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完整後設資料紀錄
DC 欄位 | 值 | 語言 |
---|---|---|
dc.contributor.advisor | 黃武良(Wuu-Liang Huang) | |
dc.contributor.author | Jun-Chin Shen | en |
dc.contributor.author | 沈俊卿 | zh_TW |
dc.date.accessioned | 2021-06-12T17:56:14Z | - |
dc.date.available | 2008-02-18 | |
dc.date.copyright | 2008-02-18 | |
dc.date.issued | 2008 | |
dc.date.submitted | 2008-02-01 | |
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Ti-Chih., 15( 1), 127-151. 何春蓀,1959,臺灣之煤礦資源。臺灣省地質調查所彙刊,第10號,第1-164頁 何春蓀,1986,臺灣地質概論,增訂第二版。經濟部中央地質調查所,共163頁。 宋德濡,1996,台灣造山帶地殼特性之研究, 國立中央大學碩士論文。 李元希,1992,臺灣中央山脈中段的構造演化,國立臺灣大學碩士論文。 李協長,1992,金瓜石地區岩漿與礦化作用之定年學研究及其大地構造運動之隱示,國立臺灣大學碩士論文。 沈俊卿、吳素慧,2003,臺灣地區油母質之油氣生成模擬。中油公司探採研究所九十二年度研究報告,第259頁。 沈俊卿、孫美蓉、邱仲信,1994,煤系地層生油岩之潛能評估,中國石油公司探採研究所年度研究報告。 沈俊卿、郭政隆,1991,新竹苗栗地區煤層與油氣之關係,中國石油公司探採研究所年度研究報告。 周次雄,1978,新竹苗票油氣田打鹿頁岩之地球化學研究,中國石油公司探採所年度研究報告。 周次雄、翁榮南、郭政隆、鄭林存,1982,錦水油氣田凝結油之地化研究,石油鑽採工程,第二十三期,第228-253頁。 周次雄、郭政隆、林麗華、沈俊卿,1985,台灣西北部中新統油氣儲集之地球化學研究,探採研究彙報,第八期,第146-161頁. 周次雄等,1987,沙河1 號井生油岩評估報告,探採研究所內部報告。 周瑞燉、楊健一,1986,台灣西部沉積盆地之特性及其儲積油氣潛能,石油,第二十二卷,第一期,第2- 55頁。 林朝棨,1935,台中豐原地方第三紀及第四紀地層之地層研究。台北帝國大學理農部紀要,第十三卷,第三期。 林朝棨,1954,台灣之地質。台灣新誌,中華文化出版事業委員會。 邱仲信、郭政隆、吳素慧、林麗華、沈俊卿、周次雄,1996,煤樣油氣生成之地化模型研究。中油公司探採研究所八十五年度研究報告,第89頁。 紀文榮,1983,台灣南投縣國姓及信義附近之超微化石生物地層:探採研究彙報,第六期,第35-61頁。 胡錦城、林國安、周次雄、紀文榮,1990,台灣西北部等三紀盆地演化與油氣潛能之綜合評估 (2/2):中國石油公司探採研究所七十九年度研究報告。 張麗旭、何春蓀,1948,台中縣之大安背斜。地質論評。第十三卷,第1- 2期。 郭政隆,1997,鏡煤素反光率在台灣西部油氣探勘的應用,國立台灣大學地質學研究所博士論文,共302頁。 郭政隆、吳素慧、孫智賢、林麗華、翁榮南、林政遠、張錦澤、黃得時、黃守仁、謝建台、陳長謙, 2003,“油岩對比技術研究”,經濟部石油基金獎勵石油開發技術研究發展計畫期末執行報告,共381頁。 