台湾海岸山脉岩石地球化学特征及其构造意义
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摘要
台湾岛位于欧亚板块与菲律宾海板块的交界带，所处构造背景十分复杂，台湾岛的隆升是吕宋岛弧和欧亚大陆东南边缘斜向碰撞（弧陆碰撞）的结果。海岸山脉位于台湾岛东部，包括其南部的绿岛、兰屿两座离岛，是吕宋岛弧的北段，最初是南海洋壳俯冲于菲律宾海板块之下形成的洋内弧，最先与欧亚大陆发生碰撞。本研究以海岸山脉出露的火成岩和沉积岩以及混杂岩为研究对象，并结合台湾及邻域大地构造演化，通过岩石学、地球化学和年代学的综合分析，讨论弧陆碰撞背景下岩石地球化学特征和海岸山脉（吕宋岛弧北段）的演化过程。
通过细致的野外调查和42件样品岩石学分析，结合前人研究资料，海岸山脉（奇美和成广澳火山组成）-绿岛-兰屿都峦山层都以安山质岩石为主，但在微观特征上有所差别，成广澳火山的安山岩与奇美火山安山岩相比角闪石的含量明显增加，绿岛和小兰屿的安山岩中出现了较多的黑云母斑晶。这种现象说明了北吕宋岛弧自北向南、由老至新岩浆逐渐向高级方向演化。这种时空分布特征也表现在地球化学特征上，安山岩从北向南、由老至新碱性渐强，稀土元素内部分馏作用逐渐增强，安山岩越年轻、εNd值越负。吕宋岛弧北段在岩石学和地球化学特征表现出越向南越受大陆物质影响、越年轻越受大陆物质影响的时空分布特征，经过构造格局和矿物学分析表明岛弧火山所表现的这种现象主要是受陆壳表层沉积物的影响，而中下地壳物质可能未参与其中。吕宋岛弧北段岩浆成分已从岛弧拉斑玄武岩系列过度到了钙碱性系列，说明岛弧已由不成熟的洋内弧向半成熟岛弧演化。都峦山层岩浆来源相同，都是少量地幔和下地壳的部分熔融产生的岩浆，由于分异作用而形成了不同性质的火成岩。
弧前盆地的大港口层为样品浊积相的碎屑岩，大港口层下部（番薯寮层）碎屑岩包含较多的安山岩岩屑，碎屑锆石都显示为岩浆锆石，年龄主要分布在10-8Ma，表明沉积时弧前盆地距离欧亚大陆距离较远，其物源主要来自火山岛弧，沉积中心在盆地东部；大港口层上部（八里湾层）的碎屑岩含有较多的板岩和变质砂岩岩屑，碎屑锆石主要为岩浆锆石，少部分显示为变质锆石，年龄分布跨度非常大且年龄段分布分散，以1300-1200Ma、2500-1800Ma和260-216Ma的年龄段为主，这些从古-中元古代吕梁-晋宁阶段到中生代燕山阶段碎屑锆石都来自欧亚大陆，此时弧前盆地不断接近碰撞边缘的欧亚大陆，沉积中心向西迁移。
利吉混杂岩的泥岩-粉砂岩基质中夹杂各类大小不一的岩块，包括砂岩、粉砂岩、辉长岩、辉绿岩、花岗岩、玄武岩、安山岩和灰岩以及蛇纹岩等，另外还有来自中央山脉的板岩岩块等，所有的岩块和基质都经过了强烈的剪切作用。岩石学和年代学分析表明，利吉混杂岩基质与八里湾层碎屑岩相似，推测利吉混杂岩起源于弧前盆地环境。就此推断现今北吕宋海槽中的花东海脊是利吉混杂岩的前身，为一反冲断层形成的冲起构造，花东海脊向西逆冲混杂了欧亚大陆边缘中央山脉/增生楔的变质砂岩、板岩等岩块，随岛弧及其弧前盆地的逆冲作用混杂了吕宋火山岛弧安山岩、辉长岩等火成岩和礁灰岩岩块，一些洋壳岩块也被岛弧的逆冲作用带入了混杂岩。
综合上述研究，总结海岸山脉形成演化过程：中新世中期时南海洋壳沿马尼拉海沟向东俯冲于菲律宾海板块之下，形成吕宋岛弧，16Ma吕宋岛弧开始了火山活动。16-14Ma是初期喷发阶段，13-9Ma这段时期是火山活动活跃期，同时俯冲增生楔规模逐渐增大。至晚中新世以前，弧前盆地主要接受火山喷发物和火山角砾，形成了弧前盆地的下部的番薯寮层。晚中新世（~6.5Ma）时吕宋岛弧最北端的奇美火山随菲律宾海板块向西逆冲至欧亚板块陆壳上，脱离了俯冲带岩浆房，停止了岩浆活动，进入了初期弧陆碰撞阶段。吕宋岛弧逐渐接近欧亚大陆，增生楔开始出露水面，此时有来自出露的增生楔和欧亚大陆的浊流沉积物堆积于岛弧周围的盆地中，八里湾层逐渐形成。岛弧向西逆冲碰撞时产生斜滑断层，而使局部火山岛快速下陷而形成弧间盆地。晚上新世，弧前盆地的沉积物已经逐渐开始向西逆冲，3.5Ma时，弧前盆地八里湾层沉积物反冲变形成为原花东海脊。随后两期逆冲作用形成了利吉混杂岩。2Ma时，随着岛弧的进一步向北西运动挤压碰撞，利吉混杂岩、残留弧前盆地及火山岛弧，再向西逆冲到中央山脉东侧，形成了现今的海岸山脉和台东纵谷碰撞缝合线。
Taiwan is situated in the active subduction-collision region between the southeasternEurasian Plate and the Philippine Sea Plate. The island of Taiwan is the product of the collision ofthe Luzon Arc with the Eurasian Continent (arc-continent collision). The Coastal Range of easternTaiwan with Lutao and Lanhsu islets represents the northern segment of the Luzon Arc, which wascreated as a result of eastward subduction of the South China Sea oceanic lithosphere beneath thePhilippine Sea plate. The northern Luzon Arc first accreted to the Eurasian Continent margin andformed the Coastal Range. In the graduation thesis I study the petrography, geochemistry andchronology for the igneous rocks, sedimentary rocks and mélanges from the Coastal Range, andsummarize the temporal and spatial variation of petrographic and geochemical characteristicscombined with the tectonic background, finally conclude the evolution of the Coastal Rangeduring the arc-continent collision.
