臺灣博碩士論文加值系統

臺灣地處新生代弧陸碰撞造山帶，高侵蝕速率與高沉積速率的影響下，第四紀沉積層廣布於海岸平原前陸盆地。受到構造活動、海水面變遷與沉積物供應等因素影響，晚更新世以來沉積層中記錄豐富的環境變化史。為了解西部平原的環境變化，本研究分析了雲林至嘉義一帶尚未詳細研究的鑽井岩心的沉積相，並蒐集了台灣西部以及西南部平原地區鑽井資料與研究結果，期望能了解晚第四紀末次最大冰期以來海水面上升對西南部海岸環境所造成的影響。另外針對全球海水面、構造活動與沉積物供應等沉積環境變化的控制因素，以解析這三項因素如何操控西部平原沉積環境與海岸線的變遷。
經由層序與環境分析，得知末次最大冰期時西部平原出露水面，受到風化侵蝕形成不整合面（層序界限）。而此時期旺盛的河流下蝕作用，在海側形成數個下蝕凹谷，其中以高屏溪與曾文溪所形成的規模最大。由剖面對比建立的古環境變化史如下：約18,000年前因大規模暴露地表而形成土壤層及侵蝕面。約16,000~14,000年前，海水入侵到下蝕凹谷形成河口灣。約14,000~12,000年前，海水面逐漸上升，下蝕河谷被淹沒形成溺谷，且海岸線已推移至現今海岸平原中部。約9,500~9,000年前屏東平原以及雲嘉南平原南段先達到最大海漫面時期，而其他區域仍持續海進。約8,500~8,000年前雲嘉南平原北段至中段、台南與高雄北部地區以及高雄地區才陸續達到最大海漫面時期，此時屏東平原以及雲嘉南平原南段已呈現海退樣貌。彰化平原則必須到7,500~7,000年前才達到最大海漫面時期。6,000~4,000年前環境逐漸變淺，海岸線向海側移動至平原中部，此時台南台地已出露水面，而大灣低地仍覆蓋著海水形成大灣海峽。4,000年前至今環境快速變淺，海岸線快速向海側移動至今日樣貌。
研究結果顯示西部平原的環境變遷受到全球海水面、構造活動與沉積物三者交互作用，使不同平原具有不盡相同的古環境演變，而古地形起伏與坡度同樣會影響海岸線與環境的變遷。如各個平原達到最大海漫面時期的時間並不相同，但大致可以由形成時間分為三種區域，分別代表受到不同程度海水面變化、構造作用與沉積物供應的影響。另外經由自8,000年來平原地殼垂直變動速率的計算，得知6,000~4,000年之間嘉南平原海岸線快速朝海側遷移15~10公里，可歸因於受到平原東側傾斜台地的抬升，造成海岸線快速移動到平原西側的沉降盆地內。

In order to understand the depositional environment evolution and solve the impacts of eustacy, tectonic and sediment yield on western coastal plain of Taiwan since the last glacial maximum period, we use several borehores to reconstruct it. Based on the depositional environment, sequence stratigraphy and radiocarbon dating, significant environment and shoreline changes are recognized.
(1) The western Taiwan is characterized by a subaerial environment and formed several incised valleys during the sea-level fall in the last glacial maximum period.
(2) The environment experienced the sea-level rising with retrogradational deposition of the trangression system tracts and the shoreline was migrated into the incised valley and formed a drowned valley during 16,000~14,000 years ago.
(3) The ongoing sea-level rise causes the valley filled and environment changed deepen into intertidal zone during 14,000~12,000 years ago.
(4) Most areas occurred the deepest environment from shoreface to inner offshore during 8,500~8,000 years ago, and maximum flooding surface formed. But Tainan and Pingdong plain was experience the deepest environment earlier than 8,500~8,000 years ago.
(5) After 8,500~8,000 years ago, the system occurred progradational deposition of the highstand system tracts. The sediments progradated to the seaward, hence, the environment was shallow from intertidal zone to fluvial environment and the shoreline was retreated and migrated to the westward to the recent appearance.
The period of maximum flooding surface in different parts of the western plains are not the same. Based on the occurrence time of maximum flooding surface, it can be roughly divided into three types. Each type represents the complex interplay between eustacy, tectonics and sediment supply. In addition to the above three factors will control the depositional environment and shoreline changes, the ancient topography and slope will also affect the shoreline and environment evolution.
Based on the vertical deformation rate rechecked in order to solve the impact on shoreline evolution during 6,000~4,000 years ago. The result shows the eastern part of coastal plain is uplift environment, causing shoreline move quickly into the western side of the subsidence coastal plain.

