本研究利用自行施放的30顆SVP浮標、分析AOML歷史浮標資料與三艘研究船的Sb-ADCP同步觀測，並結合衛星高度與風速資料、NPACNFS、NLOM、EASNFS模式結果等資料探討台灣海峽(TS)附近海域流場的季節性變化與颱風對於表層流場的影響。由歷史浮標資料的分析結果顯示夏季TS的表層水大部分是源自於南海陸棚上的水，冬季TS北部的表層平均海流為向南流，平均流速約0.3~0.4 m/s，秋季TS內流場主要是東側為北流，西側為南流，春季TS內的資料較少，只有少數的北流。夏季黑潮的表層水沒有從呂宋海峽入侵南海，而是菲律賓西邊有一股0.5~0.7 m/s的東北流穿越呂宋海峽後匯入黑潮。TS的浮標漂流軌跡類型可依當時為西南風、強勁東北風與微弱東北風分類，第一種類型為西南風盛行時，浮標是由南朝北漂流通過TS。第二、三類型為東北風強勁時，浮標從黑潮或東海進入東海陸棚，而後南下進入TS，部份浮標會擱淺在台灣西海岸，部份浮標會直接南下穿越TS進入南海。浮標如果從呂宋海峽出發，將北上進到TS，但最多只能北上至澎湖群島後就無法北上轉而向南或西南漂流進入南海。第四種浮標軌跡類型先是微弱東北季風而後變成強勁東北季風，浮標從南海北上進到TS，但是沒有繼續北上進入東海，而是反轉南下再回到南海。第五種浮標軌跡主要呈現TS北端在東北季風微弱時的往北漂流型態，此種漂流軌跡似乎屬於冬季的台灣暖流(Taiwan Warm Current, TWC)，TWC表層流速約為朝北0.2 ~ 0.4 m/s，第二、四與五類型皆是過去文獻罕見的漂流軌跡。颱風下的海洋觀測也是稀有與寶貴的資料，颱風中心附近浮標觀測到的最大流速為2.0 m/s，當時瞬間風速約37 m/s，浮標觀測到的SST溫度降低約2~4℃。迴歸結果顯示馬祖氣象站在海棠颱風通過時每小時平均風速增加3 m/s，浮標流速約增加0.52 m/s，浮標流向約在風向的右方45度。2006年夏天碧利斯颱風與桑美颱風通過台灣東北海域時，黑潮附近的浮標轉而向東海陸棚內漂流，觀測到的最大流速約1.1 m/s，這也意味著在夏季颱風通過時位在颱風中心北方的黑潮海水會藉由颱風入侵到東海陸棚。
本研究利用三艘研究船Sb-ADCP在2002月8月、2003月9月與2004年3月聯合監測TS的流量，經過相位平均法濾潮後三個航次所得到的TS流量分別為3.4、3.6和2.8 Sv，此結果與NRL EASNFS模式估算的TS流量相互比對落於合理的流量範圍。在澎湖水道也測試與評估了多種相位平均法的適用性，3, 4和5相位平均法適用於各種潮型的海域(F=0~3)，濾潮效果顯著，最佳觀測間隔時間分別約在8、6與5小時左右，如果觀測測線過長，無法在最佳觀測時間進行觀測時可以考慮使用次佳的觀測時間。2相位平均法除了以半日潮為主導的海域濾潮明顯外，其餘潮型海域並不適用。