The Tuluanshan Formation in the Coastal Range (Chimei and Chengkuangao volcanoes),Lutao and Lanhsu is mainly composed of andesitic rocks. But there are some differences inpetrography. Pyroxene phenocrysts are common in the andesites from the Chimei volcano besidesthe dominated plagioclase phenocrysts. But hornblende phenocrysts extensively turn up in theandesites from the Chengkuangao volcano. There is no biotite phenocryst in the andesites from theCoastal Range, while it widely turns up in the andesites from Lutao and Hsiaolanhsu. It is shownthe magma evolution could be advanced with the northern Luzon Arc getting younger southward.The temporal and spatial variation also could be shown in geochemistry. An alkali-rich trend andstronger fractionation of REE could been shown southward in younger rocks, and the values of εNdbecome more negative in younger andesites. In a word it is shown that the rocks are contaminatedby continental materials more intensively southward in younger rocks. These continental materialscould be sediments from the Eurasian continent but not the lower continent crusts by petrographic,geochemical and tectonic analyses. The magma has evolved from low-K tholeiite series tomedium-K calc-alkaline series and the arc has already reached to semi-mature stage southwardfrom an immature intra-oceanic arc. All the igneous rocks of the Tuluanshan Formation have thesame magma source forming by partial melting of lower crust with a little mantle and they aredifferent in lithology because of partial melting in varying degree.
The Takangkou Formation in the Coastal Range was turbidite facies in the forearc basin,including the lower Fanshuliao Formation and upper Paliwan Formation. The sandstones in theFanshuliao Formation contain more andesitic clastics and their zircons are all magmatic zircon,forming in middle Miocene from10to8Ma mainly. It is indicated that these sediments weremainly from the Luzon Arc because of the basins were far away from the Eurasian Continent atthat time. Their sedimentation centers are in the eastern basins. The sandstones in the PaliwanFormation contain more slate and metamorphic sandstone clastics. The zircons in the PaliwanFormation are mainly magmatic zircon and some metamorphic zircons. Their U-Pb datingresults yield dominant middle Proterozoic (1300-1200Ma)、early Proterozoic (2500-1800Ma) and late Permian to Triassic (260-216Ma). These zircon are from the Eurasian Continent. Theseforearc basins were closer to the Eurasian Continent margin and the sedimentation centers weremoving westward when the Paliwan Formation formed.
