga的鋯石對(duì)應(yīng)的Hf同位素模式年齡峰值為2.75 Ga(Li et al.,2007;Jiang et al.,2010;Diwu et al.,2011;Wan et al.,2011a,b;Wang et al.,2011),二者存在明顯的差別。此外,牛首山地區(qū)＞3.0 Ga碎屑鋯石的 Hf同位素特征也明顯區(qū)別于華北板塊同時(shí)代碎屑鋯石,這些特征說(shuō)明牛首山地區(qū)中—上泥盆統(tǒng)的碎屑物源很可能不是來(lái)自華北地塊,這些結(jié)果暗示河西走廊—阿拉善地塊與華北板塊的拼合時(shí)間可能是在晚泥盆世以后。本次研究中牛首山中—上泥盆統(tǒng)出現(xiàn)的典型的格林威爾期碎屑物質(zhì),其U-Pb峰值和Hf同位素特征與華夏地塊古生代地層中碎屑鋯石十分相似(圖2c,d)。古生物研究表明祁連山地區(qū)寒武紀(jì)地層中所產(chǎn)的三葉蟲(chóng)Galahetes,Sanduspis,Huzhuia,Jialaopsis,Szechuanella,Acrocephalina等均為塔里木揚(yáng)子生物地理區(qū)的特有屬種(段吉業(yè)等,2005),與我國(guó)湘西、黔東過(guò)渡相區(qū)及澳大利亞昆士南西北的三葉蟲(chóng)動(dòng)物群有比較密切的關(guān)系(周志強(qiáng)等,1996)。牛首山地區(qū)中寒武統(tǒng)碎屑物質(zhì)來(lái)源與澳大利亞也有一定的親緣性(袁偉等,2012b)。而在本次采樣的牛首山地區(qū),上泥盆統(tǒng)中寧組中發(fā)現(xiàn)的淡水魚(yú)類(lèi)胴甲魚(yú),在華南以及澳大利亞的新南威爾士同時(shí)期地層中均有出現(xiàn)(潘江等,1987;Jia et al.,2010)。并且,中寧組下段地層中發(fā)現(xiàn)了中華豆石介族(介形類(lèi)),該化石以下垂“V”字型肌痕為特征與世界其它地區(qū)地層同期的豆石介族相區(qū)別,其主要產(chǎn)于華南的泥盆紀(jì)地層中(王尚啟等,1995)。這些古生物學(xué)證據(jù)表明寒武紀(jì)—泥盆紀(jì)期間阿拉善地塊與華南同屬一個(gè)生物地理區(qū),它們的地理位置應(yīng)該比較接近。本研究還在牛首山上泥盆系地層中發(fā)現(xiàn)了一顆 U-Pb年齡為(4022±17) Ma的碎屑鋯石,它與西澳的Jack Hills、華南、西藏等地冥古代鋯石沉積物源區(qū)可能具有成因聯(lián)系(袁偉等,2012a)。另外,0.4～0.7 Ga碎屑鋯石的Hf同位素研究顯示,對(duì)于＞550 Ma鋯石的εHf(t)在0.5 ～ –26.0之間(只有一個(gè)正值),代表地殼物質(zhì)的再循環(huán),而＜550 Ma的鋯石εHf(t)開(kāi)始出現(xiàn)了正值,表明開(kāi)始出現(xiàn)新生地殼物質(zhì),標(biāo)志北祁連洋洋殼在 550 Ma開(kāi)始形成,與北祁連造山帶中發(fā)現(xiàn)的蛇綠巖的年代分布(490—550 Ma)相一致(袁偉等,2012b)。

表1 河西走廊—阿拉善地塊與華北板塊晚古生代以來(lái)古地磁極Table 1 Late Paleozoic paleomagnetic data from the Hexi Corridor–Alxa Block and North China Block

2 石炭紀(jì)—二疊紀(jì)古地磁學(xué)研究結(jié)果

本次研究對(duì)河西走廊—阿拉善地塊東部的早石炭世、晚二疊世和早中三疊世地層開(kāi)展詳細(xì)的古地磁研究(Yuan et al.,2014b)。巖石磁學(xué)研究結(jié)果表明,早石炭世灰?guī)r的載磁礦物主要為磁鐵礦和赤鐵礦,可能含有鈦磁鐵礦,磁性礦物多為假單疇顆粒;晚二疊世和早—中三疊世紫紅色長(zhǎng)石石英砂巖主要載磁礦物為赤鐵礦。

