張廣才嶺“新元古代”一面坡群的形成時(shí)代：來(lái)自巖漿鋯石和碎屑鋯石U-Pb年齡的制約*

郝文麗　許文良　王楓　唐杰　徐美君　高福紅

1.吉林大學(xué)地球科學(xué)學(xué)院，長(zhǎng)春　1300612.黑龍江省地質(zhì)科學(xué)研究所，哈爾濱　1500361.

1　引言

小興安嶺-張廣才嶺位于興蒙造山帶的東段，古生代期間，該區(qū)經(jīng)歷了多陸塊的拼合與古亞洲洋的演化(Seng?retal.,1993; Li,2006; Lietal.,2009)，這些微陸塊自西至東包括額爾古納地塊、興安地塊、松嫩-張廣才嶺地塊、佳木斯地塊和興凱地塊。近年來(lái)，對(duì)這些微陸塊上存在的前寒武紀(jì)地質(zhì)體的研究取得了新的進(jìn)展，先前確定的絕大多數(shù)“古元古代”或“新元古代”地層已經(jīng)被解體，這不僅包括位于佳木斯地塊上的麻山群(Wildeetal.,2000,2003; Wuetal.,2001)和額爾古納地塊上的興華渡口群(Miaoetal.,2003,2007; Wuetal.,2012)，也包括位于興安地塊上的風(fēng)水溝河群(Xuetal.,2012)和位于松嫩-張廣才嶺地塊上的張廣才嶺群(Wangetal.,2012a,b)和東風(fēng)山群(Wangetal.,2014)，這些所謂的前寒武紀(jì)地質(zhì)體主體上形成于古生代，尤其是晚古生代-早中生代，部分形成于新元古代(Wangetal.,2014)。那么，依據(jù)巖石組合和區(qū)域?qū)Ρ人_定的“新元古代”一面坡群(黑龍江省地質(zhì)礦產(chǎn)局,1993)的形成時(shí)代如何？它是不是代表了該區(qū)的前寒武紀(jì)地質(zhì)體？目前對(duì)于這些問(wèn)題至今沒(méi)有得到回答。鑒于此，本文報(bào)道了一面坡群唐家屯組下部流紋巖和上部長(zhǎng)石石英砂巖、楊木崗組粉砂質(zhì)泥巖和覆蓋其上的中生代太安屯組流紋巖的鋯石U-Pb定年結(jié)果，結(jié)合不同時(shí)代地質(zhì)體之間的覆蓋和穿切關(guān)系，確定了一面坡群的形成時(shí)代與物源，并討論了唐家屯組流紋巖形成的構(gòu)造背景及其區(qū)域構(gòu)造演化意義。

2　地質(zhì)背景與樣品描述

“一面坡群”位于松嫩-張廣才嶺地塊的東南緣，分布在敦化-密山斷裂與伊通-舒蘭斷裂之間，東側(cè)以牡丹江斷裂為界與佳木斯地塊相鄰(圖1a)。該區(qū)出露的地層主要為“新元古代”的一面坡群、晚二疊世的五道嶺組以及中生代太安屯組火山巖和少量新生代的沉積(圖1b)。此外，該區(qū)分布大面積的中生代花崗巖(Wuetal.,2011)和少量的中生代火山巖(唐杰等,2011)。本文研究的一面坡群成殘留孤島狀分布在中生代的花崗巖“海洋”之中(Wuetal.,2011)。

“一面坡群”屬?gòu)垙V才嶺-完達(dá)山地層大區(qū)，該群由黑龍江省區(qū)域地質(zhì)志所創(chuàng)建(黑龍江省地礦局,1993)。“一面坡群”呈近南北向帶狀分布，主要由一套輕微變質(zhì)的火山-沉積巖組成。以尚志市一面坡一帶分布的較有代表性，依據(jù)在一面坡土門(mén)子附近的深灰色粉砂巖中發(fā)現(xiàn)的微體古生物-原始球藻化石，將其劃分為額頭山組和固安屯組，時(shí)代為新元古代(黑龍江省地礦局,1993)。上述劃分與1:20萬(wàn)區(qū)域地質(zhì)調(diào)查(黑龍江省地質(zhì)礦產(chǎn)局,1967,1969)所確定的唐家屯組和楊木崗組相對(duì)應(yīng)，與黑龍江省巖石地層清理(黑龍江省地質(zhì)礦產(chǎn)局,1997)所確定的北寬河組和新興組相對(duì)應(yīng)(表1)。本文使用1:20萬(wàn)區(qū)域地質(zhì)調(diào)查(黑龍江省地質(zhì)礦產(chǎn)局,1967,1969)所確定的地層組進(jìn)行描述。

唐家屯組主要分布在德都縣、北起科洛河南岸，向南經(jīng)庫(kù)依河中、上游兩岸、額頭山、一直延續(xù)到小邊河上游兩岸。在尚志市炮守營(yíng)子、三鍋盔山、五?？h的寶龍殿等有零星分布。該組的巖性主要是灰-灰黑色、淺灰綠色的各種千枚巖、變粒巖、變質(zhì)中酸性火山巖及變質(zhì)酸性凝灰?guī)r。楊木崗組主要分布在尚志市一面坡至三合站一帶及其以南至與吉林省交界地帶，主要巖性為斑點(diǎn)板巖、炭質(zhì)板巖、泥質(zhì)粉砂巖和粉砂質(zhì)泥巖(圖2)。依據(jù)1:20萬(wàn)區(qū)域地質(zhì)調(diào)查資料，前人認(rèn)為唐家屯組與其上覆的楊木崗組為整合接觸，而侏羅紀(jì)太安屯組不整合覆蓋在楊木崗組之上(黑龍江省地質(zhì)礦產(chǎn)局,1967,1969)。本文樣品的具體采樣位置如圖1b和圖2所示，其巖相學(xué)特征如下。

圖1研究區(qū)地質(zhì)簡(jiǎn)圖(a,據(jù)Wuetal.,2007；b,據(jù)黑龍江省地質(zhì)礦產(chǎn)局,1967*黑龍江省地質(zhì)礦產(chǎn)局.1967.1:20萬(wàn)五?？h幅區(qū)域地質(zhì)調(diào)查報(bào)告,1969*黑龍江省地質(zhì)礦產(chǎn)局.1969.1:20萬(wàn)一面坡幅區(qū)域地質(zhì)調(diào)查報(bào)告；花崗巖時(shí)代據(jù)Wuetal.,2011)
Fig.1Simplified geological map of the study area (a,after Wuetal.,2007; Formation time of granitoid is from Wuetal.,2011)