The Lichi mélange, contained in a fine-grained deformed matrix, consists of a jumble ofblocks of sandstone, siltstone, gabbro, diabase, granite, basalt, andesite, limestone, ophiolite, slateand metamorphic sandstone. The Lichi mélange shows varying degrees of fragmentation of strata,mixing and shearing. The petrographic and chronological evidences show that the matrix could beorigin of the forearc basin. The Huatung Ridge, a Popup formed by back-thrust in the forearcbasin now, could be the proto-mélange. The Ridge was accreted to the accretionary prismwestward with slate and matermorphic sandstone blocks from accretionary prism. At the sametime the Taiyuan forearc basin and its volcanic basement were thrust westward over the PopupRidge taking andesite, gabbro, limestone and oceanic crust blocks into the mélange.
The Luzon Arc was created in middle Miocene time and its volcanism started at about16Ma.The period of initial volcanism ranges from16Ma to14Ma, and the active period ranges from13Ma to9Ma. The sedimentation in the forearc basin has began with the arc derived FanshuliaoFormation before late Miocene, which contains andesitic breccias and tuffaceous sandstones. TheChimei volcano in the north of the Luzon Arc firstly was thrusted westward onto the Eurasiancrust in late Miocene (~6.5Ma). Its volcanic activity was terminated because of moving away fromthe magma chamber in the subduction zone. The initial arc-continent collision was started. TheLuzon Arc was getting close to the Eurasian Continent and the accretionary prism was upliftedwith continuous subduction. The turbidites from the Eurasian Continent and the accretionaryprism deposited in the forearc basin and the Paliwan Formation formed. During the collision,strikep-slip faults would have been developed in the arc volcano to induce transtensionmovements and the intra-arc basins formed. The forearc basin began to thrust wesward in latePliocene. The proto-mélange Ridge formed because of the Paliwan Formation back-thrust at about3.5Ma. Then two westward thrustings of the forearc basin talked above induced the Lichi mélange.The volcanic island, forearc basin and mélange all collided north-westward with the EurasianContinent margin and they were accreted to the east of the Central Range so that the CoastalRange and the Longitudinal Valley formed at about2Ma.
