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        哈薩克斯坦Ust-Kamenogorsk地區(qū)額爾齊斯構(gòu)造帶構(gòu)造演化的年代學(xué)制約

        2016-07-27 07:47:40潘成澤邱林董永觀
        西北地質(zhì) 2016年2期

        潘成澤 , 邱林 , 董永觀

        (1 新疆維吾爾自治區(qū)國(guó)家三〇五項(xiàng)目辦公室,新疆 烏魯木齊 830000;2 南京地質(zhì)礦產(chǎn)研究所,江蘇 南京 210016)

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        哈薩克斯坦Ust-Kamenogorsk地區(qū)額爾齊斯構(gòu)造帶構(gòu)造演化的年代學(xué)制約

        潘成澤1, 邱林1, 董永觀2

        (1 新疆維吾爾自治區(qū)國(guó)家三〇五項(xiàng)目辦公室,新疆 烏魯木齊830000;2 南京地質(zhì)礦產(chǎn)研究所,江蘇 南京210016)

        摘要:額爾齊斯構(gòu)造帶呈北西-南東向從西西伯利亞南緣經(jīng)Ust-Kamenogorsk、齋桑進(jìn)入中國(guó)的阿勒泰,向南東方向延伸進(jìn)入蒙古南戈壁地區(qū),全長(zhǎng)超過(guò)2 000km,是中亞造山帶重要的構(gòu)造邊界之一。對(duì)哈薩克斯坦境內(nèi)Ust-Kamenogorsk地區(qū)額爾齊斯構(gòu)造帶的宏觀巖石-構(gòu)造特征和不同巖石類型鋯石U-Pb定年研究表明,Ust-Kamenogorsk地區(qū)的額爾齊斯構(gòu)造帶的強(qiáng)變形片麻巖變質(zhì)時(shí)間發(fā)生在460~400Ma,代表了加里東期的碰撞造山事件。侵入其中的片麻狀花崗巖的結(jié)晶年齡為282Ma,而最晚期切穿構(gòu)造面理的塊狀花崗巖的結(jié)晶年齡為252Ma。結(jié)合前人的研究成果綜合分析,表明額爾齊斯構(gòu)造帶經(jīng)歷了古生代的板塊拼合、二疊紀(jì)的左旋走滑以及三疊紀(jì)西伯利亞地幔柱事件導(dǎo)致的巖漿巖侵入等主要構(gòu)造演化階段。

        關(guān)鍵詞:Ust-Kamenogorsk;額爾齊斯構(gòu)造帶;鋯石U-Pb年齡;構(gòu)造演化階段

        額爾齊斯構(gòu)造帶是阿爾泰南緣最重要的板塊邊界(圖1),其南屬于準(zhǔn)噶爾-哈薩克斯坦板塊,北屬于阿爾泰造山帶(何國(guó)琦等,1990,1996;李天德等,1996,2001)。

        該構(gòu)造帶在哈薩克斯坦境內(nèi)長(zhǎng)千余千米,中國(guó)境內(nèi)約600余千米,向東延伸到蒙古境內(nèi)的南蒙造山帶南帶。額爾齊斯縫合帶演化時(shí)間長(zhǎng), 構(gòu)造極為復(fù)雜,多期構(gòu)造疊加完全改變了早期構(gòu)造面貌。因此要全面研究該構(gòu)造帶的構(gòu)造演化序列,需要從多方面進(jìn)行綜合分析。

        額爾齊斯構(gòu)造帶在哈薩克斯坦境內(nèi)分隔了Kalba-Narym地體和Rudny阿爾泰地體(BUSLOV et al.,2002;ZHANG et al., 2012)(圖2),最寬處可達(dá)到50 km。在構(gòu)造帶內(nèi)發(fā)育各種類型的構(gòu)造巖片,包括來(lái)自2個(gè)地體邊緣的構(gòu)造巖塊。MELNIKOV et al(1997;1998)的研究表明,額爾齊斯構(gòu)造帶在東哈薩克斯坦發(fā)育典型的韌性剪切變形, 礦物拉伸線理、旋轉(zhuǎn)碎斑構(gòu)造等顯示以左行剪切構(gòu)造變形為主,北西—南東方向展布,產(chǎn)狀陡傾。BUSLOV et al(2002)對(duì)構(gòu)造帶進(jìn)行云母Ar-Ar定年分析(圖2),發(fā)現(xiàn)2個(gè)主要的年齡峰期,分別是283~276Ma及273~265Ma。但由于研究區(qū)構(gòu)造-巖漿活動(dòng)強(qiáng)烈且復(fù)雜,加之云母礦物自身封閉溫度的限制,云母Ar-Ar年齡數(shù)據(jù)還不足以對(duì)額爾齊斯構(gòu)造帶的演化過(guò)程做出客觀描述。通過(guò)對(duì)構(gòu)造帶宏觀特征的調(diào)查研究和主要巖石類型的鋯石U-Pb年齡測(cè)定,以期對(duì)Ust-Kamenogorsk地區(qū)額爾齊斯構(gòu)造帶的顯生宙構(gòu)造演化過(guò)程做進(jìn)一步闡釋。