表1黑龍江省一面坡群劃分的歷史沿革
Table 1Stratigraphic division history of the Yimianpo Group in Heilongjiang Province

資料來(lái)源黑龍江省地質(zhì)礦產(chǎn)局(1967，1969)黑龍江省地質(zhì)礦產(chǎn)局(1993)黑龍江省地質(zhì)礦產(chǎn)局(1997)一面坡群(Pt23ym)組名代號(hào)組名代號(hào)組名代號(hào)楊木崗組P11y固安屯組Pt23g新興組(張廣才嶺群)Pt3x唐家屯組P11t額頭山組Pt23e北寬河組(落馬湖群)Pt3∈1b

圖2　“新元古代”一面坡群巖性柱狀圖及采樣位置Fig.2　Column diagram of the “Neoproterozoic” Yimianpo Group showing lithology and sampling locations

樣品號(hào)11HSZ2-1 (1:20萬(wàn)一面坡圖幅)：楊木崗組下段的粉砂質(zhì)泥巖，采自一面坡東南約3km處(E128°06′58.2″，N45°02′50.0″)，該樣品風(fēng)化面為褐色，新鮮面為灰黑色，碎屑結(jié)構(gòu)，塊狀構(gòu)造。主要為石英、長(zhǎng)石組成，鈣質(zhì)膠結(jié)。此粉砂質(zhì)泥巖以捕虜體形式存在于中生代花崗巖內(nèi)(圖3a)。

樣品號(hào)11HSZ3-4 (1:20萬(wàn)五常縣圖幅)：為覆蓋在楊木崗組之上的中生代太安屯組流紋巖，采自扶民村南2km處(E127°55′30.4″，N45°05′21.6″)，該流紋巖呈灰黑色，斑狀結(jié)構(gòu)，塊狀構(gòu)造。斑晶約占30%，主要為石英及堿性長(zhǎng)石，基質(zhì)為隱晶質(zhì)(圖3b)。

樣品號(hào)11HSZ4-3 (1:20萬(wàn)一面坡圖幅)：為唐家屯組底部流紋巖，樣品采自葦河鎮(zhèn)炮守營(yíng)子村西北山腳處(N44°54′54.9″，E128°13′50.8″)，為一面坡群典型剖面，流紋巖呈斑狀結(jié)構(gòu)，塊狀構(gòu)造。斑晶約占15%，斑晶主要為石英及堿性長(zhǎng)石和少量斜長(zhǎng)石(圖3c)。

樣品號(hào)11HSZ5-1 (1:20萬(wàn)一面坡圖幅)：為唐家屯組上部細(xì)粒長(zhǎng)石石英砂巖，采自葦河鎮(zhèn)炮守營(yíng)子村西北山頂(E128°13′28.5″，N44°54′53.6″)，碎屑結(jié)構(gòu)，塊狀構(gòu)造。主要為石英、長(zhǎng)石組成，鈣質(zhì)膠結(jié)(圖3d)。

3　分析方法

本文鋯石U-Pb定年樣品均在河北省廊坊區(qū)域地質(zhì)調(diào)查研究所采用常規(guī)方法進(jìn)行粉碎，并用浮選和電磁選方法進(jìn)行分選，然后在雙目鏡下挑選出不同晶形，顆粒大小、磨蝕程度以及顏色不同的鋯石顆粒，進(jìn)而確保所選鋯石的代表性。在此基礎(chǔ)上，將鋯石粘在雙面膠上，用無(wú)色透明的環(huán)氧樹(shù)脂澆灌固定，待環(huán)氧樹(shù)脂充分固化后拋光，使鋯石暴露出內(nèi)部結(jié)構(gòu)，從而進(jìn)行透射光、反射光和陰極發(fā)光掃描電鏡顯微照像，根據(jù)鋯石陰極發(fā)光(CL)圖像，盡量選擇包裹體較少且吸收程度均勻的區(qū)域進(jìn)行分析測(cè)試。

鋯石U-Pb同位素分析在中國(guó)地質(zhì)大學(xué)地質(zhì)過(guò)程與礦產(chǎn)資源國(guó)家重點(diǎn)室采用標(biāo)準(zhǔn)測(cè)定程序進(jìn)行，使用的ICP-MS為Agilient公司生產(chǎn)的Agilient 7500，激光剝蝕系統(tǒng)為德國(guó)MicroLas公司的GeoLas 200M，該系統(tǒng)由德國(guó)Lambda Physik公司的Compex 102 Excimer激光器(工作物質(zhì)ArF，波長(zhǎng)193nm)與MicroLas公司的光學(xué)系統(tǒng)組成。分析中采用的激光束斑直徑為32μm，以29Si作為內(nèi)標(biāo)，哈佛大學(xué)標(biāo)準(zhǔn)鋯石91500作外標(biāo)校正，詳細(xì)參考值及儀器操作條件及步驟見(jiàn)參考文獻(xiàn)(Liuetal.,2008)。實(shí)驗(yàn)獲得的同位素比值數(shù)據(jù)利用ICPMSDataCal軟件(版本號(hào)：7.0)進(jìn)行處理，具體處理過(guò)程見(jiàn)參考文獻(xiàn)(Liuetal.,2008,2010)，年齡采用ISOPLOT軟件計(jì)算(版本號(hào)3.0)(Ludwigetal.,2003)。實(shí)驗(yàn)獲得的數(shù)據(jù)采用Andersen的方法進(jìn)行同位素比值的校正(Andersen,2002)，以扣除普通Pb的影響。所給定的同位素比值和年齡的誤差(標(biāo)準(zhǔn)誤差)在1σ水平。鋯石的LA-ICP-MS U-Pb分析結(jié)果見(jiàn)表2。

圖3　一面坡群和太安屯組部分樣品的顯微照片(a)-楊木崗組粉砂質(zhì)泥巖；(b)-太安屯組流紋巖；(c)-唐家屯組流紋巖；(d)-唐家屯組長(zhǎng)石石英砂巖.正交偏光.Q-石英;Pl-斜長(zhǎng)石;Af-堿性長(zhǎng)石Fig.3　Photomicrographs of selected samples from the Yimianpo Group and Taiantun Formation(a)-silty mudstone from theYangmugang Formation; (b)-rhyolite from the Taiantun Formation; (c)-rhyolite from the Tangjiatun Formation; (d)-feldspathic quartzose sandstone from the Tangjiatun Formation.Cross-polarized light.Q-quartz; Pl-plagioclase; Af-alkali feldspar

圖4　一面坡群和太安屯組鋯石樣品中的陰極發(fā)光圖像Fig.4　CL images of the selected zircons from the Yimianpo Group and Taiantun Formation in the study area

