湖南大義山、塔山巖體鋯石U-Pb年齡及其構(gòu)造意義

李　勇, 張岳橋, 蘇金寶, 李建華, 董樹文

1)北京大學(xué), 北京 100871;　2)中國地質(zhì)科學(xué)院地質(zhì)力學(xué)研究所, 北京 100081; 3)河海大學(xué), 江蘇南京 210098;　4)中國地質(zhì)科學(xué)院, 北京 100037

湖南大義山、塔山巖體鋯石U-Pb年齡及其構(gòu)造意義

李勇1,2), 張岳橋2), 蘇金寶3), 李建華2), 董樹文4)*

1)北京大學(xué), 北京 100871;2)中國地質(zhì)科學(xué)院地質(zhì)力學(xué)研究所, 北京 100081; 3)河海大學(xué), 江蘇南京 210098;4)中國地質(zhì)科學(xué)院, 北京 100037

華南中部地區(qū)大義山、塔山等早中生代花崗巖的展布和侵入特征與這一時期褶皺構(gòu)造之間存在著非常密切的關(guān)系, 對這些巖體進行精確年代學(xué)研究, 可以為構(gòu)造變形時代提供年代學(xué)約束。大義山巖體南部地區(qū)鋯石U-Pb LA-ICP-MS年齡為東緣(171.8±1.9) Ma、西緣(169.9±1.8) Ma、中部(164.2±2.6) Ma, 塔山巖體東段為(247±5.9) Ma。大義山巖體在164.2—171.8 Ma之間經(jīng)歷兩個期次的侵入, 形成了一個復(fù)式巖體, 巖體形成后至125 Ma經(jīng)歷了快速隆升, 之后以接近1°C/Ma的冷卻速率抬升到地表。大義山和塔山巖體記錄了華南早中生代印支和燕山兩期重要的巖漿活動。陽明山、塔山巖體等E—W向展布巖體受印支期構(gòu)造帶控制; 大義山、騎田嶺等巖體年齡限定了燕山期構(gòu)造地層的變形下限時代, 華南地區(qū)NNE向褶皺構(gòu)造形成時代應(yīng)早于(171.8±1.9) Ma。

華南地區(qū); 大義山巖體; 塔山巖體; 鋯石U-Pb年齡

華南板塊分布著巨量的花崗巖體, 這些巖體為研究同期構(gòu)造事件提供很好的窗口(Zhou et al.,2000; Zhou et al., 2006; Zhou et al., 2007)。中生代的“印支運動”和“燕山運動”是對華南大地構(gòu)造具有重要影響的兩次構(gòu)造事件, 與這兩次構(gòu)造事件對應(yīng)的同期巖漿活動存在著一個明顯的平靜期, 將兩期構(gòu)造事件分開(Zhou et al., 2006)。由于大量不同期的侵入巖和火山巖的發(fā)育破壞了原始沉積地層,尤其是東南沿海地區(qū), 所以難以確定華南地區(qū)中生代“印支運動”與“燕山運動”兩次構(gòu)造事件轉(zhuǎn)換的精確時代。從東南沿海向華南內(nèi)陸巖漿作用逐漸減弱, 在華南中部地區(qū)巖體的分布與構(gòu)造地層之間存在非常清楚的時代關(guān)系, 通過對這些巖體的分布特征和精確年代學(xué)的研究, 可以對這兩次構(gòu)造事件的轉(zhuǎn)換時代提供約束。

大義山巖體位于湖南南部, 屬于南嶺中段重要的錫鉛鋅多金屬含礦巖體。李四光研究大義山式構(gòu)造時, 將該巖體稱為“大義山式”花崗巖(李四光, 1973)。大義山巖體一直被認為是一個多時代、多期次侵入的復(fù)式巖體, 常以關(guān)口—野鹿灘一線為界,分成了南體和北體兩部分(劉耀榮等, 2006)。長期以來由于缺少精確的年代學(xué)研究, 對于大義山巖體形成時代存在不同認識, 伍光英等(2000, 2005)研究大義山巖體地質(zhì)特征和巖體侵位機制時把南體歸于中三疊世, 整體巖體同位素年齡為210～278 Ma, 156～185 Ma和128～148 Ma, 侵人時代從印支期持續(xù)到燕山晚期。劉耀榮等(2006)對南體北側(cè)的中細粒斑狀黑云母二長花崗巖中黑云母作Ar-Ar法定年測試, 其年齡為156.2 Ma, 認為巖體形成時間應(yīng)為中—晚侏羅世, 相當于“燕山”早期。塔山巖體和陽明山巖體呈東西向展布, 陽明山巖體年齡為218 Ma, 屬于三疊紀“印支”巖體(范蔚茗等, 2004; Li X H et al., 2007; 羅志高等, 2010), 塔山巖體西段年代為(224±2) Ma也屬于三疊紀“印支期”(Chu et al., 2012), 但塔山巖體東段年代一直未見報道。對大義山和塔山巖體進行精確的年代學(xué)研究, 能夠更好地理解華南早中生代大地構(gòu)造過程, 尤其是對于華南地區(qū)中生代“印支運動”與“燕山運動”兩次構(gòu)造事件的轉(zhuǎn)換時代能夠更好地提供約束。