In order to better understand the flow dynamics in the Taiwan Strait (TS) and the adjacent seas, a series of field experiments were conducted to monitor the currents by deploying 30 SVP drifters, using shipboard ADCP measurements and analyzing historical drifter data in the TS. Examinations of historical drifter data reveal that the surface waters in the TS originate from the shelf of the South China Sea (SCS) in the summer. In wintertime, the mean surface current flows toward the south in the northern TS with a mean speed of approximately 0.3~0.4 m/s. The surface current in the eastern TS mainly flows northward, and it flows southward in the western TS in the fall. The surface waters of the Kuroshio do not intrude into the SCS in summer. Instead, a northeastward current of 0.5~0.7 m/s west of Luzon Island impinges on the Kuroshio across the Luzon Strait. Drifter tracks in the TS are classified according to the wind condition. The first type of drifter tracks is that the drifters move northward in the TS with an intensified flows in the Peng-hu Channel when the southwest monsoon prevails. The second and third types of drifter tracks are under the influence of strong northeast monsoon. The drifters are carried onto the shelf of East China Sea from the Kuroshio or the East China Sea, and then move southward along the TS. Some drifters are grounded at the west coast of Taiwan, and the others drift through the TS. The third type of drifter tracks show that drifters start from the Luzon Strait and move northward into the TS. However, they can only reach the neighboring area of Peng-Hu archipelagoes, then they change the direction of drifting to the south or southwest and toward the SCS. The fourth type is that drifters are carried northward from the SCS into the northern TS under the weak northeast wind, and then veer to the south when the northeast monsoon intensifies. The fifth type of drifter tracks demonstrates the flow pattern of the northern TS when the northeast monsoon diminishes. This flow pattern belongs to the Taiwan Warm Current (TWC) in wintertime. The surface speed of TWC is about 0.2~0.4 m/s northward. The second, fourth and fifth flow patterns in the TS have not been quite discovered in previous studies. In-situ marine observations right beneath typhoons are very scanty and valuable. In this study we have found several events with some drifters happened to get caught by typhoons. The maximum speed of drifters near the typhoon center is found to be about 2 m/s. The SST, which is observed by the drifter, reduces 2~4℃ after the typhoon passes. Our results indicate that for the case of the Typhoon Haitang the Matsu weather station measured a sudden increase of wind speed of about 3 m/s every hour, and the corresponding drifter speed increases 0.52 m/s. There were two events in summer of 2006 when the Typhoon Billis and Saomai passed the northern region of Taiwan, and some drifters located at the Kuroshio to the north of typhoon were carried rapidly onto the ECS shelf with a maximum speed of about 1.1 m/s. This result indicates that the Kuroshio waters can penetrate into the ECS shelf by means of the passage of typhoon in this region during summertime.
Three cruises with the shipboard ADCP were performed by three research vessels concurrently along two transects during 2002-2004. Various phase averaging methods were employed to eliminate tidal effects. The calculated volume transport of the TS for the period of August 2002, September 2003 and March 2004 is 3.4, 3.6 and 2.8 Sv, respectively. These transport values are compatible with the output of EASCNFS model. The estimated uncertainty of the residual flow through the Peng-hu Channel derived from the 5-phase-averaging, 4-phase-averaging, 3-phase-averaging and 2-phase-averaging methods is 0.3, 0.3, 1.3 and 4.6 cm/s, respectively. Procedures for choosing a best phase average method to remove tidal currents in any particular region are also suggested.

謝誌…I
目錄…II
圖目錄…III
表目錄…VI
中文摘要…VII
英文摘要…IX
第一章 緒論…1
第二章 觀測方法與資料來源…7
2-1 三艘研究船Sb-ADCP聯合觀測…7
2-2 Lagrangian浮標…9
2-3其他資料來源…11
第三章 分析方法…18
3-1移除Sb-ADCP潮流分量…18
3-2 Sb-ADCP流量之估算…20
3-3 Lagrangian浮標資料…20
第四章 台灣附近海域之季節流場-Lagrangian觀測…24
4-1 觀測結果…24
4-2 表層流場的季節性變化…27
4-3 台灣海峽附近的漂流軌跡類型…30
第五章 颱風對表層流場的影響…57
5-1 颱風造成的表層強流…57
5-2 夏季因颱風造成黑潮入侵東海陸棚的現象...61
第六章 台灣海峽流場與流量之觀測-三船聯合觀測…78
6-1 相位平均法應用與估算…78
6-2 三船聯合觀測…82
第七章 結論…99
參考文獻…103
個人著作表…109
附件一 …110

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