        1Ust-Kamenogorsk地區(qū)額爾齊斯構(gòu)造帶的基本特征

        在Ust-Kamenogorsk地區(qū),額爾齊斯構(gòu)造帶是由一系列的韌性剪切斷裂構(gòu)成的斷裂系統(tǒng)(圖2)。構(gòu)造帶包含4類主要巖石類型:

        第一類是黑云母斜長(zhǎng)片巖及片麻巖類,局部出現(xiàn)混合巖化片麻巖,是前寒武紀(jì)雜巖中所能見到的“最老”的巖石單元。

        巖石呈灰黑色、灰白色,片狀片麻狀構(gòu)造(圖3,圖4A、圖4B),主要礦物包括黑云母、長(zhǎng)石(斜長(zhǎng)石為主,可能有少量的鉀長(zhǎng)石類)、石英。石榴子石少量且分布不均勻,常以條帶狀分布于偉晶巖邊部,可能與局部的巖漿熱液活動(dòng)有關(guān)。

        1.片巖;2.片麻巖、混合巖、片麻狀花崗巖;3塊狀花崗巖;4.塊狀花崗閃長(zhǎng)巖;5.基性巖墻;6.斷層圖2 Ust-Kamenogorsk地區(qū)額爾齊斯構(gòu)造帶地質(zhì)簡(jiǎn)圖(依據(jù)Buslov等2004)Fig.2 Geological map along the Iritish belt in Ust-Kamenogorsk (After Buslov et al.,2004)

        第二類為片麻狀花崗巖,呈巖墻、巖株?duì)钋秩氲胶谠颇感遍L(zhǎng)片巖片麻巖中(圖3),接觸邊界清晰,并與巖體發(fā)生同期韌性變形,形成復(fù)雜的褶皺構(gòu)造。露頭宏觀特征顯示片麻狀花崗巖是黑云母斜長(zhǎng)片(麻)巖部分熔融的產(chǎn)物,巖漿發(fā)生位移的距離有限,與中國(guó)阿勒泰地區(qū)很多片麻狀花崗巖類似。

        第三類是侵入到片麻巖及片麻狀花崗巖中的花崗閃長(zhǎng)巖,塊狀構(gòu)造,未發(fā)生變質(zhì)及變形,局部含有片麻巖團(tuán)塊,其產(chǎn)出特征明確表明花崗閃長(zhǎng)巖侵入是發(fā)生在韌性剪切變形之后(圖3,圖4C、圖4D)。

        第四類是侵入到片麻巖及片麻狀花崗巖中的偉晶巖類,偉晶巖類型單一,主要為白云母長(zhǎng)石偉晶巖,偉晶巖脈寬度一般為0.5~1m,很少超過(guò)1m,延伸3~50m,部分偉晶巖脈發(fā)生強(qiáng)烈變形。偉晶巖組成和出露特征與中國(guó)阿勒泰一帶片麻巖中的偉晶巖非常相似,應(yīng)是變質(zhì)作用的產(chǎn)物。

        2主要巖石類型礦物特征

        黑云母片麻巖(HZK01,82°42′16"E,50°01′14"N):巖石呈灰黑色,片狀構(gòu)造;主要的礦物組成包括黑云母(20%~35%)、斜長(zhǎng)石(20%~30%)、鉀長(zhǎng)石(15%~25%)、石英(30%~45%),局部見少量綠簾石和石榴子石,其中石榴子石以變斑晶形式出現(xiàn)。巖石礦物組合表明其原巖屬于正常沉積巖。