郭政隆、吳素慧、孫智賢、林麗華、張錦澤、林政遠、黃守仁、謝建台、俞聖法、趙美訓,2004,氣、油、岩對比技術研究,經濟部石油基金獎勵石油開發技術研究發展計畫九十三年度執行報告。 郭政隆、林麗華、沈俊卿、張錦澤、吳素慧、孫智賢,2000,台灣西北部生油岩生成油氣相態及潛量研究:中國石油公司探採研究所八十九年度研究報告。 郭政隆、邱仲信、沈俊卿、周次雄、吳素慧等,1995,台灣西北部油氣蘊藏地化研究,探採研究所彙報,第十八期,第393~405 頁。 陳振華,1993,由晚期新生代沈積物之岩象學與構造地層學研究探討台灣中西部褶皺逆衝帶之演化:國立台灣大學地質學研究所博士論文。 鄒常璽、張培礎,1989,煤田地质学.北京:煤炭工業出版社,第22∼23頁。 劉清華,1992,金瓜石第三長仁金礦床鏡煤素之研究.國立臺灣大學碩士論文。 蔡龍珆,1988,基隆一台北問煤層鏡煤素之共生次序含意,地質第8卷,第1- 2期,第63- 70頁。 | |
dc.identifier.uri | http://tdr.lib.ntu.edu.tw/jspui/handle/123456789/27138 | - |
dc.description.abstract | 在有機物成熟度的探討過程中,發現採自不同地區的煤層其鏡煤素反射率並未隨其氫指數增加而降低,而頁岩則與Lo,(1993)的頁岩中之鏡煤素反射率隨其氫指數增加而降低相同。為了進一步探討頁岩及煤層有機物成熟度差異的意義,本研究進行煤樣化學成份分析,以探討生物指標的成熟度工具,以作為比較參照。煤的成份霍烷類含量較豐富,固醇類相對偏低,故化學成份的成熟度指標以霍烷類較為可靠。但煤的霍烷類生物指標的成熟度指標,如Ts/(Ts+Tm)及C31 22S/ (22S+22R) 最常用成熟度工具均在煤中無法使用。因此本研究尋求新的工具。首先進行煤樣水合熱裂模擬,來探討人工熱成熟作用中生物指標的含量變化,再採集煤樣進行萃取分析後,發現以C31-22S, C31-22R homohopanes 及 C29, C30 moretanes四種成份所組成的參數如 (1) (normoretane/ moretane) / [C31 22S/ (22S+22R) ]; (2) (normoretane/ norhopane) / [C31 22S/(22S+22R) ]. (3) (moretane/hopane) / [C31 22S/ (22S+22R) ] 。可有效解決煤樣本身形成過程及外來因素所導致霍烷類的使用問題。這些參數之中又以(normoretane/ moretane) / [C31 22S/ (22S+22R) ]為最佳,因其於平衡後值的變動最小。同時也藉由這四種成份所組成的參數的達成平衡值之位置點,得知這些分析過臺灣煤樣的油窗起點約為0.6 %Ro。
另外,本研究也進行高成熟度化學成熟度指標的開發。為求工具使用的廣度,除芳香烴外,也針對飽合烴探討, pristane/ n-C17 、phytane/ n-C18及pristane/ phytane 為常用工具,但pristane/ phytane在有些樣品中可應用至1.5% Ro以上。 另外在高成熟度的應用方面,發現芳香烴中的 (3-MB)/ (4-MB+DBF),可避免MPDF在此範圍使用之不可靠的問題迎刃而解。 沉積環境所導致的差異之探討,先以同一煤層中所含碳質物在相同的熱應力下的鏡煤素反射率,以苗栗縣三義剖面分析結果顯示煤層與下覆砂層中所夾碳質物並無差異,為確認沉積環境對有機物成熟度的影響,接著再特別蒐集並分析13個與煤形成環境不同的十六份頁岩中沈積,而所受成熟作用幾乎完全相同的獨立碳質塊體,以探討其各項成熟指標的變化(包含鏡煤素反射率及化學的成熟指標),並以明德剖面的上福基砂岩中煤層、煤頁岩及頁岩在接近油窗時鏡煤素反射率及化學成份的變化,並探討其是否已進入油窗。