東台灣蛇綠岩(ETO)位於南中國海(SCS)和西菲律賓海盆(WPB)岩石圈的碰撞邊緣，其構造親緣性仍具爭議，南中國海及西菲律賓海盆的親緣性皆曾被論及。本論文提出東台灣蛇綠岩之玄武岩中玻璃的新Nd-Hf-Pb同位素和微量元素數據，並與南中國海和西菲律賓海盆的玄武岩數據比較，以對東台灣蛇綠岩構造親緣性提供制約。並重新檢視南台灣（墾丁）玄武岩的構造親緣性，以釐清這兩個外來岩塊之間的關係。最後，詳細檢視Yu等人(2022)的東台灣蛇綠岩中酸性岩的成分，並通過熔融和結晶模式計算推測其生成機制，將結果與玄武質玻璃的數據結合，以深入探討東台灣蛇綠岩的構造親緣性。針對採自台東縣關山鎮的嘉武溪和電光國小附近的25個玻璃樣本，分析主要元素、微量元素和Sr-Nd-Pb-Hf同位素比值。根據TAS圖，東台灣蛇綠岩玻璃樣本為玄武質。在原始地函標準化分布圖中，大部分樣本顯示稀土元素貧瘠或平坦的分布，分別代表正常型和過渡型洋脊玄武岩之特徵。樣品39因為其富含輕稀土而具富集型洋脊玄武岩之特徵。相較於南中國海和西菲律賓海盆的正常型洋脊玄武岩，部分東台灣蛇綠岩之正常型洋脊玄武岩具有更高放射性之Nd-Hf同位素核種，與虧損-虧損洋脊玄武岩地函（D-DMM）相似，將其稱為「極端虧損洋脊玄武岩」。另一群東台灣蛇綠岩之正常型洋脊玄武岩則具相對較少的放射性之Nd-Hf同位素核種，其Nd-Hf同位素比值與西菲律賓海盆之正常型洋脊玄武岩的比值重疊，將其稱為「虧損洋脊玄武岩」。東台灣蛇綠岩之正常型洋脊玄武岩的206Pb/204Pb、207Pb/204Pb和208Pb/204Pb與西菲律賓海盆之正常型洋脊玄武岩的分布重疊，且這些Pb同位素比值低於南中國海之正常型洋脊玄武岩；但南中國海僅有一鑽探點，且樣本數據雷同，因而不能代表整個南中國海的正常型洋脊玄武岩。現有之南中國海和西菲律賓海盆的洋脊玄武岩之Nd-Hf -Pb同位素數據不足以闡明東台灣蛇綠岩中玻璃的構造親緣性。高度不相容元素的濃度比值，亦能指示地函來源。在Th/Ce和Nb/Ce對比176Hf/177Hf、143Nd/144Nd和206Pb/204Pb分布圖中，東台灣蛇綠岩和南中國海的正常型洋脊玄武岩皆位於虧損-虧損地函以及富集-虧損地函序列上方（Workman and Hart, 2005），成線性趨勢；西菲律賓海盆之正常型洋脊玄武岩則分布在此序列下方。此外，東台灣蛇綠岩之正常型洋脊玄武岩和南中國海之正常型洋脊玄武岩形成連續的Nb/Ce-Nb和Th/Ce-Th線性趨勢，而西菲律賓海盆偏向較低的Nb/Ce和Th/Ce；此特徵有利於東台灣蛇綠岩和南中國海的構造親緣性。熔體混合模式計算顯示東台灣蛇綠岩中玄武質玻璃的176Hf/177Hf、143Nd/144Nd和206Pb/204Pb以及 Nb/Ce 和 Th/Ce的變化，大致可以混合虧損地函和富集地函之熔體來解釋。「極端虧損洋脊玄武岩」的成分需要虧損-虧損洋脊玄武岩地函和海南玄武質之熔體混合，「虧損洋脊玄武岩」需虧損地函熔體以及下部大陸地殼物質的混合解釋之，過渡型洋脊玄武岩的成分可以透過混合富集-虧損地函、虧損地函以及海南玄武岩的熔體而成。因此，海南玄武質熔體的參與強化東台灣蛇綠岩玻璃和南中國海的親緣性，並暗示海南地函（幔）柱的規模。相對於由東台灣蛇綠岩玻璃成分而提出的南中國海親緣性，Yu等人(2022)則基於東台灣蛇綠岩中酸性岩（斜長花崗岩）的成分，認為該酸性岩的埃達克岩特徵乃隱沒之南中國海地殼的部分熔融導致。然而，三項證據表明東台灣蛇綠岩中酸性岩的成分並非埃達克岩的成分，包含（1）SiO2含量> 70%，（2）Sr/Y < 20伴隨低Y濃度（< 7 ppm），以及（3）缺乏K、Pb和Sr富集。基性熔體的分異結晶、輝長岩或角閃岩的部分熔融之模式計算顯示，東台灣蛇綠岩中酸性岩是由南中國海岩石圈中海水交代換質之角閃岩的含水熔融和輝長岩的熔融而生成。因此，玻璃樣本與酸性岩的成分皆顯示南中國海親緣性，據此，東台灣蛇綠岩是南中國海上部岩石圈推覆至陸塊上之物質。

Located at the convergent margin between South China Sea (SCS) and West Philippine basin (WPB) slabs, East Taiwan Ophiolite (ETO) has been debated for its tectonic affinity. Earlier researchers considered ETO basaltic rocks as parts of accreted SCS slab. In contrast, Yu et al. (2022) argued plagiogranites from ETO showed adakitic compositions resulted from partial melting from the subducted SCS slab to postulate an affinity to the forearc of WPB slab. We analyzed 25 basaltic glass for major, trace elements and Nd-Hf-Pb isotope ratios. In the Th/Ce and Nb/Ce versus (176Hf/177Hf)i, (143Nd/144Nd)i, and (206Pb/204Pb)i plots, the N-MORB-like ETO glass and SCS N-MORB plot above the D-DMM–DMM–E-DMM array, whereas the WPB N-MORB plot below the array. Moreover, the N-MORB-like ETO glass and SCS N-MORB form continuous Nb/Ce–Nb and Th/Ce–Th trends, whereas the WPB N-MORB deviate to lower Nb/Ce and Th/Ce. These features favor a SCS affinity for the ETO N-MORB-like glass. Melt mixing calculations indicated the 176Hf/177Hf, 143Nd/144Nd, and 206Pb/204Pb as well as Nb/Ce and Th/Ce of the ETO glass can be can be produced by mixing melts from depleted mantle and Hainan basalts. The involvement of Hainan basalts strengthens the SCS affinity of the ETO glass and hints the scale of the Hainan mantle plume. The ETO felsic rocks are not adakitic and can be produced by hydrous melting of seawater metasomatized amphibolites in the SCS lithosphere, also favoring a SCS affinity. Therefore, the compositions of ETO mafic and felsic rocks both conclude a SCS affinity.

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