        片麻狀花崗巖(HSK15,82°42′18"E,50°01′16"N)(圖4C):片麻狀構(gòu)造,面理總體展布方向與額爾齊斯構(gòu)造帶一致,構(gòu)造變形復(fù)雜,主要表現(xiàn)為左行韌性剪切構(gòu)造。礦物組成包括黑云母(2%~5%)、角閃石(1%~3%)、斜長(zhǎng)石(30%~40%)、微斜長(zhǎng)石(10%~20%)、石英(25%~35%),副礦物主要有磷灰石、Ti-Fe氧化物、鋯石等。巖石露頭構(gòu)造變形強(qiáng)烈,但薄片中的礦物卻保留相對(duì)完整,未見明顯的旋轉(zhuǎn)碎斑結(jié)構(gòu),僅石英顆粒顯示波狀消光特征。在區(qū)域上,片麻狀花崗巖大多呈北西向的小巖脈或巖株沿額爾齊斯構(gòu)造帶分布,盡管與圍巖突變接觸,但其面理與圍巖面理一致。由此可以推斷片麻狀花崗巖是同構(gòu)造就位的,屬于構(gòu)造同期花崗巖。

        1.黑云母(斜長(zhǎng))片巖、片麻巖;2.片麻狀花崗巖、混合巖;3.花崗閃長(zhǎng)巖;4.砂巖、粉砂巖;5.逆沖斷層;6.采樣點(diǎn)位置及編號(hào)圖3 Ust-Kamenogorsk南部前寒武系路線地質(zhì)剖面圖Fig.3 Precambrian geological section at the southern margin of the Ust-Kamenogorsk

        圖4 Ust-Kamenogorsk一帶額爾齊斯構(gòu)造帶主要構(gòu)造特征圖Fig.4 Field photos along the Iritish belt in Ust-Kamenogorsk (see details in the text)

        花崗閃長(zhǎng)巖(HSK16,82°42′18"E,50°01′18"N):取樣巖體呈巖株?duì)睿娣e約0.5km2,塊狀構(gòu)造,花崗結(jié)構(gòu),無(wú)變形。主要礦物包括角閃石(15%~25%)、斜長(zhǎng)石(40%~50%)、石英(30%~35%)。另有,少量的黑云母等(<5%),除角閃石有少量被交代現(xiàn)象外,礦物原生結(jié)構(gòu)基本得到完整保留。此類花崗閃長(zhǎng)巖應(yīng)是額爾齊斯構(gòu)造帶穩(wěn)定后的巖漿產(chǎn)物。

        3鋯石特征及測(cè)年結(jié)果

        對(duì)上述黑云母片麻巖、片麻狀花崗巖和花崗閃長(zhǎng)巖進(jìn)行鋯石U-Pb定年分析,以期對(duì)額爾齊斯構(gòu)造帶的構(gòu)造演化提供精確的年代學(xué)約束(表1)。樣品測(cè)試分析由天津地質(zhì)礦產(chǎn)研究所完成,測(cè)試方法見侯可軍等(2009)。

        片麻巖(HSK01):鋯石均無(wú)色透明,從其晶體形態(tài)、結(jié)構(gòu)特征等可分為2組。一組具有明顯的磨圓度,多為長(zhǎng)柱狀,長(zhǎng)度一般為150~250 um,長(zhǎng)短軸之比為2∶1~4∶1,具有顯著的生長(zhǎng)環(huán)帶結(jié)構(gòu)。表明此類鋯石是巖漿成因,并經(jīng)歷了剝蝕、搬運(yùn)和再沉積過(guò)程。另一組鋯石呈不規(guī)則粒狀,部分為短柱狀,無(wú)明顯環(huán)帶結(jié)構(gòu)。從測(cè)試結(jié)果分析,2組鋯石具有顯著的不一致年齡,其中第一組的206Pb/238U年齡為650~850Ma,而第二組鋯石的206Pb/238U年齡為400~460Ma(表1,圖5)。很顯然,第一組年齡代表了源區(qū)的年齡,第二組鋯石年齡則代表了變質(zhì)事件,片麻巖沉積的時(shí)代大致為650~460Ma,為震旦紀(jì)—早古生代早期。早古生代的構(gòu)造事件使沉積巖發(fā)生角閃巖相變質(zhì),這與中國(guó)阿勒泰地區(qū)及蒙古中部地區(qū)部分片麻巖年齡特征一致(陳麗秋等,2012)。