4　分析結(jié)果

4.1　一面坡群唐家屯組底部流紋巖和頂部長(zhǎng)石石英砂巖

樣品11HSZ4-1，為流紋巖，其中鋯石多為短柱狀-長(zhǎng)柱狀，呈半自形-自形晶，鋯石內(nèi)部結(jié)構(gòu)較清晰，均發(fā)育有典型的巖漿成因的振蕩生長(zhǎng)環(huán)帶(圖4a)。16個(gè)測(cè)點(diǎn)中15個(gè)測(cè)點(diǎn)的206Pb/238U年齡介于289～302Ma之間，其加權(quán)平均值為295±2Ma(n=15)，另一個(gè)測(cè)點(diǎn)的206Pb/238U年齡為428Ma(表2、圖5a)。前者代表了流紋巖的形成時(shí)代，后者應(yīng)為捕獲鋯石的年齡。

表2張廣才嶺“新元古代”一面坡群和太安屯組鋯石LA-ICP-MS U-Pb定年結(jié)果
Table 2LA-ICP-MS zircon U-Pb dating results for the “Neoproterozoic” Yimianpo Group and Mesozoic Taiantun Formation in the Zhangguangcai Range

測(cè)點(diǎn)號(hào)ThU(×10-6)Th/U同位素比值同位素年齡(Ma)207Pb206Pb207Pb235U206Pb238U207Pb206Pb207Pb235U206Pb238U比值1σ比值1σ比值1σ年齡1σ年齡1σ年齡1σ11HSZ2?1粉砂質(zhì)泥巖11HSZ2?1?0110094932 050 051860 002530 300480 015250 042050 000682798626712266411HSZ2?1?02881340 660 064510 005910 362290 029720 041430 0010075913331422262611HSZ2?1?0310519551 100 052030 001830 312570 011010 043280 00050287592769273311HSZ2?1?043169500 330 051110 004420 295430 023710 041770 0011224613326319264711HSZ2?1?052102660 790 053980 004080 442560 033640 059140 0012237013537224370711HSZ2?1?062205060 440 055630 003450 310450 018230 040670 0006643810227514257411HSZ2?1?073784660 810 052250 003570 294350 019630 040690 0005929612626215257411HSZ2?1?081041780 580 050900 004680 309750 028920 043440 0009123617227422274611HSZ2?1?091902830 670 055020 003440 315880 018880 041840 0007841310027915264511HSZ2?1?102254870 460 057320 005310 341100 030990 042910 0009250416429823271611HSZ2?1?111454140 350 051380 002740 306540 017160 042980 000942588827113271611HSZ2?1?1255616700 330 057450 002080 463500 018930 057710 0009636214436018360611HSZ2?1?131843520 520 052840 003700 310990 021770 042830 0007332212927517270411HSZ2?1?143004820 620 064060 004780 359770 025180 041310 0007774311731219261511HSZ2?1?151592810 570 050660 002910 291810 018120 042390 0007222511226014268411HSZ2?1?161522650 570 052970 003900 311270 025920 043240 0010832814427520273711HSZ2?1?171484030 370 052320 003550 251410 018610 035660 0005529914122815226311HSZ2?1?182672681 000 065690 003371 163360 073460 129170 0016479711278434783911HSZ2?1?192995050 590 055520 003030 500910 031170 065760 0009643311341221411611HSZ2?1?20591120 530 058630 005410 609370 053520 078200 0015155316048334485911HSZ2?1?213565910 600 062380 002840 368910 017960 043240 0005527617027017269311HSZ2?1?221011420 710 067470 003500 719550 037380 078990 0013751519549033485911HSZ2?1?232044670 440 060710 002630 484490 022340 057490 0010139516136221357611HSZ3?4流紋巖11HSZ3?4?0160112850 470 052560 001200 216630 004890 029770 00024310361994189211HSZ3?4?022235370 410 050150 001700 202270 007010 029160 00030202611876185211HSZ3?4?031494590 330 050900 002130 210110 008800 029880 00034236751947190211HSZ3?4?041042480 420 048920 004250 196350 016760 029110 0004814419718214185311HSZ3?4?052146670 320 046990 001470 192750 006050 029610 0002849521795188211HSZ3?4?0645310600 430 049000 001400 200470 005600 029610 00026148491865188211HSZ3?4?07602000 300 053670 002970 220290 013150 029760 0005235710320211189311HSZ3?4?082588010 320 052730 001700 210170 006160 029140 00033317461945185211HSZ3?4?091623970 410 050420 002600 208050 010450 029920 000362151201929190211HSZ3?4?102234930 450 055250 002600 227180 009970 029930 0004422742088190211HSZ3?4?112354120 570 048930 001880 200390 007280 029880 00034145641856190211HSZ3?4?121083030 360 050170 003300 201240 012830 029090 0004720315018611185311HSZ3?4?133679540 390 052010 001460 219270 006360 030410 0003286482015193211HSZ3?4?14671190 560 054810 009470 224360 038560 029690 0005440436320632189311HSZ3?4?152434110 590 054720 001960 220290 007860 029180 00027401632027185211HSZ3?4?16912510 360 05150 002620 210660 010630 029990 0004263911949190311HSZ3?4?172346750 350 050220 002190 209410 008910 030240 000272051031937192211HSZ3?4?181484040 370 052280 002110 210380 008510 029270 00031298731947186211HSZ3?4?19941500 720 053470 00290 213900 011770 029420 00053499419710187311HSZ3?4?201033580 750 056730 002050 235650 008740 030180 00038481592157192211HSZ3?4?211092110 390 051490 002620 204980 010020 02920 00036263891898186211HSZ3?4?222074641 010 057350 002080 238130 008840 030180 00038505592177192211HSZ3?4?231143131 410 050740 002230 208140 009150 029920 000362298019281902