1　區(qū)域大地構(gòu)造背景及樣品采集

整個華南經(jīng)歷了多期次區(qū)域規(guī)模的大陸動力學(xué)過程, 大多具有板塊內(nèi)部變形的特點, 只有在新元古代和晚中生代具有活動陸緣背景(Charvet, 2013; 舒良樹, 2012)。從晚古生代開始到中三疊紀(D2-3-T2)處在一個穩(wěn)定淺海相的沉積環(huán)境, 華南板塊在這一時期經(jīng)歷了伸展拉張作用成為一個洋盆,古地殼基底減薄, 通常將這一時期的海相地層稱為印支構(gòu)造層, 其底部不整合超覆在前泥盆地層之上,泥盆系底部為一套河流相砂礫巖沉積, 向上主體為淺海相碳酸鹽沉積, 其中有海陸交互相沉積夾層,晚三疊世至早中侏羅世地層(T3-J1-2)構(gòu)成了早燕山構(gòu)造層, 主體為陸相沉積, 僅在華南東南部沿海地區(qū)分布海相地層, 整個華南地區(qū)的沉積地層已發(fā)生強烈擠壓變形, 形成構(gòu)造樣式復(fù)雜、東西寬大于1300 km的褶皺構(gòu)造帶(Li Z X et al., 2007; 徐先兵等, 2009; 張岳橋等, 2009; Wang et al., 2013), 兩套構(gòu)造層之間成角度不整合接觸。在兩套構(gòu)造層中大量分布著疊加構(gòu)造, 如廣西柳州山字形疊加構(gòu)造、南嶺中段疊加構(gòu)造、鄂西南湘北地區(qū)疊加褶皺構(gòu)造、贛中地區(qū)疊加褶皺構(gòu)造、尤其是湘中南地區(qū)疊加構(gòu)造最為典型(圖1), 其特點是早期褶皺構(gòu)造軸呈近東西或北西西—南東東向展布, 晚期呈北東—北北東向展布, 局部地區(qū)為南北向(張岳橋等, 2009)。湘中南地區(qū)橫跨疊加褶皺構(gòu)造是對早中生代從印支期碰撞構(gòu)造體系向燕山期俯沖構(gòu)造體系轉(zhuǎn)換的形變記錄, 而這兩個構(gòu)造體系轉(zhuǎn)換的時間可以用構(gòu)造地層的侵入巖體年齡來限定(徐先兵等, 2009; 張岳橋等, 2009, 2012)。

本文研究區(qū)域大義山、塔山巖體位于華南中部湘南疊加構(gòu)造發(fā)育地區(qū)。大義山巖體長約39 km, 寬約10 km, 總面積250 km2左右, 侵入的最老地層為元古界板溪群至中寒武地層, 只在西緣中部地區(qū)侵入, 巖體主體侵入到泥盆至石炭紀的碳酸鹽巖中,地層發(fā)育強烈近南北向褶皺構(gòu)造, 鑒于大義山巖體形成時代分歧主要集中在南部, 本文在巖體南部從西緣, 中部和東緣各采集了一塊樣品, 進行LA-ICP-MS鋯石U-Pb法年代學(xué)分析。塔山巖體東西長25 km, 南北寬12 km, 總面積約為200 km2,巖體處在東西向大背斜核部, 主體侵入到寒武、奧陶和志留紀地層中, 只在東緣侵入到泥盆紀灰?guī)r中,本研究在塔山巖體東段中心部位采集了一塊樣品進行LA-ICP-MS鋯石U-Pb法年代學(xué)研究。具體采樣地點和分析結(jié)果見圖2。