        片麻狀花崗巖(HSK15):鋯石呈柱狀,無(wú)色透明,長(zhǎng)軸一般為150~200 um。在CL圖象及BSE圖象中,鋯石顯示了清晰的震蕩環(huán)帶結(jié)構(gòu),未見繼承性的核;20粒鋯石U含量為53×10-6~380 ×10-6,Th含量為27×10-6~258×10-6,Th/U值為0.40~1.12(表1)。鋯石結(jié)構(gòu)和放射性元素均表明鋯石是巖漿結(jié)晶形成的。20個(gè)測(cè)點(diǎn)具有在誤差范圍內(nèi)一致的206Pb/238U表面年齡,采用算術(shù)平均,獲得的年齡為(281±1.1) Ma,代表了片麻狀花崗巖的結(jié)晶年齡(圖5)。

        花崗閃長(zhǎng)巖(HSK16):鋯石顆粒相對(duì)細(xì)小,一般為100~150 um,少量小于100 um。鋯石無(wú)色透明,具有不規(guī)則的環(huán)帶結(jié)構(gòu),Th/U值為0.2~0.6。16粒鋯石16次分析,U含量為46×10-6~737×10-6,Th含量為25×10-6~277×10-6。從分析結(jié)果看,有2粒鋯石可能為巖漿捕獲鋯石,年齡約320Ma。其余14個(gè)測(cè)點(diǎn)中,有6個(gè)測(cè)點(diǎn)由于誤差較大未納入計(jì)算,其他8個(gè)測(cè)點(diǎn)在誤差范圍內(nèi)有一致的206Pb/238U年齡,其算術(shù)平均值為(252.4±2.6) Ma(圖5),可以代表花崗閃長(zhǎng)巖的結(jié)晶年齡。

        表1 Ust-Kamenogorsk地區(qū)額爾齊斯構(gòu)造帶中不同巖石類型鋯石LA-ICPMS U-Pb定年結(jié)果表

        續(xù)表1

        樣品編號(hào)Th*U*Th/U206Pb/238U1σ207Pb/235U1σ207Pb/206Pb1σ206Pb/238U年齡(Ma)1σ207Pb/235U年齡(Ma)1σHSK011014880.150.064860.49680.02110.05560.00234054435461126580.450.076470.60020.03060.05660.00284754474551229570.510.077360.61010.03260.05720.00304804500581350990.500.077660.61210.02230.05720.002148245004014771550.500.067350.52080.01430.05610.00154203458301526670.390.070160.54810.03020.05670.00324374481621639890.440.073170.57970.02400.05750.00244555510461736900.390.1197121.05550.02740.06400.00167297740261849411.200.1097100.95250.05340.06300.00356716707581942740.570.067860.51830.02640.05540.00284234429552018570.320.072460.56030.03410.05610.003445044586721801890.420.073960.57790.01370.05670.0013459448126221631970.830.067260.52050.01240.05620.00144194460272330630.470.067460.51880.02600.05540.002842144305624981450.670.1376121.28340.02590.06760.001383178572125981450.670.1376121.28390.02590.06770.0013831785821樣品編號(hào)Th*U*Th/U206Pb/238U1σ207Pb/235U1σ207Pb/206Pb1σ206Pb/238U年齡(Ma)1σ207Pb/235U年齡(Ma)1σHSK151741140.650.044840.36130.01650.05850.0026282231314239610.630.045540.33620.02770.05360.00422873294243782020.390.044840.31750.01080.05140.0017282228010457930.610.044840.32340.02280.05240.00362832285205661530.430.044440.36310.01690.05930.00272802314156951960.480.044040.52760.01190.08690.0019278243010773940.780.044040.32180.01710.05300.00282782283158701000.700.044640.33030.01940.05380.0032281229017927530.500.044550.32720.02940.05330.004628132872610572800.200.045240.33180.00950.05330.00152853291811371340.280.044940.33180.01850.05350.0029283329116122583730.690.044130.31620.00760.05200.001227822797131391940.720.044440.47940.01300.07830.002228023981114681630.420.044840.32990.01140.05340.0018282228910151261131.120.045040.32760.01710.05280.00272842288151640750.540.043940.33170.02400.05480.0038277329121171011750.580.044440.31770.01210.05190.002028022801118751590.480.044340.43770.01260.07170.0021279236911