早石炭世樣品系統(tǒng)熱退磁共設(shè)12～17步,300℃以下以 50℃為間隔,340～420℃以 30～40℃為間隔,420℃以上以10～20℃為間隔。熱退磁過(guò)程中出現(xiàn)兩個(gè)分量,第一個(gè)分量在 200～300℃時(shí)解阻,為低溫分量;第二個(gè)分量到達(dá) 460℃時(shí)剩磁達(dá)到最小,但是該分量未趨向于原點(diǎn),應(yīng)為中溫分量。460℃以后樣品剩磁過(guò)于微弱,超出了儀器測(cè)試范圍,未能獲得高溫分量。運(yùn)用主向量分析法對(duì)所有樣品退磁結(jié)果進(jìn)行分析(Kirschvink,1980),采點(diǎn)平均采用通用的 Fisher統(tǒng)計(jì)平均法(Fisher,1953),獲得低溫分量A和中溫分量M。其中,低溫分量未能通過(guò)褶皺檢驗(yàn)(McFadden,1990),其方向與現(xiàn)代地磁場(chǎng)一致,很可能是現(xiàn)代地磁場(chǎng)的粘滯剩磁。中溫分量的形成可能與造山熱液流體活動(dòng)有關(guān)(Addison et al.,1985)。研究區(qū)緊鄰祁連造山帶,并且上泥盆世—中石炭世的巖層間斷裂中賦存有熱液型金、銅礦,中石炭世地層局部受到熱液活動(dòng)影響,經(jīng)受不同程度的變質(zhì)作用,變質(zhì)熱液的溫度在 250～300℃(邵潔漣等,1988;宋新華等,2009)。因此,該中溫分量M很可能是熱液流體作用后重磁化的結(jié)果。中溫分量M在 95%置信度下通過(guò)了 Mcfadden褶皺檢驗(yàn)(McFadden,1990),表明該分量為中侏羅世褶皺前獲得。但是其極位置又明顯有別于河西走廊—阿拉善地區(qū)二疊紀(jì)以后的古地磁極,因此我們推測(cè)早石炭世中溫 M 分量重磁化時(shí)間可能在中—晚石炭世,其對(duì)應(yīng)的古地磁極為 λ=12.1°N,Ф=10.7°E,A95=4.2°,古緯度在 3.6±4.2°N。

晚二疊世和早—中三疊世樣品系統(tǒng)熱退磁共設(shè) 14～16步,500℃以下以 80～100℃為間隔,500～600℃以 20～30℃為間隔,600℃以上以 5～20℃為間隔。運(yùn)用主向量分析法對(duì)所有樣品退磁結(jié)果進(jìn)行分析(Kirschvink,1980),采點(diǎn)平均采用通用的Fisher統(tǒng)計(jì)平均法(Fisher,1953)。兩個(gè)時(shí)代的樣品均獲得了低溫和高溫分量,其中低溫分量為現(xiàn)代地磁場(chǎng)的粘滯剩磁;高溫分量均趨向于原點(diǎn),并且通過(guò)了褶皺檢驗(yàn)和區(qū)域一致性檢驗(yàn),代表了原生特征剩磁。晚二疊世對(duì)應(yīng)的古地磁極為λ=26.2°N,Ф=18.0°E,A95=7.5°,古緯度為 17.4±7.5°N;早—中三疊世古地磁極為λ=37.5°N,Ф=14.4°E,A95=3.7°,古緯度為 21.6°N(Liu et al.,2010)。

圖3 阿拉善地塊(藍(lán)色)與華北板塊(紅色)石炭紀(jì)—三疊紀(jì)視極移曲線(xiàn)(據(jù)Yuan et al.,2014b修改)Fig.3 Equal-area projection of Carboniferous-Triassic apparent polar wander paths for the Alxa Block (blue) and North China Block (red) (modified after Yuan et al.,2014b)

圖4 晚二疊世亞洲主要板塊古地理重建圖(據(jù)Yuan et al.,2014b修改)Fig.4 Paleomagnetic-based paleogeographic reconstruction of major Asian blocks in the Late Permian(modified after Yuan et al.,2014b)