2　LA-ICP-MS鋯石U-Pb法測試方法與測試結(jié)果

2.1測試方法

定年樣品均采集自新鮮花崗巖露頭, 首先經(jīng)粉碎、淘洗、磁選和重液分選后分離出鋯石, 在雙目鏡下仔細挑出不同晶形、不同顏色的鋯石單礦物,在玻璃板上對鋯石進行精選, 然后用環(huán)氧樹脂將其固定凝結(jié), 再打磨至鋯石顆粒中心, 最后進行拋光處理。在開始鋯石U-Pb分析前, 用裝有陰極熒光探頭的掃描電鏡對鋯石樣品進行陰極發(fā)光(CL)照相,以確定鋯石顆粒的內(nèi)部結(jié)構(gòu), 選取適合定年分析的鋯石顆粒, 樣品年代學(xué)測試是在中國地質(zhì)科學(xué)院國家地質(zhì)實驗測試中心完成, 代表性鋯石顆粒的CL圖像見圖3。詳細的分析流程、分析精度和準確性見宋彪等(宋彪等, 2002)。分析結(jié)果根據(jù)Andersen (2002)方法進行普通Pb校正。每個鋯石微區(qū)原位測試點的同位素比值和U-Pb年齡由專用的GLITTER軟件計算, 采用Isoplot程序計算和繪制加權(quán)平均年齡及諧和圖。

圖1　華南中部構(gòu)造簡圖Fig. 1　Simplified structural map of central South China

圖2　大義山、塔山巖體構(gòu)造簡圖和采樣位置(綠色五角星標識)Fig. 2　Simplified structural map of Dayishan pluton and Tashan pluton, showing sampling sites (green stars)

圖3　大義山、塔山巖體部分鋯石的陰極發(fā)光圖像、原位測試點(圓圈)和206Pb/238U視年齡Fig. 3　CL images, locations of the points for LA-ICP-MS measurements (white circles) and206Pb/238U apparent ages of representative detected zircons from Dayishan pluton and Tashan pluton

2.2測試結(jié)果

從樣品的顯微鏡下觀察和CL圖像可見, 所分析的鋯石均為透明—淺褐色, 棱角清楚, 表面光滑,普遍發(fā)育平行的晶體生長環(huán)帶, 少數(shù)鋯石出現(xiàn)破損和局部熔蝕現(xiàn)象。晶體形態(tài)大部分為長板狀, 長寬比主要集中在2:1～4:1之間, 顆粒較大, 其長寬比可達5:1。粒徑介于100～300 μm之間。圖3為部分測定鋯石的陰極發(fā)光圖像, 從圖3中可看到鋯石顆粒均可見清晰的內(nèi)部結(jié)構(gòu), 都具有震蕩環(huán)帶生長邊巖漿結(jié)晶成因的特征, 所測試的4個樣品幾乎所有數(shù)據(jù)點都投影在206Pb/238U-207Pb/235U諧和曲線上或諧和曲線附近, 表明這些鋯石顆粒在形成后的U-Pb同位素體系是基本封閉的, 沒有U或Pb同位素的明顯丟失或加入, 測試獲得的年齡可以代表巖體的結(jié)晶年齡。表1列出了大義山和塔山巖體巖石鋯石U-Pb同位素定年結(jié)果, 圖4為年齡諧和圖, 測試點的誤差橢圓大小為68.3％置信度。本文所測定的花崗巖都是早中生代形成, 由于235U和238U的半衰期及豐度不同, 對于較年輕的鋯石(<1 Ga), 采用206Pb/238U年齡更加準確(Griffin et al., 2004; 邱檢生等, 2011), 因此本文采用了206Pb/238U年齡進行加權(quán)平均值的計算。

樣品Xn12-1采自大義山巖體南部東緣, 鋯石顆粒陰極發(fā)光圖像和測試結(jié)果如圖3、圖4和表1所示。共選取17粒晶體生長環(huán)帶比較發(fā)育的淡黃色鋯石進行了分析, 所有測試點參與計算, 絕大部分數(shù)據(jù)點都位于諧和線上, 它們的206Pb/238U加權(quán)平均年齡為(171.8±1.9) Ma, MSWD=0.25, 該年齡代表了巖體的結(jié)晶年齡。

樣品Xn306-1采自塔山巖體東段中心部位, 鋯石顆粒陰極發(fā)光圖像和測試結(jié)果如圖3、圖4和表1所示。共選取12粒晶體生長環(huán)帶比較發(fā)育的淡黃色鋯石進行了分析, 所有測試點參與計算, 它們的206Pb/238U加權(quán)平均年齡為(247.2±5.9) Ma, MSWD=3.5, 該年齡可以代表巖體的結(jié)晶年齡。