續(xù)表2ContinuedTable2測(cè)點(diǎn)號(hào)ThU(×10-6)Th/U同位素比值同位素年齡(Ma)207Pb206Pb207Pb235U206Pb238U207Pb206Pb207Pb235U206Pb238U比值1σ比值1σ比值1σ年齡1σ年齡1σ年齡1σ11HSZ4?1流紋巖11HSZ4?1?014164260 680 059550 002230 567110 021320 068720 000725876345614428411HSZ4?1?02201410520 810 053930 001320 353780 009930 047150 00052368433087297311HSZ4?1?031592421 150 055280 002700 358430 017510 046950 000614248631113296411HSZ4?1?042883360 850 053790 001750 351690 011660 047100 00050362553069297311HSZ4?1?05140012900 920 053690 001360 356400 009160 048000 00062358353107302411HSZ4?1?062453240 650 055900 002390 357630 015090 046930 000724486631011296411HSZ4?1?079026210 170 055800 001570 361260 010150 046760 00044445453138295311HSZ4?1?085585440 600 052740 001690 344970 011140 047130 00045318563018297311HSZ4?1?094973791 230 053990 001690 350150 010100 047190 00051370453058297311HSZ4?1?105445370 690 051110 002250 335330 014840 047270 000602467829411298411HSZ4?1?113064190 700 053440 001690 338980 010530 045860 00051348502968289311HSZ4?1?125284550 640 053880 001480 348550 009750 046570 00045366463047293311HSZ4?1?131812380 760 057380 002100 366940 012870 046440 000515065831710293311HSZ4?1?147719190 840 055310 001420 356730 010040 046470 00059425403108293411HSZ4?1?152082440 850 057710 002250 374480 014420 047120 000555196432311297311HSZ4?1?164414480 990 051070 001780 323430 011510 045790 00051244612859289311HSZ5?1長(zhǎng)石石英砂巖HSZ5?1?011541331 160 053050 002890 357680 01990 049120 0007833197310153095HSZ5?1?027247211 000 053180 001390 341810 009090 046320 000483364229972923HSZ5?1?034692961 580 052520 002060 331680 011970 046160 000513086229192913HSZ5?1?0496710690 900 058220 001630 335090 010540 041250 000475384929382613HSZ5?1?055813891 490 053620 001710 341890 010530 046080 000423555329982903HSZ5?1?063375170 650 052570 003730 297220 020720 041010 00053310164264162593HSZ5?1?074265610 760 056670 001630 323760 009080 041190 000364794628572602HSZ5?1?08164721810 760 052280 001040 301610 008950 041320 000922983226872616HSZ5?1?092262720 830 055110 002890 348680 017920 046180 0008741781304132915HSZ5?1?101762480 710 053510 003190 308320 018750 041380 0008350103273152615HSZ5?1?116083501 740 046940 004170 263370 023090 040690 000646197237192574HSZ5?1?123112691 150 054180 002010 348410 012740 046310 0004937863304102923HSZ5?1?131888680 220 058770 001960 342390 01560 041330 0011155954299122617HSZ5?1?144028840 450 051230 002810 263630 01490 036950 00051251105238122343HSZ5?1?154696440 730 053270 001450 341490 009950 046260 000663404129882924HSZ5?1?161193260 360 055590 001390 353860 009360 046120 00074363330872914HSZ5?1?1759311510 520 051160 002060 289880 011840 041230 000692486325892604HSZ5?1?181963310 590 051750 002170 332870 014870 046150 0005227482292112913HSZ5?1?193732391 560 052390 001730 299820 011510 041180 000803035326692605HSZ5?1?204966440 770 052840 003240 334510 020000 045910 00062322143293152894HSZ5?1?214655340 870 053410 001240 341250 007970 046070 000383463829862902HSZ5?1?2226720 360 046970 004840 261720 026620 040420 0006947216236212554HSZ5?1?2326730 360 051610 00230 327960 014690 046080 0005526881288112903HSZ5?1?24402115632 570 058570 002040 383910 012770 047870 000485515533093013HSZ5?1?253163220 980 051350 001960 294140 01330 041160 0010425759262102606HSZ5?1?261031860 560 051580 002160 329520 015030 046090 0008226772289112905HSZ5?1?272082280 910 056340 004180 345590 027990 046320 00132466129301212928HSZ5?1?282254920 460 055400 002450 356550 018770 046370 0012142871310142927HSZ5?1?297887111 110 051160 003020 268570 015220 03840 00046248109242122433HSZ5?1?301763820 460 055680 001560 354130 010540 046010 000514394630882903HSZ5?1?31772860 270 052930 001830 384030 01420 052370 0007332658330103294

續(xù)表2ContinuedTable2測(cè)點(diǎn)號(hào)ThU(×10-6)Th/U同位素比值同位素年齡(Ma)207Pb206Pb207Pb235U206Pb238U207Pb206Pb207Pb235U206Pb238U比值1σ比值1σ比值1σ年齡1σ年齡1σ年齡1σHSZ5?1?32474310 110 054310 004290 355810 026070 049030 00116384122309203097HSZ5?1?335155530 930 050940 002170 307830 014260 043210 0008323871273112735HSZ5?1?342662880 920 051400 002740 30930 015550 043240 0005325993274122733HSZ5?1?352325330 440 051000 003900 307880 021170 043130 00063241130273162724HSZ5?1?362772761 000 048870 004710 310690 026820 046120 00089141157275212916HSZ5?1?371472410 610 049610 004450 257170 020750 036740 00065177149232172334HSZ5?1?382314980 460 050070 003940 304780 021770 043360 0007198132270172744HSZ5?1?392121841 150 049530 003760 321850 023330 046340 00079173132283182925HSZ5?1?409089670 940 052240 003820 315460 022930 04320 00083296131278182735HSZ5?1?414254670 910 054990 003320 349730 019950 046150 0006412105305152914HSZ5?1?422672081 280 052120 002150 332770 013480 045990 0004729174292102903HSZ5?1?43711340 530 056730 001880 338250 010920 043230 000524815029682733HSZ5?1?441961481 330 054830 002820 350040 018460 046010 0005840596305142904HSZ5?1?456493701 750 057340 002370 325740 012180 041210 000795044928692605HSZ5?1?465224481 160 050240 002670 320490 017160 046160 0006620698282132914HSZ5?1?472503730 670 053020 003980 334610 024320 046040 00068330139293182904HSZ5?1?485676150 920 054210 002260 346770 014720 046060 0005338075302112903HSZ5?1?492335160 450 051840 003250 332930 022520 046270 00104278114292172926HSZ5?1?503942741 440 054340 003240 335950 019010 046060 0008638593294142905HSZ5?1?512524370 580 058160 005150 296290 026190 036830 00092536151264212336HSZ5?1?527274161 750 054260 002450 34250 015110 04610 0006038275299112914HSZ5?1?5311078781 260 052300 002920 266090 014950 036910 0006629896240122344HSZ5?1?545165350 960 052510 002420 332530 015330 046210 0006230881291122914HSZ5?1?553205200 610 055820 003450 39440 024030 051760 00090445105338173256HSZ5?1?569958641 150 054020 002570 34390 016210 046290 0008037275300122925HSZ5?1?575535321 040 063010 002590 451090 018990 051380 0006570968378133234HSZ5?1?584913181 550 065260 003660 46470 025790 052290 0009378387388183296HSZ5?1?5910939151 190 054730 002150 350250 014640 045710 0006940166305112884HSZ5?1?6018949891 910 055510 002540 351690 016000 045530 0005643380306122873HSZ5?1?6166413930 480 055410 002740 289600 016970 037260 0012542973258132368HSZ5?1?627796421 210 055000 005110 277330 025490 036570 00051412212249202323HSZ5?1?636166121 010 057430 002450 360030 014580 045450 0005650867312112873HSZ5?1?643162471 280 054480 005140 344790 031080 046150 00117391158301232917HSZ5?1?654156500 640 054680 003580 349470 023670 046030 00105399111304182906HSZ5?1?6611747831 500 046050 005510 228520 027090 035990 00059238209222284HSZ5?1?6745415620 290 054710 002750 277450 017360 036420 0012440081249142318HSZ5?1?685787990 720 050790 003130 262000 018690 036660 00098231114236152326HSZ5?1?693828140 470 052290 003870 261470 019660 036060 00078298132236162285HSZ5?1?703955310 740 055040 003240 282720 01860 036890 00062414118253152344HSZ5?1?711361970 690 060960 004710 444040 0340 052410 00124638124373243298HSZ5?1?72106023310 450 052400 002020 331680 014740 045950 0013230352291112908