        續(xù)表1

        樣品編號(hào)Th*U*Th/U206Pb/238U1σ207Pb/235U1σ207Pb/206Pb1σ206Pb/238U年齡(Ma)1σ207Pb/235U年齡(Ma)1σHSK1519431080.400.044440.54780.02120.08950.00342803444172043660.650.044140.59310.02890.09760.0047278347323HSK161551860.300.040340.32050.01380.05770.0025255228212225460.530.051050.39150.04340.05570.00583213335373492870.170.040130.29620.00950.05360.00172542263841262270.560.039830.28290.01030.05160.0018252225395441990.220.039440.43040.01410.07920.00232492363126401550.260.040640.29310.01440.05230.00262572261137942850.330.043540.38040.00920.06340.00152753327882777370.380.031740.36230.00700.05560.00132013314691082740.390.040730.29450.00890.05250.0015257226281030860.350.039340.29110.01780.05370.003224932591611321230.260.050140.36530.01460.05290.0021315331613122034020.510.035830.25650.00640.05190.0013227223261334810.420.038340.31840.02490.06040.0047242228122141142710.420.038530.28050.00960.05280.00182442251915752280.330.039530.40360.01160.07400.0020250234410161103460.320.039240.27910.00710.05160.001324822506

        注 :U、Th含量為10-6。

        4討論

        根據(jù)不同巖石類型鋯石U-Pb年齡和鋯石結(jié)構(gòu)特征,可以初步認(rèn)為。①Ust-Kamenogroask一帶前人歸屬于早前寒武紀(jì)的變質(zhì)巖系是新元古代-早古生代早期的沉積產(chǎn)物(Vasyukova等,2011),其巖石類型、變質(zhì)變形、副變質(zhì)礦物組合、鋯石特征及U-Pb年齡等,與中國(guó)阿勒泰地區(qū)的克木其群幾乎一致(楊富全等,2006;XIAO et al. 2008, 2009, 2010)。②變質(zhì)巖系變質(zhì)時(shí)間為加里東期(400~460 Ma),與中國(guó)阿勒泰克木其群變質(zhì)年齡相吻合,充分表明加里東期造山事件在區(qū)域上可能延伸上千千米(WINDLEY et al. 2007; XIAO et al. 2004; METELKIN et al. 2005)。Ust-Kamenogorsk地質(zhì)研究所在該地區(qū)額爾齊斯構(gòu)造帶南部的超高壓-高壓變質(zhì)巖中(榴輝巖),獲得變質(zhì)礦物Ar-Ar年齡為430Ma,也進(jìn)一步佐證了這一點(diǎn)。③280Ma左右的片麻狀花崗巖,是在額爾齊斯構(gòu)造帶發(fā)生左行剪切的構(gòu)造背景下,局部溫壓變化導(dǎo)致部分熔融形成的(胡藹琴等,2006;周剛等,2007)。④250Ma時(shí)期,處于伸展構(gòu)造背景,形成塊狀花崗閃長(zhǎng)巖。

        結(jié)合前人的Ar-Ar年齡結(jié)果,可以確定Ust-Kamenogorsk地區(qū)構(gòu)造熱事件序列。①850Ma~460Ma期間,是以被動(dòng)大陸邊緣沉積組合為特征的沉積巖系形成階段,代表在新元古代晚期—早古生代早期山區(qū)阿爾泰褶皺造山后的又一沉積旋回。厚度巨大的哈巴河群是這一時(shí)期沉積的典型代表,也是Rundy阿爾泰的重要組成部分。②460Ma~400Ma期間,是山區(qū)阿爾泰南緣重要的構(gòu)造演化階段,這一時(shí)期造成了被動(dòng)大陸邊緣的沉積組合發(fā)生全面的褶皺變形和中深程度的變質(zhì)作用,甚至在局部地區(qū)還出現(xiàn)麻粒巖相及榴輝巖相變質(zhì)作用,如在Ust-Kaminogorsk南部地區(qū)412Ma的榴輝巖是這一時(shí)期深俯沖作用的重要證據(jù)。③280~270Ma期間,是另一個(gè)重要的構(gòu)造演化階段,除了左行走滑作用,在額爾齊斯構(gòu)造帶兩側(cè)還發(fā)育了大量的超鎂鐵巖及A型花崗巖(秦克章等,2012),近年來(lái)的研究認(rèn)為,它們可能和塔里木二疊紀(jì)地幔柱有關(guān)(ZHANG et al., 2010; 2013a, 2013b, 2014)。④250Ma左右,走滑構(gòu)造作用結(jié)束,區(qū)域上處于伸展構(gòu)造背景,形成塊狀花崗閃長(zhǎng)巖。這一期的構(gòu)造熱事件,可能受到西伯利亞地幔柱的影響(VASYUKOVA et al., 2011)。