通过细致的野外调查和42件样品岩石学分析，结合前人研究资料，海岸山脉（奇美和成广澳火山组成）-绿岛-兰屿都峦山层都以安山质岩石为主，但在微观特征上有所差别，成广澳火山的安山岩与奇美火山安山岩相比角闪石的含量明显增加，绿岛和小兰屿的安山岩中出现了较多的黑云母斑晶。这种现象说明了北吕宋岛弧自北向南、由老至新岩浆逐渐向高级方向演化。这种时空分布特征也表现在地球化学特征上，安山岩从北向南、由老至新碱性渐强，稀土元素内部分馏作用逐渐增强，安山岩越年轻、εNd值越负。吕宋岛弧北段在岩石学和地球化学特征表现出越向南越受大陆物质影响、越年轻越受大陆物质影响的时空分布特征，经过构造格局和矿物学分析表明岛弧火山所表现的这种现象主要是受陆壳表层沉积物的影响，而中下地壳物质可能未参与其中。吕宋岛弧北段岩浆成分已从岛弧拉斑玄武岩系列过度到了钙碱性系列，说明岛弧已由不成熟的洋内弧向半成熟岛弧演化。都峦山层岩浆来源相同，都是少量地幔和下地壳的部分熔融产生的岩浆，由于分异作用而形成了不同性质的火成岩。
弧前盆地的大港口层为样品浊积相的碎屑岩，大港口层下部（番薯寮层）碎屑岩包含较多的安山岩岩屑，碎屑锆石都显示为岩浆锆石，年龄主要分布在10-8Ma，表明沉积时弧前盆地距离欧亚大陆距离较远，其物源主要来自火山岛弧，沉积中心在盆地东部；大港口层上部（八里湾层）的碎屑岩含有较多的板岩和变质砂岩岩屑，碎屑锆石主要为岩浆锆石，少部分显示为变质锆石，年龄分布跨度非常大且年龄段分布分散，以1300-1200Ma、2500-1800Ma和260-216Ma的年龄段为主，这些从古-中元古代吕梁-晋宁阶段到中生代燕山阶段碎屑锆石都来自欧亚大陆，此时弧前盆地不断接近碰撞边缘的欧亚大陆，沉积中心向西迁移。
利吉混杂岩的泥岩-粉砂岩基质中夹杂各类大小不一的岩块，包括砂岩、粉砂岩、辉长岩、辉绿岩、花岗岩、玄武岩、安山岩和灰岩以及蛇纹岩等，另外还有来自中央山脉的板岩岩块等，所有的岩块和基质都经过了强烈的剪切作用。岩石学和年代学分析表明，利吉混杂岩基质与八里湾层碎屑岩相似，推测利吉混杂岩起源于弧前盆地环境。就此推断现今北吕宋海槽中的花东海脊是利吉混杂岩的前身，为一反冲断层形成的冲起构造，花东海脊向西逆冲混杂了欧亚大陆边缘中央山脉/增生楔的变质砂岩、板岩等岩块，随岛弧及其弧前盆地的逆冲作用混杂了吕宋火山岛弧安山岩、辉长岩等火成岩和礁灰岩岩块，一些洋壳岩块也被岛弧的逆冲作用带入了混杂岩。
综合上述研究，总结海岸山脉形成演化过程：中新世中期时南海洋壳沿马尼拉海沟向东俯冲于菲律宾海板块之下，形成吕宋岛弧，16Ma吕宋岛弧开始了火山活动。16-14Ma是初期喷发阶段，13-9Ma这段时期是火山活动活跃期，同时俯冲增生楔规模逐渐增大。至晚中新世以前，弧前盆地主要接受火山喷发物和火山角砾，形成了弧前盆地的下部的番薯寮层。晚中新世（~6.5Ma）时吕宋岛弧最北端的奇美火山随菲律宾海板块向西逆冲至欧亚板块陆壳上，脱离了俯冲带岩浆房，停止了岩浆活动，进入了初期弧陆碰撞阶段。吕宋岛弧逐渐接近欧亚大陆，增生楔开始出露水面，此时有来自出露的增生楔和欧亚大陆的浊流沉积物堆积于岛弧周围的盆地中，八里湾层逐渐形成。岛弧向西逆冲碰撞时产生斜滑断层，而使局部火山岛快速下陷而形成弧间盆地。晚上新世，弧前盆地的沉积物已经逐渐开始向西逆冲，3.5Ma时，弧前盆地八里湾层沉积物反冲变形成为原花东海脊。随后两期逆冲作用形成了利吉混杂岩。2Ma时，随着岛弧的进一步向北西运动挤压碰撞，利吉混杂岩、残留弧前盆地及火山岛弧，再向西逆冲到中央山脉东侧，形成了现今的海岸山脉和台东纵谷碰撞缝合线。
Taiwan is situated in the active subduction-collision region between the southeasternEurasian Plate and the Philippine Sea Plate. The island of Taiwan is the product of the collision ofthe Luzon Arc with the Eurasian Continent (arc-continent collision). The Coastal Range of easternTaiwan with Lutao and Lanhsu islets represents the northern segment of the Luzon Arc, which wascreated as a result of eastward subduction of the South China Sea oceanic lithosphere beneath thePhilippine Sea plate. The northern Luzon Arc first accreted to the Eurasian Continent margin andformed the Coastal Range. In the graduation thesis I study the petrography, geochemistry andchronology for the igneous rocks, sedimentary rocks and mélanges from the Coastal Range, andsummarize the temporal and spatial variation of petrographic and geochemical characteristicscombined with the tectonic background, finally conclude the evolution of the Coastal Rangeduring the arc-continent collision.