圖5　一面坡群和太安屯組鋯石LA-ICP-MS U-Pb年齡諧和圖Fig.5　U-Pb concordia diagrams summarizing the LA-ICP-MS zircon data for the Yimianpo Group and the Taiantun Formation

樣品11HSZ5-1，為細(xì)粒長(zhǎng)石石英砂巖，其中的鋯石多數(shù)呈長(zhǎng)柱狀，在陰極發(fā)光圖像中多具核邊結(jié)構(gòu)，邊部發(fā)育有明顯的振蕩環(huán)帶(圖4b)。72個(gè)測(cè)點(diǎn)給出的同位素年齡主要介于234～329Ma之間(表2、圖5b)，形成了六組諧和年齡，其206Pb/238U加權(quán)平均年齡自下而上分別為234±3Ma(n=12)、260±2Ma(n=12)、273±3Ma(n=6)、291±1Ma(n=35)，309±8Ma(n=2)、327±4Ma(n=5)。其中最小一組年齡應(yīng)代表了該巖石沉積年齡的下限，即長(zhǎng)石石英砂巖形成于232±3Ma之后。

4.2　楊木崗組下部的粉砂質(zhì)泥巖

樣品11HSZ2-1：為粉砂質(zhì)泥巖，該樣品僅選出23粒鋯石，這些鋯石多數(shù)呈短柱狀的半自形晶，鋯石內(nèi)部結(jié)構(gòu)清晰，均發(fā)育有顯示巖漿成因的振蕩生長(zhǎng)環(huán)帶(圖4c)。23個(gè)測(cè)點(diǎn)的206Pb/238U年齡介于226±3Ma～783±9Ma之間，其中和諧年齡包括：226±3Ma(n=1)、267±3Ma(n=15)、362±7Ma(n=3)、411±6Ma(n=1)、485±12Ma(n=2)和783±9Ma(n=1)(表2、圖5c)。其中最小一組年齡應(yīng)代表了該巖石沉積年齡的下限，即粉砂質(zhì)泥巖形成于226Ma之后。

4.3　中生代太安屯組流紋巖

樣品11HSZ3-4：為太安屯組流紋巖，其中鋯石多為短柱狀-長(zhǎng)柱狀，呈半自形-自形晶，鋯石內(nèi)部結(jié)構(gòu)清晰，均發(fā)育有典型巖漿成因的振蕩生長(zhǎng)環(huán)帶(圖4d)。23個(gè)測(cè)點(diǎn)的206Pb/238U年齡介于185±3Ma～190±2Ma之間，其加權(quán)平均年齡為189±1Ma(MSWD=1.5，n=23)，這表明太安屯組流紋巖形成時(shí)代為早侏羅世(表2、圖5d)。

5　討論

5.1　“新元古代”一面坡群的形成時(shí)代

一面坡群為《黑龍江省區(qū)域地質(zhì)志》于1993年創(chuàng)建(黑龍江省地質(zhì)礦產(chǎn)局，1993)。它是分布在松嫩-張廣才嶺地塊東緣一套淺變質(zhì)巖系，其中以尚志市一面坡一帶分布的一面坡群具代表性，該群自下而上劃分為額頭山組和固安屯組，基于巖石組合和區(qū)域?qū)Ρ葘⑵渲糜谛略糯?。早?0世紀(jì)60年代1:20萬(wàn)區(qū)域地質(zhì)調(diào)查過(guò)程中(黑龍江省地質(zhì)礦產(chǎn)局,1967,1969)，曾將其劃分為下部的唐家屯組和上部的楊木崗組，并將其時(shí)代確定為早二疊世，它們分別對(duì)應(yīng)于地質(zhì)志所劃分的額頭山組和固安屯組，二者為整合接觸。

在一面坡群形成時(shí)代的確定過(guò)程中，主要依據(jù)區(qū)域地層對(duì)比(1:20萬(wàn)區(qū)域地質(zhì)報(bào)告,黑龍江省地質(zhì)礦產(chǎn)局,1967,1969)和所發(fā)現(xiàn)的原始藻類(lèi)的形成時(shí)代(黑龍江省地質(zhì)礦產(chǎn)局，1993)，由于該區(qū)覆蓋嚴(yán)重，以區(qū)域?qū)Ρ鹊脑瓌t進(jìn)行地層時(shí)代的確定依據(jù)不充分。因此，對(duì)一面坡群中火山巖鋯石U-Pb定年是確定該地層形成時(shí)代的關(guān)鍵，同時(shí)可以從一面坡群中碎屑巖中最年輕碎屑鋯石年齡限定其沉積下限，而從上覆地層形成的時(shí)間限定其沉積上限?；谶@一原則，可以看出，1)采自唐家屯組下部流紋巖中鋯石U-Pb定年結(jié)果為295Ma，這表明唐家屯組下部流紋巖形成于早二疊世，而非前人認(rèn)為的“新元古代”(黑龍江省地質(zhì)礦產(chǎn)局，1993)；2)唐家屯組頂部長(zhǎng)石石英砂巖(11HSZ5-1)中最年輕的碎屑鋯石年齡(234Ma)與楊木崗組粉砂質(zhì)泥巖(11HSZ2-1)中最年輕的碎屑鋯石年齡(226Ma)在誤差范圍內(nèi)基本一致，這表明唐家屯組頂部長(zhǎng)石石英砂巖應(yīng)屬于楊木崗組，它們的形成時(shí)代應(yīng)晚于這些最年輕的碎屑鋯石年齡——即晚三疊世，結(jié)合覆蓋其上太安屯組流紋巖的形成時(shí)代(189Ma)，可以判定一面坡群楊木崗組形成于晚三疊世(約226Ma)至早侏羅世(189Ma)之間，而非前人所確定“新元古代”(黑龍江省地質(zhì)礦產(chǎn)局，1993)或早二疊世(1:20萬(wàn)區(qū)域地質(zhì)報(bào)告,黑龍江省地質(zhì)礦產(chǎn)局,1967,1969)。同時(shí)，也暗示唐家屯組與上覆的楊木崗組之間可能為構(gòu)造接觸，而非整合接觸關(guān)系(圖2)。此外，對(duì)于東北地區(qū)地層時(shí)代的確定，尤其是那些缺少生物學(xué)證據(jù)的古生代和前寒武紀(jì)地層，利用區(qū)域?qū)Ρ确椒ㄐ枰稚髦?，在不同地質(zhì)體野外關(guān)系研究的基礎(chǔ)上，應(yīng)加強(qiáng)精確的年代學(xué)研究，進(jìn)而限定這些底層的形成時(shí)代。