誌謝 I
摘要 II
Abstract IV
目錄 VI
圖目錄 X
表目錄 XIII
第一章 前言 1
1.1 研究動機 1
1.2 研究目的 3
1.3 地質背景與前人研究 4
1.3.1 嘉義地區 4
1.3.2 末次最大冰期以來海水面變動 6
1.4 研究材料 7
1.5 研究方法 10
第二章 鑽井岩心岩相分析與砂質沉積物成分觀察 17
2.1 岩相分析 17
2.1.1 礫相 19
2.1.2 砂岩相 19
2.1.3 砂岩泥岩互層相 21
2.1.4 泥岩相 22
2.2 砂質沉積物成分觀察 24
第三章 岩相組合與沉積環境 26
3.1 以波浪與暴風為主的濱面-淺海沉積體系 26
3.1.1 內遠濱相（Inner Offshore Facies） 26
3.1.2 濱面相（Shoreface Facies） 28
3.2 沿岸砂洲-潟湖沉積體系 29
3.2.1 潮坪相（Tidal Flat Facies） 29
3.2.2 沿岸砂洲相（Longshore Bars Facies） 30
3.2.3 潟湖相（Lagoon Facies） 30
3.2.4 潮汐水道相（Tidal Channel Facies） 31
3.2.5 沼澤相（Marsh Facies） 31
3.2.6 河口砂洲相（River Mouth Bar Facies） 32
3.3 陸相河流沉積體系 32
3.3.1 曲流河相（Meander Facies） 33
第四章 層序分析 34
4.1 層序界限 36
4.2 最大海漫面 36
4.3 低水位體系域 37
4.4 海進體系域 38
4.5 高水位體系域 38
4.6 層序分析結果 39
4.6.1 蔡厝井 39
4.6.2 崙子井 39
4.6.3 三和井 39
4.6.4 北港井 40
4.6.5 瓊埔井 40
4.6.6 大溝井 40
4.6.7 水林井 41
4.6.8 安和井 41
4.6.9 東榮井 41
4.6.10 東石井 42
4.6.11 大崙井 42
4.6.12 竹圍井 42
4.6.13 新港井 42
4.6.14 嘉義井 43
4.6.15 新埤井 43
4.6.16 南新井 43
4.6.17 港墘井 44
第五章 綜合分析 63
5.1 剖面對比 63
5.1.1 海側南北向剖面：蔡厝-大溝-瓊埔-港墘 63
5.1.2 平原中部南北向剖面：北港-新港-安和-新埤-大崙 64
5.1.3 山麓側南北向剖面：三合-東榮-南新-嘉義 65
5.1.4 北側東西向剖面：大溝-水林-北港-崙子-三和 66
5.1.5 南側東西向剖面：東石-港墘-竹圍-新埤-大崙-嘉義 67
5.2 末次最大冰期以來嘉義地區的古環境演化 74
1. 末次最大冰期，約18,000年前 74
2. 約11,000年前 74
3. 約8,000年前 75
4. 約5,000年前 75
5. 約4,000年前至今 75
第六章 西部平原環境變化 78
6.1 西部平原地區環境 78
6.1.1 彰化平原 78
6.1.2 雲嘉南平原北段 81
6.1.3 雲嘉南平原中段 84
6.1.4 雲嘉南平原南段 87
6.1.5 台南與高雄北部地區 90
6.1.6 高雄地區 94
6.1.7 屏東平原 97
6.2 末次最大冰期以來的海岸線變遷 101
第七章 討論 106
7.1 海進事件的時間記錄 106
7.2 最大海漫面時間 106
7.2.1 彰化平原 108
7.2.2 雲嘉南平原北段-中段、台南、高雄地區 109
7.2.3 雲嘉南平原南段與屏東平原 110
7.3 相對海退時期海岸線與環境變化的紀錄 111
第八章 結論 114
參考文獻 116
附錄：鑽井岩心紀錄 130

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