南海內波起源於呂宋海峽，因潮流受蘭嶼海脊及恆春海脊的作用，產生內潮。內潮向西傳播進入南海，受非線性作用及海水分層強度的變化等之影響，波形變陡，逐漸演化成非線性內波(內孤立波)。當非線性內波傳播到東沙環礁東側大陸斜坡時，受淺化效應波形開始轉變。本研究以現場觀測資料，解析東沙海域大陸斜坡上，非線性內波淺化過程及波形變形的機制，觀測資料主要由三個海研三號航次收集，包含2010年8月的1組溫度計串及海流錨碇，及2008年5月的5組溫度計串錨碇，及2007年4月的紊流觀測。
在東沙海域，深水區非線性內波觀測到以下沉型為主，振幅介於30–110公尺，相位速度約1 m s-1向淺水傳播，流場在內波界面上方向西，界面下方流場向東。從東沙斜坡上5組溫度計串觀測，內波從水深285公尺至100公尺，由原本對稱的波形，淺化過程中波形前端逐漸拉長但後端維持原本波形，當傳播至更淺的測站時，波形後端形成上舉型波形。波形變形的機制的研究，統計分析5組溫度計串觀測資料中挑選的78個內波波形，在兩層流體系統假設下，發現內波波形轉變過程主要受內波振幅大小及下層厚度之關係控制。內波波形轉變的臨界條件為，內波振幅與下層厚度比值約0.66±0.2。當內波振幅小於0.45倍的下層厚度時，內波將維持下沉型波形繼續向淺水傳播。當振幅大於0.83倍下層厚度時，形成冷水抬升的上舉型內波。從東沙環礁周邊紊流觀測結果顯示，下沉型非線性內波在其波谷及波形後緣引發水體混合，其渦流動能消散率約10-6 Wkg-1–10-5 Wkg-1，與東沙海域背景值相比之下，非線性內波能增強水體混合約100–1000倍，與本海域相關研究相符。

Large amplitude nonlinear internal waves have been frequently observed in the northern South China Sea. These waves are originated from internal tide generated by barotropic tidal currents over the two submarine ridges in Luzon strait, propagate westward across the basin, shoal and dissipate at the shallow continental shelves. This study is focus on the deformation and shoaling of large-amplitude nonlinear internal wave near the Dongsha Atoll based on field observations. Field data were collected mainly from three R/V Ocean Research III cruises, including an intensive array of T-string moorings and a bottom mounted current meter (May, 2008 and August, 2010) and microstructure profiling observations (April, 2007).
For the wave shoaling study, in deeper water depth, depression waves were observed with the amplitude in range of 30 m–110 m. The vertical structure of flow pattern shows an anti-clockwise rotation, ie, flow to the west in the upper and to the east in the lower layer of an internal soliton wave. Shoaling of large-amplitude nonlinear internal waves over a steep slope (~3°) from 285 m to 100 m on the east side of Dongsha Atoll in the northern South China Sea was observed by five T-string moorings. In deeper water depth, the waveform of depression wave was symmetry. Whiling shoaling, the front edge of depression wave was elongated, the rear edge of the wave remained its shape. As the wave propagated further shallow water, the bottom-trapped elevation wave formed. The phase speed was estimated 0.4 ms-1 - 1 ms-1. For the shoaling mechanism study, 78 nonlinear internal waves with clear waveforms were selected among the 5 T-string moorings data. Their wave amplitude (A), mixed layer depth (H1) and water depth (Ht) were identified. Statistics showed that the wave deformation was related to the ratio between wave amplitude and lower layer thickness. The critical conditions of wave transiting from depression to elevation occurred while A/(Ht-H1) is around 0.6±0.2. The depression wave would remain its shape propagating toward shallow water as A/(Ht-H1) is less than 0.45. When A/(Ht-H1) is greater than 0.83, all waves are in the form of bottom trapped elevation wave.
Turbulence observations near the Dongsha showed that the enhanced turbulence kinetic energy dissipation rates were found near the trough and in the wake of depression wave with the levels of 10-6 Wkg-1–10-5 Wkg-1. The dissipation rates induced by depression internal wave were about 100–1000 times higher than background values near the Dongsha Atoll.

目錄
謝誌 i
摘要 ii
Abstract iii
目錄 v
圖目錄 vii
表目錄 xii
第一章、緒論 1
1.1 前言 1
1.2 前人研究 6
1.2.1 內波觀測研究 6
1.2.2 內波數值模擬研究 14
1.3 研究動機與目的 17
第二章、觀測與分析及結果 19
2.1 觀測方法 20
2.1.1 溫度計 20
2.1.2 都卜勒剖流儀 22
2.2 分析方法 23
2.2.1 溫度計校正 23
2.2.2 調和分析 23
2.2.3 KdV理論 27
2.3 結果 28
2.3.1 溫度觀測 28
2.3.2 海流觀測 29
第三章、東沙大振幅非線性內波在大陸斜坡上淺化過程 38
3.1 現場觀測 39
3.2 觀測結果 40
3.2.1 溫度觀測 40
3.2.2 內波波形淺化轉變 47
3.2.3 內波流場結構觀測 49
3.3 淺化特性 55
第四章、東沙大振幅非線性內波波形變形機制 56
4.1 現場觀測 58
4.2 觀測分析結果 61
4.2.1 溫度觀測 61
4.2.2 現場觀測資料之KdV理論應用 63
4.2.3 非線性內波淺化過程 67
4.2.4 非線性內波波形之轉變 72
4.3 變形機制 76
第五章、東沙環礁紊流觀測 77
5.1 紊流儀簡介 77
5.2 資料分析方法 80
5.3 紊流觀測結果 84
第六章、結論與建議 94
6.1 結論 94
6.2 建議 96
參考文獻 97

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