5.2　“新元古代”一面坡群楊木崗組的沉積物源

鋯石以高硬度及較高的封閉溫度為特點(diǎn)得以在經(jīng)歷各種地質(zhì)過(guò)程后仍然保持穩(wěn)定的U-Pb同位素體系(Bruguieretal.,1997; Leeetal.,1997; Cherniak and Watson,2000; Ko?ler and Sylvester,2003; Mengetal.,2010; Wangetal.,2012b)。因此，根據(jù)碎屑鋯石的年齡組成和區(qū)域?qū)Ρ龋梢杂脕?lái)判斷地層的沉積物源。

圖6　一面坡群楊木崗組碎屑鋯石年齡頻率圖Fig.6　Relative probability of detrital zircons from the Yangmugang Formation of the Yimianpo Group

從本次楊木崗組碎屑鋯石研究中可以看出，約占92.7%的碎屑鋯石年齡介于226～329Ma之間，呈現(xiàn)出233Ma、260Ma、271Ma、291Ma和327Ma的峰期年齡(表2、圖6)，它們構(gòu)成了一面坡群楊木崗組沉積物源的主體，其中233Ma的年齡與本區(qū)青龍屯組火山巖的形成時(shí)代(～228Ma)相吻合(Xuetal.,2013)，260Ma和271Ma的年齡與松嫩-張廣才嶺地塊東緣以及佳木斯地塊西緣分布的中-晚二疊世花崗巖的形成時(shí)代相近(李錦軼等,1999; Wuetal.,2011; Yuetal.,2013; Caoetal.,2013)，291Ma的年齡與本區(qū)濱東地區(qū)唐家屯組和一面坡群中唐家屯組火山巖的形成時(shí)代(293～295Ma)相吻合(Mengetal.,2011)，327Ma的年齡與東北地區(qū)廣泛報(bào)道的中-晚石炭世(320Ma)的巖漿事件相吻合(Gaoetal.,2007; 趙芝等,2010; Wuetal.,2011)。此外，約有7.3%的碎屑鋯石年齡介于357～783之間(表2)，并且呈現(xiàn)出4個(gè)明顯的年齡組，分別為362Ma、411Ma、485Ma和783Ma(圖6)，其中362Ma的年齡與張廣才嶺南段機(jī)房溝巖群中流紋巖的形成時(shí)代相吻合(本項(xiàng)目組未發(fā)表資料)，411Ma和485Ma的年齡組與松嫩-張廣才嶺地塊東緣近南北向展布的早古生代花崗巖的形成時(shí)代相吻合(劉建峰等,2008; Wangetal.,2012a)，783Ma年齡與松嫩-張廣才嶺地塊東緣東風(fēng)山群和塔東群中部分前寒武紀(jì)地質(zhì)體的時(shí)代相吻合(Wangetal.,2014; Tangetal.,2013)。因此，從上述楊木崗組碎屑鋯石年齡組合與本區(qū)巖漿事件時(shí)間的一致性可以看出，該組沉積時(shí)的物源主要來(lái)源于沉積盆地周邊的晚古生代地質(zhì)體以及次要的早中生代、早古生代和新元古代地質(zhì)體，這也得到了碎屑鋯石近于自形和半自形晶形的支持——即晶形揭示碎屑物經(jīng)歷了較近距離的搬運(yùn)過(guò)程。

5.3　早二疊世唐家屯組流紋巖的形成與區(qū)域構(gòu)造演化

從本文的定年結(jié)果已知，位于尚志附近的一面坡群中唐家屯組主要由流紋巖組成，其形成時(shí)代為早二疊世，這與濱東地區(qū)1:20萬(wàn)區(qū)域地質(zhì)報(bào)告中(黑龍江省地質(zhì)礦產(chǎn)局,1967,1969)確定的唐家屯組典型剖面處的流紋巖和玄武質(zhì)巖石形成時(shí)代類(lèi)似(Mengetal.,2011)，同時(shí)與佳木斯地塊東緣早二疊世二龍山組玄武質(zhì)安山巖的形成時(shí)代相同(Mengetal.,2008)。雖然前人確定唐家屯組中存在安山玢巖，但由于該區(qū)覆蓋嚴(yán)重，野外并沒(méi)有觀察到，故本文并沒(méi)有對(duì)其進(jìn)行研究。本文確定一面坡群中唐家屯組流紋巖的形成時(shí)代為早二疊世，它與濱東地區(qū)唐家屯組典型剖面處同時(shí)代流紋巖和玄武巖以及張廣才嶺北段存在的早二疊世輝長(zhǎng)巖(作者，未發(fā)表資料)一起共同構(gòu)成了典型雙峰式火成巖組合，它們共同揭示了松嫩-張廣才嶺地塊東部在早二疊世處于一種伸展環(huán)境(Mengetal.,2011)，而佳木斯地塊東緣早二疊世鈣堿性火山巖組合揭示了一種活動(dòng)陸緣的構(gòu)造背景(Mengetal.,2008)。結(jié)合大興安嶺地區(qū)早二疊世A型花崗巖帶的出現(xiàn)(洪大衛(wèi)等，1994)以及早二疊世玄武巖的形成(Zhuetal.,2001)，可以判定，松嫩-張廣才嶺地塊與興安地塊一起，在早二疊世期間共同經(jīng)歷了一次區(qū)域性的伸展事件。

