ODP 195航次1202站位(24°48.24’N, 122°30.00’E, 水深約 1274 m)位於台灣東北外海南沖繩海槽區，依據Wei et al. (2005)氧同位素地層及AMS C-14定年結果，得知前110 mbsf為過去~ 28 ka，岩心底部估計不老於68 ka。
　　本研究進行岩心描述的基本沉積學工作，並利用沉積構造和粉砂-細砂厚度變化量(Silt-Sand Layer Ratio, SLR)、主要岩屑及底棲有孔蟲分析，以探討此岩心之沉積機制及特性。計算每1.5公尺岩心長的SLR值，顯示岩心可分為A～H八段：SLR值由A段(19.2～133 mbsf; <5%)逐漸增加至C段(167.95～199.12 mbsf; 漸增至45%)及D段(199.12～223.82 mbsf; 10～45% )，到E段達到最高值(223.82～280.35 mbsf; 30～100%)，然後再逐漸在F～G段(280.35～338.15mbsf; 3～27%)降低到H段(338.15～407.24 mbsf; <5%)。底棲有孔蟲在全部岩心中含量均非常低(平均33個/10g)，顯示高沉積速率造成稀釋效應。根據底棲有孔蟲化石含量可大致將岩心分成X、Y、Z三段。其中X段(1.25～136 mbsf)相當於SLR之A段，以泥質沉積為主，底棲有孔蟲數量<10個/10g，底棲有孔蟲主要為深海種；而Y段(136～218 mbsf)相當於SLR之B-C-D段，底棲有孔蟲數量增加至200～800個/10g，其中絕大部分為淺海種(40～100 %)；Z段(218～408 mbsf)相當於SLR之E～H段，Z段上部(218～283 mbsf)為SLR最高值，底棲有孔蟲數量卻極微<10個/10g，主要為淺海種，顯示濁流快速沉積，Z段下部(286～408 mbsf) SLR降低、主要為泥質沉積，底棲有孔蟲數量亦極微，底棲有孔蟲組成為深海種。主要粗顆粒岩屑(>250 μm)組成為板岩屑、雲母及其他變質岩屑、及火山碎屑(含火山結晶、火山玻璃及浮石)。另外沉積物中含有大量淺海底棲有孔蟲、海綿、海膽、軟體動物、苔蘚蟲及少量珊瑚等生物屑片。
　　計算岩心1202的沉積速率顯示MIS 2的沉積速率(2.71 m/ka)反而比MIS 1 (4.65 m/ka) 及MIS 3～4 (7.04 m/ka)為低，顯示冰期海水面變化不是控制岩心1202沉積的最主要機制。綜合SLR、底棲有孔蟲及岩屑分析結果，顯示台灣在間冰期時因夏季季風增強氣候暖濕、風化侵蝕加劇，使陸源沉積物供應增多，MIS 1的沉積速率高於MIS 2，但MIS 3～4卻是沉積速率最高時期。顯然古氣候變化為岩心1202的沉積機制之一，但仍有其他影響因素。
　　岩心1202位於菲律賓海板塊隱沒入歐亞板塊的弧後張裂及板塊壓縮碰撞區，火山活動及地震頻繁。岩心附近有三個深海河道，最北邊的海底河道源自臺灣島中央山脈西側的蘭陽溪，另二支河道源自宜蘭陸棚。推測來自中央山脈北段並沉積在宜蘭陸棚之板岩屑、變質岩屑及淺海生物碎屑，因快速累積到不穩定的臨界值時，受地震頻繁的影響，致使大陸棚或上部斜坡物質不穩定、重力崩塌向低處輸送，產生濁流層並經由海底河道搬運到南沖繩海槽南段堆積，同時南沖繩海槽的火山活動亦供應物質到臨近地區。
　　岩心1202以濁流沉積為主，不同時期濁流強度不一。在MIS 1～2 (19.2～133 mbsf)雖然沉積顆粒較細卻含有淺海生物碎屑，以細粒濁流沉積為主；MIS 3濁流沉積開始大量出現，MIS 3～4 (223.82～280.35 mbsf)為濁流最強盛期，MIS 4 (278～408 mbsf)濁流沉積迅速降低，亦為細粒濁流沉積。由沉積物岩性及淺海底棲有孔蟲的出現與否，顯示淺海底棲有孔蟲的分佈，可作為細粒濁流沉積的指標。

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