        圖5 Ust-Kamenogorsk南部不同類型巖石鋯石U-Pb年齡諧和圖Fig.5 Zircon U-Pb concordia of the diverse rocksat the Iritish belt in Ust-Kamenogorsk

        5結(jié)論

        根據(jù)野外地質(zhì)調(diào)查和鋯石U-Pb定年,可以得出以下結(jié)論。

        (1)Ust-Kamenogorsk地區(qū)額爾齊斯構(gòu)造帶主要經(jīng)歷了3期構(gòu)造-巖漿-變質(zhì)事件,分別為460~400Ma、280~270Ma和250Ma。

        (2)早期的構(gòu)造熱事件可能代表了Kalba-Narym地體和Rudey-Altai地體的拼合事件,與中國(guó)境內(nèi)的阿勒泰造山帶這一時(shí)期的造山事件相當(dāng)。

        (3)280~270Ma的構(gòu)造熱事件是由于西伯利亞板塊的逆時(shí)針旋轉(zhuǎn)造成額爾齊斯構(gòu)造帶左旋走滑效應(yīng)的結(jié)果。

        (4)250Ma代表了最晚期的巖漿事件,可能是西伯利亞地幔柱在中亞造山帶的巖漿效應(yīng)。

        致謝:感謝審稿人對(duì)本文認(rèn)真細(xì)致的審閱和寶貴意見;感謝國(guó)家三〇五項(xiàng)目“成礦動(dòng)力學(xué)背景和成礦過(guò)程研究”(2011BAB06B03-01)的資助。

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        收稿日期:2015-06-15;修回日期: 2016-1-20

        基金項(xiàng)目:十二五國(guó)家三〇五項(xiàng)目“成礦動(dòng)力學(xué)背景和成礦過(guò)程研究”(2011BAB06B03-01)

        作者簡(jiǎn)介:潘成澤(1964-),男,遼寧寬甸人,地質(zhì)礦產(chǎn)高級(jí)工程師,2005年畢業(yè)于中國(guó)地質(zhì)大學(xué)地質(zhì)工程碩士專業(yè),主要從事地質(zhì)礦產(chǎn)調(diào)查研究和科技管理工作。E-mail:xj305pcz@vip.163.com

        中圖分類號(hào):P597

        文獻(xiàn)標(biāo)志碼:A

        文章編號(hào):1009-6248(2016)02-0189-09

        Tectonic Evolution of the Iritish belt in Ust-Kamenogorsk Area, Kazakhstan: New Geochronological Evidence

        PAN Chengze1, QIU Lin1, DONG Yongguan2

        (1.National 305 Project Office, Urumuqi 830000,Xinjiang, China;2.Nanjing Institute of Geology and Mineral Resources, Nanjing210016,Jiangsu,China)

        Abstract:The Iritish belt, served as one of the most important tectonic boundary in Central Asian Orogenic Belt (CAOB), extends more than 2 000 kilometers from west Siberian, through Ust-Kamenogorsk and Zhaisang Lake in Kazakhstan, Chinese Altai and then into Mogonia. In combination with systematic geochronological data, the detailed field observation along the Iritish belt in Ust-Kamenogorsk have been reported in this paper, aiming to have a better understanding its tectonic evolution process.The data reveals that amphibolite-facies metamorphism of the gneiss in this belt took place during 460~400 Ma, representing the Caledonian orogenic event. The gneissic granitesintruded into the gneiss along the lamellar structure and crystallized at ca.282 Ma, while the massive granodiorites sharply cut across the schistosity, with crystallized age of ca.252 Ma. Based on these observations, the evolution process of the Iritish belt can be divided into three stages at least, i.e., the Caledonian orogenic event (460~400 Ma), the Permian sinistral strike-slip and the Triassic magmatic event possibly related to the Siberia mantle plume.

        Keywords:Ust-Kamenogorsk; Iritish belt; zircon U-Pb age; tectonic evolution

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