6　結(jié)論

通過(guò)對(duì)位于張廣才嶺一面坡群中碎屑鋯石和巖漿鋯石U-Pb年代學(xué)的研究，得出以下幾點(diǎn)結(jié)論：

(1)先前確定的“新元古代”一面坡群實(shí)際上是由早二疊世的唐家屯組流紋巖和早中生代楊木崗組沉積巖所構(gòu)成，而非前人確定的新元古代。

(2)一面坡群楊木崗組的沉積物主要來(lái)源于周邊的晚古生代地質(zhì)體以及次要的早中生代、早古生代和新元古代地質(zhì)體。

(3)早二疊世唐家屯組流紋巖，與區(qū)域早二疊世玄武質(zhì)巖石一起構(gòu)成了典型雙峰式火山巖組合，揭示該區(qū)早二疊世處于一種伸展環(huán)境。

致謝感謝河北省廊坊物探勘察院在鋯石的分選過(guò)程中給予的幫助;同時(shí)感謝中國(guó)地質(zhì)大學(xué)(武漢)地質(zhì)過(guò)程與礦產(chǎn)資源國(guó)家重點(diǎn)實(shí)驗(yàn)室在鋯石LA-ICP-MS U-Pb分析中給予的大力幫助。

Andersen T.2002.Correction of common lead in U-Pb analyses that do not report204Pb.Chemical Geology,192(1-2): 59-79

Bruguier O,Lancelet JR and Malavieille J.1997.U-Pb dating on single detrital zircon grains from the Triassic Songpan-Ganze flysch (central China): Provenance and tectonic correlations.Earth and Planetary Science Letters,152(1-4): 217-231

Bureau of Geology and Mineral Resources of Heilongjiang Province.1993.Regional Geology of Heilongjiang Province.Beijing: Geological Publishing House,1-713 (in Chinese with English abstract)

Bureau of Geology and Mineral Resources of Heilongjiang Province.1997.Stratigraphy of Heilongjiang Province Clearing.Wuhan: China University of Geosciences Press,1-298 (in Chinese)

Cao HH,Xu WL,Pei FP,Wang ZW,Wang F and Wang ZJ.2013.Zircon U-Pb geochronology and petrogenesis of the Late Paleozoic-Early Mesozoic intrusive rocks in the eastern segment of the northern margin of the North China Block.Lithos,170-171: 191-207

Cherniak DJ and Watson EB.2001.Pb diffusion in zircon.Chemical Geology,172(1-2): 5-24

Gao FH,Xu WL,Yang DB,Pei FP,Liu XM and Hu ZC.2007.LA-ICP-MS zircon U-Pb dating from granitoids in southern basement of Songliao basin: Constraints on ages of the basin basement.Science in China (Series D),50(7): 995-1004

Hong DW,Huang HZ,Xiao YJ,Xu MH and Jin MY.1994.The Permian alkaline granites in central Inner Mongolia and their geodynamic significance.Acta Geologica Sinica,68(3): 219-230 (in Chinese)

Ko?ler J and Sylvester PJ.2003.Present trends and the future of zircon in geochronology: Laser ablation ICPMS.Review in Mineralogy and Geochemistry,53(1): 243-275

Lee JKW,Williams IS and Ellis DJ.1997.Pb,U and Th diffusion in natural zircon.Nature,390(6656): 159-162

Li JY,Niu BG,Song Betal.1999.Crustal Formation and Evolution of Northern Changbai Mountains,Northeast China.Beijing: Geological Publishing House,1-136 (in Chinese with English abstract)

Li JY.2006.Permian geodynamic setting of Northeast China and adjacent regions: Closure of the Paleo-Asian Ocean and subduction of the Paleo-Pacific Plate.Journal of Asian Earth Sciences,26(3-4): 207-224

Li WM,Takasu A,Liu YJ,Genser J,Neubauer F and Guo XZ.2009.40Ar/39Ar ages of the high-P/Tmetamorphic rocks of the Heilongjiang Complex in the Jiamusi Massif,northeastern China.Journal of Mineralogical and Petrological Sciences,104: 110-116

Liu JF,Chi XG,Dong CY,Zhao Z,Li GR and Zhao YD.2008.Discovery of Early Paleozoic granites in the eastern Xiao Hinggan Mountains,northeastern China and their tectonic significance.Geological Bulletin of China,27(4): 534-544 (in Chinese with English abstract)

Liu YS,Hu ZC,Gao S,Günther D,Xu J,Gao CG and Chen HH.2008.In situ analysis of major and trace elements of anhydrous minerals by LA-ICP-MS without applying an internal standard.Chemical Geology,257(1-2): 34-43

Liu YS,Gao S,Hu ZC,Gao CG,Zong KQ and Wang DB.2010.Continental and oceanic crust recycling-induced melt-peridotite interactions in the Trans-North China Orogen: U-Pb dating,Hf isotopes and trace elements in zircons of mantle xenoliths.Journal of Petrology,51(1-2): 537-571

Ludwig KR.2003.User’s manual for Isoplot 3.00: A geochronological toolkit for Microsoft Excel.Berkeley Geochronology Centre,Special Publication,4: 74

Miao LC,Fan WM,Zhang FQ,Liu DY,Jian P,Shi GH,Tao H and Shi YR.2004.Zircon SHRIMP geochronology of the Xinkailing-Kele complex in the northwestern Lesser Xing’an Range,and its geological implications.Chinese Science Bulletin,49(2): 201-209

Miao LC,Liu DY,Zhang FQ,Fan WM,Shi YR and Xie HQ.2007.Zircon SHRIMP U-Pb ages of the “Xinghuadukou Group” in Hanjiayuanzi and Xinlin areas and the “Zhalantun Group” in Inner Mongolia,Da Hinggan Mountains.Chinese Science Bulletin,52(8): 1112-1134

Meng E,Xu WL,Yang DB,Pei FP,Yu Y and Zhang XZ.2008.Permian volcanisms in eastern and southeastern margins of the Jiamusi Massif,northeastern China: Zircon U-Pb chronology,geochemistry and its tectonic implications.Chinese Science Bulletin,53(8): 1231-1245

Meng E,Xu WL,Pei FP,Yang DB,Yu Y and Zhang XZ.2010.Detrital-zircon geochronology of Late Paleozoic sedimentary rocks in eastern Heilongjiang Province,NE China: Implications for the tectonic evolution of the eastern segment of the Central Asian Orogenic Belt.Tectonophysics,485(1-4): 42-51

Meng E,Xu WL,Pei FP,Yang DB,Wang F and Zhang XZ.2011.Permian bimodal volcanism in the Zhangguangcai Range of eastern Heilongjiang Province,NE China: Zircon U-Pb-Hf isotopes and geochemical evidence.Journal of Asian Earth Sciences,41(2): 119-132

Seng?r AMC,Natal’in BA and Burtman VS.1993.Evolution of the Altaid tectonic collage and Paleozoic crustal growth in Eurasia.Nature,364(6435): 299-307