樣品Xn312-1采自大義山巖體南部中心, 鋯石顆粒陰極發(fā)光圖像和測試結(jié)果如圖3、圖4和表1所示。共選取19粒晶體生長環(huán)帶比較發(fā)育的淡黃色鋯石進行了分析, 所有測試點參與計算, 絕大部分數(shù)據(jù)點都位于諧和線上, 它們的206Pb/238U加權(quán)平均年齡為(164.2±2.6) Ma, MSWD=1.8, 該年齡代表了巖體的結(jié)晶年齡。

樣品Xn316-1采自大義山巖體南部西緣, 鋯石顆粒陰極發(fā)光圖像和測試結(jié)果如圖3、圖4和表1所示。共選取17粒晶體生長環(huán)帶比較發(fā)育的淡黃色鋯石進行了分析, 所有測試點參與計算, 絕大部分數(shù)據(jù)點都位于諧和線上, 它們的206Pb/238U加權(quán)平均年齡為(169.9±1.8) Ma, MSWD=1.10, 該年齡代表了巖體的結(jié)晶年齡。

3　構(gòu)造意義

3.1大義山巖體的隆升歷史

本文給出的大義山巖體鋯石U-Pb年齡為164.2～171.8 Ma, 參考柏道遠等(2006)鉀長石K-Ar年齡為(121.6±1.2) Ma、黑云母K-Ar年齡(146.4±1.4) Ma, 磷灰石裂變痕跡(FT)年齡為(23.1±3.2) Ma、(32.3±7.7) Ma和(劉耀榮等, 2006)鉀長石40Ar/39Ar年齡為(156.2±1.6) Ma。結(jié)合各礦物封閉溫度所構(gòu)成的演化曲線(圖5)來看, 大義山巖體在164.2～171.8 Ma之間經(jīng)歷兩個期次的侵入, 形成了一個復(fù)式巖體, 巖體形成后至125 Ma經(jīng)歷了快速隆升, 冷卻速率接近14°C/Ma, 假定中國南方地殼平均地溫梯度與古地溫梯度一致為24.1℃/km(袁玉松等, 2006), 那么巖體隆升速率約為0.58 km/Ma,之后以接近1℃/Ma的冷卻速率抬升到地表, 隆升速率約為0.041 km/Ma。來自古太平洋向西俯沖可能導(dǎo)致華南陸內(nèi)變形和快速隆升(Zhou et al., 2000; Zhou et al., 2006)。

3.2“印支”與“燕山”構(gòu)造事件的轉(zhuǎn)換時代約束

圖4　大義山和塔山花崗巖ICP-MS鋯石U-Pb諧和圖(左)和平均年齡(右)Fig. 4　Zircon207Pb/235U–206Pb/238U concordia diagrams of granitoids from Dayishan and Tashan granites

表1　華南中部地區(qū)主要的巖漿巖鋯石U-Pb年齡Table 1　Zircon U-Pb dating results for the early-middle Mesozoic magmatic rocks in central South China

續(xù)表1　

圖5　大義山巖體巖漿作用和剝露過程的溫度-時間圖解Fig. 5　Temperature versus time diagram, showing the evolution history of magmatism and exhumation of Dayishan pluton鋯石鈾鉛年齡來自本研究, Ar-Ar, K-Ar和磷灰石裂變徑跡年齡參考自(柏道遠等, 2006; 劉耀榮等, 2006)。礦物封閉溫度據(jù)(陳宣華等, 2010)及引用的相關(guān)文獻。a、b、c、d分別為冷卻速率0.1℃/Ma、1℃/Ma、10℃/Ma和100℃/Ma線。粗虛線為推測冷卻曲線。礦物代號: Zr-鋯石; Bi-黑云母; Ksp-鉀長石; Ap-磷灰石U-Pb age data from this study. Ar-Ar and AFT data from BO et al., 2006 and LIU et al., 2006. The mineral closure temperatures from CHEN et al. (2010) and references cited. The a, b, c, d stand for cooling lines with rates of 0.1 °C/Ma, 1℃/Ma, 10℃/Ma and 100℃/Ma respectively. The thick dashed line represents inferred cooling curve. Zr-zircon, Bi-biotite, Ksp-K-feldspar, Ap-apatite