通過(guò)系統(tǒng)的古地磁學(xué)研究,我們獲得了阿拉善地塊東部中—晚石炭世、晚二疊世和早—中三疊世可靠的古地磁極,這些數(shù)據(jù)與華北地塊同期的古地磁極有明顯差別(圖3,表1)。河西走廊—阿拉善地塊中東部新獲得的中—晚石炭世、晚二疊世和早—中三疊世構(gòu)成的視極移曲線(xiàn)可以與華北地塊同時(shí)期極移曲線(xiàn)可以進(jìn)行擬合對(duì)比,若以44°N,84°E為參考?xì)W拉極,將阿拉善地塊的視極移曲線(xiàn)旋轉(zhuǎn) 32°,該曲線(xiàn)與華北地塊同時(shí)期極移曲線(xiàn)重合(圖 3),這說(shuō)明了在中三疊世后,特別是印支運(yùn)動(dòng)使阿拉善地塊相對(duì)于華北發(fā)生了 32°的逆時(shí)針旋轉(zhuǎn),正是這一旋轉(zhuǎn)運(yùn)動(dòng)使河西走廊—阿拉善地塊最終與華北地塊拼合形成了統(tǒng)一地塊,該邊界很可能位于賀蘭山與桌子山之間(圖4;中國(guó)地質(zhì)科學(xué)院,2014)。最新的野外地質(zhì)研究表明巴彥烏拉山—狼山存在一條中生代早期線(xiàn)理近水平的韌性剪切帶,很可能代表華北和阿拉善地塊的拼合界線(xiàn)(Zhang et al.,2013)。

3 總結(jié)

阿拉善南緣牛首山地區(qū)的中—晚泥盆世沉積巖中碎屑鋯石的U-Pb年代學(xué)和Hf同位素研究結(jié)果表明,其碎屑物質(zhì)來(lái)源明顯區(qū)別于華北板塊,表明在晚泥盆世時(shí)二者并未相連,彼此的古地理位置還相距較遠(yuǎn)。此時(shí),阿拉善地塊與華南、澳大利亞以及特提斯—喜馬拉雅在碎屑物質(zhì)來(lái)源上更具親緣性(圖2a,b,c,d)。同時(shí),對(duì)阿拉善地塊南緣石炭紀(jì)—三疊紀(jì)沉積巖開(kāi)展系統(tǒng)的古地磁研究結(jié)果表明,阿拉善地塊與華北板塊拼合時(shí)間是在早—中三疊世之后,二者的分界線(xiàn)可能位于賀蘭山與桌子山之間的南北走向的延長(zhǎng)線(xiàn)之上。華北地塊在晚三疊世—中侏羅世發(fā)生了～42°的逆時(shí)針旋轉(zhuǎn),而揚(yáng)子地塊則發(fā)生了～35°順時(shí)針旋轉(zhuǎn);這些相對(duì)旋轉(zhuǎn)作用使得揚(yáng)子地塊與華北地塊完成拼合(Yang et al.,1992)。秦嶺—大別造山帶南緣的勉略蛇綠混雜巖帶,很可能代表了華南地塊與華北地塊最后拼合的結(jié)合帶,勉略洋盆泥盆紀(jì)時(shí)打開(kāi),石炭紀(jì)—二疊紀(jì)是洋盆主體擴(kuò)張期,至三疊紀(jì)逐漸閉合(賴(lài)紹聰?shù)?2003;Lai et al.,2004);晚三疊世由于華北地塊與揚(yáng)子地塊發(fā)生碰撞造山,形成大量印支期鈣堿性同碰撞花崗巖(張國(guó)偉等,2001)。至晚侏羅世,西伯利亞、華北—蒙古聯(lián)合地塊、揚(yáng)子地塊完全拼合,形成了統(tǒng)一的大陸(Enkin et al.,1992;朱日祥等,1998)。

致謝:本研究是《中國(guó)西部大陸新生代構(gòu)造格局與演化》(編號(hào):SinoProbe08-01;201011074)的部分成果,吉林大學(xué)葛肖虹教授審閱了初稿并提出寶貴的修改意見(jiàn);野外工作得到南京大學(xué)李軍鵬、秦永鵬和張海峰等大力協(xié)助,在此深表感謝！

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