Tang J,Xu WL,Wang F,Gao FH and Cao HH.2011.Petrogenesis of the bimodal volcanic rocks from the Maoershan Formation in the Zhangguangcai Range: Evidence from geochronology and geochemistry.Global Geology,30(4): 508-520 (in Chinese with English abstract)

Tang J,Xu WL,Wang F,Wang W,Xu MJ and Zhang Y H.2013.Geochronology and geochemistry of Neoproterozoic magmatism in the Erguna Massif,NE China: Petrogenesis and implications for the breakup of the Rodinia supercontinent.Precambrian Research,224: 597-611

Wang F,Xu WL,Meng E,Cao HH and Gao FH.2012a.Early Paleozoic amalgamation of the Songnen-Zhangguangcai Range and Jiamusi massifs in the eastern segment of the Central Asian Orogenic Belt: Geochronological and geochemical evidence from granitoids and rhyolites.Journal of Asian Earth Sciences,49: 234-248

Wang F,Xu WL,Gao FH,Meng E,Cao HH and Zhao L.2012b.Tectonic history of the Zhangguangcailing Group in eastern Heilongjiang Province,NE China: Constraints from U-Pb geochronology of detrital and magmatic zircons.Tectonophysics,566-567: 105-122

Wang F,Xu WL,Gao FH,Zhang HH,Pei FP,Zhao L and Yang Y.2014.Precambrian terrane within the Songnen-Zhangguangcai Range Massif,NE China: Evidence from U-Pb ages of detrital zircons from the Dongfengshan and Tadong groups.Gondwana Research,26(1): 402-413

Wilde SA,Zhang XZ and Wu FY.2000.Extension of a newly identified 500Ma metamorphic terrane in North East China: Further U-Pb SHRIMP dating of the Mashan Complex,Heilongjiang Province,China.Tectonophysics,328(1-2): 115-130

Wilde SA,Wu FY and Zhang XZ.2003.Late Pan-African magmatism in northeastern China: SHRIMP U-Pb zircon evidence from granitoids in the Jiamusi Massif.Precambrian Research,122(1-4): 311-327

Wu FY,Sun DY,Li HM and Wang XL.2001.The nature of basement beneath the Songliao Basin in NE China: Geochemical and isotopic constraints.Physics and Chemistry of the Earth,Part A: Solid Earth and Geodesy,26(9-10): 793-803

Wu FY,Zhao GC,Sun DY,Wilde SA and Yang JH.2007.The Hulan Group: Its role in the evolution of the Central Asian Orogenic Belt of NE China.Journal of Asian Earth Sciences,30(3-4): 542-556

Wu FY,Sun DY,Ge WC,Zhang YB,Grant ML,Wilde SA and Jahn BM.2011.Geochronology of the Phanerozoic granitoids in northeastern China.Journal of Asian Earth Sciences,41(1): 1-30

Wu G,Chen YC,Chen YJ and Zeng QT.2012.Zircon U-Pb ages of the metamorphic supracrustal rocks of the Xinghuadukou Group and granitic complexes in the Argun massif of the northern Great Hinggan Range,NE China,and their tectonic implications.Journal of Asian Earth Sciences,49: 214-233

Xu MJ,Xu WL,Wang F and Gao FH.2012.Age,association and provenance of the “Neoproterozoic” fengshuigouhe group in the northwestern Lesser Xing’an Rang,NE China: Constraints from zircon U-Pb geochronology.Journal of Earth Science,23(6): 786-801

Xu WL,Pei FP,Wang F,Meng E,Ji WQ,Yang DB and Wang W.2013.Spatial-temporal relationships of Mesozoic volcanic rocks in NE China: Constraints on tectonic overprinting and transformations between multiple tectonic regimes.Journal of Asian Earth Sciences,74: 167-193

Yu JJ,Wang F,Xu WL,Gao FH and Tang J.2013.Late Permian tectonic evolution at the southeastern margin of the Songnen-Zhangguangcai Range Massif,NE China: Constraints from geochronology and geochemistry of granitoids.Gondwana Research,24(2): 635-647

Zhao Z,Chi XG,Pan SY,Liu JF,Sun W and Hu ZC.2010.Zircon U-Pb LA-ICP-MS dating of Carboniferous volcanics and its geological significance in the northwestern Lesser Xing’an Range.Acta Petrologica Sinica,26(8): 2452-2464 (in Chinese with English abstract)

Zhu YF,Sun SH,Gu LB,Ogasawara Y,Jiang N and Honwa H.2001.Permian volcanism in the Mongolian orogenic zone,Northeast China: Geochemistry,magma sources and petrogenesis.Geological Magazine,138(2): 101-115

附中文參考文獻(xiàn)

黑龍江省地質(zhì)礦產(chǎn)局.1993.黑龍江省區(qū)域地質(zhì)志.北京: 地質(zhì)出版社,1-713

黑龍江省地質(zhì)礦產(chǎn)局.1997.黑龍江省巖石地層清理.武漢: 中國(guó)地質(zhì)大學(xué)出版社,11-298

洪大衛(wèi),黃懷曾,肖宜君,徐海明,靳滿(mǎn)元.1994.內(nèi)蒙古中部二疊紀(jì)堿性花崗巖及其地球動(dòng)力學(xué)意義.地質(zhì)學(xué)報(bào),68(3): 219-230

李錦軼,牛寶貴,宋彪等.1999.長(zhǎng)白山北段地殼的形成與演化.北京: 地質(zhì)出版社,1-136

劉建峰,遲效國(guó),董春艷,趙芝,黎廣榮,趙院冬.2008.小興安嶺東部早古生代花崗巖的發(fā)現(xiàn)及其構(gòu)造意義.地質(zhì)通報(bào),27(4): 534-544

苗來(lái)成,范蔚茗,張福勤,劉敦一,簡(jiǎn)平,施光海,陶華,石玉若.2003.小興安嶺西北部新開(kāi)嶺-科洛雜巖鋯石SHRIMP年代學(xué)研究及其意義.科學(xué)通報(bào),48(22): 2315-2323

唐杰,許文良,王楓,高福紅,曹花花.2011.張廣才嶺帽兒山組雙峰式火山巖成因: 年代學(xué)與地球化學(xué)證據(jù).世界地質(zhì),30(4): 508-520

趙芝,遲效國(guó),潘世語(yǔ),劉建峰,孫巍,胡兆初.2010.小興安嶺西北部石炭紀(jì)地層火山巖的鋯石LA-ICP-MS U-Pb年代學(xué)及其地質(zhì)意義.巖石學(xué)報(bào),26(8): 2452-2464