“印支運動”和“燕山運動”是中生代以來對華南現(xiàn)今大地構(gòu)造格局具有決定性的兩期構(gòu)造事件,是對古特提斯構(gòu)造域和古太平洋構(gòu)造域作用的響應(yīng)(趙越等, 2004; Dong et al., 2008), 印支期華南大陸變形較弱, 地層中發(fā)育兩翼平緩的近E—W向的褶皺,強烈的NE向構(gòu)造主要在早燕山期形成, 蓋層和基底變形異常強烈并疊加改造了早期近E—W向構(gòu)造(郭福祥, 1999; 王清晨, 2009; 張岳橋等, 2009)。華南在400—245 Ma即從晚古生代開始到中三疊紀(D2-3-T2)處在一個穩(wěn)定淺海相的沉積環(huán)境, 華南板塊在這一時期經(jīng)歷了伸展拉張作用成為一個洋盆,古地殼基底減薄, 通常將這一時期的海相地層稱為印支構(gòu)造層, 其底部不整合超覆在前泥盆地層之上,泥盆系底部為一套河流相砂礫巖沉積, 向上主體為淺海相碳酸鹽沉積, 其中有海陸交互相沉積夾層,晚三疊世至早中侏羅世地層(T3-J1-2)構(gòu)成了早燕山構(gòu)造層, 主體為陸相沉積, 僅在華南東南部沿海地區(qū)分布海相地層, 整個華南地區(qū)的沉積地層已發(fā)生強烈擠壓變形, 形成構(gòu)造樣式復(fù)雜、東西寬大于1300 km的褶皺構(gòu)造帶, 兩套構(gòu)造層之間呈角度不整合接觸(Li Z X et al., 2007; 徐先兵等, 2009; Wang et al., 2013)。

要確定華南早中生代構(gòu)造地層的變形時代, 關(guān)鍵是要分析構(gòu)造地層與巖漿活動之間的時代關(guān)系(張岳橋等, 2009)。華南中部湘南地區(qū)是最為典型的疊加褶皺地區(qū), 分布著印支期和燕山期巖體, 印支巖體主要有白馬山巖體、關(guān)帝廟、陽明山、塔山等,燕山期巖體主要有大義山、騎田嶺等(巖體年齡如表1所示)。這一地區(qū)大多數(shù)印支期巖體呈E—W向展布, 處在E—W向褶皺核部, 受印支期E—W向構(gòu)造帶控制; 燕山期巖體侵入變形地層之中并不受某一個方向的褶皺構(gòu)造控制(圖1)。陽明山和塔山巖體與大義山巖體之間這種分布特征更為清楚(圖2),陽明山和塔山巖體侵入在E—W向大型褶皺背斜核部, 背斜兩翼之間最寬處達到60 km, 大義山巖體侵入變形地層之中非常截然, 變形地層沒有因巖體侵入發(fā)生同步隆升變形, 這說明陽明山和塔山巖體與大義山巖體形成處在不同的大地構(gòu)造環(huán)境之中。晚二疊—早中三疊紀是現(xiàn)代東亞板塊成形的一個重要聚合時期, 華北與華南板塊、華南與印支板塊發(fā)生了俯沖碰撞(Cai et al., 2009; Carter et al., 2001; Carter et al., 2008; Chen et al., 2011; Li et al., 2010; Metcalfe, 2011, 2013; Morley et al., 2012; Wang et al., 2013; Wu et al., 2013; Zhou et al., 2006), 印支板塊與華南板塊碰撞與大別—蘇魯超高壓變質(zhì)帶形成時限上在同一時期, 同時華南陸內(nèi)也發(fā)生了變形并伴有大量巖漿熱事件(Carter et al., 2001; Dong et al., 2008; Metcalfe, 2013), 印支運動時期又是華南板塊重要的一個轉(zhuǎn)折時期, 沉積相發(fā)生了明顯變化, 由海相環(huán)境進入到陸相環(huán)境, 大陸地殼增厚形成廣泛的褶皺構(gòu)造, 局部小的凹陷地區(qū)沉積T3-J1陸相地層,形成了造山型盆地, 盆地物源主要是來自秦嶺—大別造山帶剝蝕的碎屑巖(Shu et al., 2009; 張岳橋等, 2009; 趙越等, 2004), 來自西南方向的印支板塊和北東向華北板塊的共同擠壓作用導(dǎo)致華南內(nèi)陸發(fā)生變形, 形成了近E—W或NWW—SEE走向的寬緩褶皺(Cai et al., 2009; Sun et al., 2011; Wang et al., 2005; Zhao et al., 2013; Zhu et al., 2009), 陽明山、塔山巖體等E—W向展布的巖體正是在這樣的環(huán)境中形成的;來自古太平洋板塊俯沖作用導(dǎo)致華南板塊出現(xiàn)了寬約1300 km褶皺帶, 并且以江紹斷裂為界, 華南東部成為一個大的巖漿省, 大量逆沖斷層在俯沖作用下也相繼形成, 下地殼基底增厚上地殼地層發(fā)生了強烈變形, 之后華南大陸在晚中生代出現(xiàn)大范圍的地殼伸展減薄的環(huán)境(Li Z X et al., 2007; Li X H et al.,2007; Li et al., 2013)。大義山、騎田嶺等巖體侵入這套變形地層之中限定了變形下限時代, 華南地區(qū)NNE向褶皺構(gòu)造形成時代早于(171.8±1.9) Ma。