The Tuluanshan Formation in the Coastal Range (Chimei and Chengkuangao volcanoes),Lutao and Lanhsu is mainly composed of andesitic rocks. But there are some differences inpetrography. Pyroxene phenocrysts are common in the andesites from the Chimei volcano besidesthe dominated plagioclase phenocrysts. But hornblende phenocrysts extensively turn up in theandesites from the Chengkuangao volcano. There is no biotite phenocryst in the andesites from theCoastal Range, while it widely turns up in the andesites from Lutao and Hsiaolanhsu. It is shownthe magma evolution could be advanced with the northern Luzon Arc getting younger southward.The temporal and spatial variation also could be shown in geochemistry. An alkali-rich trend andstronger fractionation of REE could been shown southward in younger rocks, and the values of εNdbecome more negative in younger andesites. In a word it is shown that the rocks are contaminatedby continental materials more intensively southward in younger rocks. These continental materialscould be sediments from the Eurasian continent but not the lower continent crusts by petrographic,geochemical and tectonic analyses. The magma has evolved from low-K tholeiite series tomedium-K calc-alkaline series and the arc has already reached to semi-mature stage southwardfrom an immature intra-oceanic arc. All the igneous rocks of the Tuluanshan Formation have thesame magma source forming by partial melting of lower crust with a little mantle and they aredifferent in lithology because of partial melting in varying degree.
The Takangkou Formation in the Coastal Range was turbidite facies in the forearc basin,including the lower Fanshuliao Formation and upper Paliwan Formation. The sandstones in theFanshuliao Formation contain more andesitic clastics and their zircons are all magmatic zircon,forming in middle Miocene from10to8Ma mainly. It is indicated that these sediments weremainly from the Luzon Arc because of the basins were far away from the Eurasian Continent atthat time. Their sedimentation centers are in the eastern basins. The sandstones in the PaliwanFormation contain more slate and metamorphic sandstone clastics. The zircons in the PaliwanFormation are mainly magmatic zircon and some metamorphic zircons. Their U-Pb datingresults yield dominant middle Proterozoic (1300-1200Ma)、early Proterozoic (2500-1800Ma) and late Permian to Triassic (260-216Ma). These zircon are from the Eurasian Continent. Theseforearc basins were closer to the Eurasian Continent margin and the sedimentation centers weremoving westward when the Paliwan Formation formed.
The Lichi mélange, contained in a fine-grained deformed matrix, consists of a jumble ofblocks of sandstone, siltstone, gabbro, diabase, granite, basalt, andesite, limestone, ophiolite, slateand metamorphic sandstone. The Lichi mélange shows varying degrees of fragmentation of strata,mixing and shearing. The petrographic and chronological evidences show that the matrix could beorigin of the forearc basin. The Huatung Ridge, a Popup formed by back-thrust in the forearcbasin now, could be the proto-mélange. The Ridge was accreted to the accretionary prismwestward with slate and matermorphic sandstone blocks from accretionary prism. At the sametime the Taiyuan forearc basin and its volcanic basement were thrust westward over the PopupRidge taking andesite, gabbro, limestone and oceanic crust blocks into the mélange.
The Luzon Arc was created in middle Miocene time and its volcanism started at about16Ma.The period of initial volcanism ranges from16Ma to14Ma, and the active period ranges from13Ma to9Ma. The sedimentation in the forearc basin has began with the arc derived FanshuliaoFormation before late Miocene, which contains andesitic breccias and tuffaceous sandstones. TheChimei volcano in the north of the Luzon Arc firstly was thrusted westward onto the Eurasiancrust in late Miocene (~6.5Ma). Its volcanic activity was terminated because of moving away fromthe magma chamber in the subduction zone. The initial arc-continent collision was started. TheLuzon Arc was getting close to the Eurasian Continent and the accretionary prism was upliftedwith continuous subduction. The turbidites from the Eurasian Continent and the accretionaryprism deposited in the forearc basin and the Paliwan Formation formed. During the collision,strikep-slip faults would have been developed in the arc volcano to induce transtensionmovements and the intra-arc basins formed. The forearc basin began to thrust wesward in latePliocene. The proto-mélange Ridge formed because of the Paliwan Formation back-thrust at about3.5Ma. Then two westward thrustings of the forearc basin talked above induced the Lichi mélange.The volcanic island, forearc basin and mélange all collided north-westward with the EurasianContinent margin and they were accreted to the east of the Central Range so that the CoastalRange and the Longitudinal Valley formed at about2Ma.
引文
[1] Barrier E, Angelier J. Active collision in eastern Taiwan: the Coastal Range [J].Tectonophysics,1986,125:39-72.
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