4　結(jié)論

(1)大義山巖體南部地區(qū)鋯石U-Pb LA-ICP-MS年齡為東緣(171.8±1.9) Ma、西緣(169.9±1.8) Ma、中部(164.2±2.6) Ma, 塔山巖體東段(247±5.9) Ma。大義山巖體在164.2—171.8 Ma之間經(jīng)歷兩個期次的侵入, 形成了一個復(fù)式巖體, 巖體形成后至125 Ma經(jīng)歷了快速隆升, 之后以接近1℃/Ma的冷卻速率抬升到地表。

(2)大義山和塔山巖體記錄了華南早中生代印支和燕山兩期重要的巖漿活動。陽明山、塔山巖體等E—W向展布巖體受印支期構(gòu)造帶控制; 大義山、騎田嶺等巖體年齡限定了燕山期構(gòu)造地層的變形下限時代, 華南地區(qū)NNE向褶皺構(gòu)造形成時代應(yīng)早于(171.8±1.9) Ma。

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Zircon U-Pb Dating of Dayishan and Tashan Plutons in Hunan Province and Its Tectonic Implications

LI Yong1,2), ZHANG Yue-qiao2), SU Jin-bao3), LI Jian-hua2), DONG Shu-wen4)*
1) Peking Universty, Beijing 100871; 2) Institute of Geomechanics, Chinese Academy of Geologicl Scienses, Beijing 100081; 3) Hohai University, Nanjing, Jiangsu 210098; 4) Chinese Academy of Geologicl Scienses, Beijing 100037

The distribution and intrusion of Early Mesozoic granites in central South China such as Dayishan pluton and Tashan pluton are closely related to folded structure in this region. Precise chronologic studies can constrain the age of the tectonic deformation. This paper report zircon U-Pb LA-ICP-MS ages of the southern part of Dayishan pluton based on dating of 3 samples: the age of the eastern margin is (171.8±1.9) Ma, that of the western margin is (169.9±1.8) Ma and that of the central part is (164.2±2.6) Ma. The zircon U-Pb LA-ICP-MS age of the eastern part of Tashan pluton is (247±5.9) Ma. Dayishan pluton experienced two phases of intrusion between 164.2 and 171.8 Ma and formed a composite pluton; after that, it experienced rapid uplift prior to 125 Ma, and then it was rapidly raised to the surface at the cooling rate of 1°C/Ma. Dayishan pluton and Tashan pluton recorded Indosinian and Yanshanian magmatic activities. The EW-trending structural zone controlled Indosinian granites, such as Yangmingshan and Tashan; the ages of Dayishan and Qitianling plutons constrain the Yanshanian tectonic deformation, and the formation of the NNE-trending folds in South China should be earlier than (171.8±1.9) Ma.

South China; Dayishan pluton; Tashan pluton; zircon U-Pb age

P588.121; P597.1

A

10.3975/cagsb.2015.03.05

本文由財政部“深部探測技術(shù)與實驗研究”專項之子課題(編號: Sinoprobe-08-01)資助。

2014-10-08; 改回日期: 2014-11-31。責任編輯: 閆立娟。

李勇, 男, 1980年生。博士研究生。構(gòu)造地質(zhì)學(xué)專業(yè)。E-mail: colyly@163.com。

董樹文, 男, 1954年生。研究員, 博士生導(dǎo)師。長期從事構(gòu)造地質(zhì)和深部地質(zhì)研究, 近年來重點探討燕山運動和東亞大陸地球動力學(xué)問題。E-mail: swdong@cags.ac.cn。