探討完相同的熱應力下的影響後再進行垂直變化的探討。而根據豐富三號井採樣分析顯示,較高的鏡煤素反射率往地層淺部較年輕的卓蘭層延伸,而並未隨埋藏深度變淺而降低,此與露頭岩樣分析所得,南莊層以上年輕地層頁岩均較煤層鏡煤素反射率為高的結果相同。換言之,二次沉積有機物佔多數的現象係自南莊層開始出現。所顯示的地質意義,就是不排除自南莊層沉積時期開始,即由陸地侵蝕而帶來大量的再沉積有機物充斥於頁岩中,也可能受造山運動影響所致。而年輕地層的真正鏡煤素反射率則由頭嵙山層的碳質物分析來獲得並驗證前述發現。 十六份頁岩中獨立碳質塊體,所顯示沈積對有機物成熟度的影響,以MPI-1所計算出來的成熟度值變化較小。除兩個樣品值較高外,其餘的值變化均小且樣品間的差異不大,顯示其為一可靠的成熟度工具。換算出來的Ro%值以0.6MPI-1 +0.4所得的較接近鏡煤反射率(Ro%),也證實此一比值適用範圍可延伸至0.4 %Ro,而不是僅在0.65 % Ro以上,反而0.7 MPI-1 +0.22換算式被認為適用範圍可至0.35 %Ro,但本文所得的換算值卻都明顯偏低,顯然並不適用於此一成熟度範圍。計算值與測值的高低並無明顯正相關。鏡煤素反射率的差異則在0.1%Ro以內。此項探討所獲得的結果為就岩性的差異而言,所分析的桂竹林層十六份頁岩段樣品,夾含於粉砂層中的與頁岩中的碳質塊體之各項分析值中僅甲基菲異構物9MP/1MP比值有明顯差異。頁岩中的樣品9MP/1MP比值較高。而MPI-1則顯示粉砂層的樣品有較高值。 除前述在煤樣的油窗探討外亦進行煤樣的天然氣生成探討,以不同種類樣品的水合熱裂模擬結果天然氣累積生成量,以同為194小時加溫時間顯示原始氫指數與甲烷氣的生成量呈正相關,其關係式為甲烷生成量=1.5653(HI)0.2194,C2+亦隨氫指數增加而增加,C2+ = 0.4869(HI)0.3126,但甲烷相對乙烷生成量的比值卻隨氫指數增加而降低,其關係式為C1/C2 = 8E-0.7(HI)2- 0.0017(HI)+ 4.2356。換言之,氣體之生成量不論甲烷或C2+隨氫指數值增加,異丁烷對正丁烷隨加熱時間降低後再微幅上昇。 在完成水合熱裂模擬油氣形成後,進行火山噴發岩熱成熟作用對圍岩中有機物所造成的鏡煤素反射率變化,結果顯示碳質頁岩層有機物的成熟度,由接近火成岩體的2.44 %Ro在短距離之內急劇降為1.05 %Ro。有機物的成熟度值係由產油高峯橫跨至氣窗。這些分析樣品中殘留的可裂解碳氫化合物皆為0的結果,顯示雖然火成熱成熟作用所造成的鏡煤素反射率並不高且未達正常深埋所造成完全轉化階段,但卻能令有機物完全裂解而無殘留,可提供較預期為多的油氣,此與高溫高壓水合熱裂及深層火成岩脈所導致的結果並不同。而此一分析結果顯示殘留的可裂解碳氫化合物的存在與否並未影響煤的煤化作用。 | zh_TW |
dc.description.abstract | The distribution of hopanoids and alkanes in bitumen extracts of coals, coaly shales, and shales from northwestern Taiwan has been measured to assess the maturity of potential petroleum source rocks in the studied area. The C31 homohopane isomers of the studied coals and coaly shales attain equilibrium at maturity corresponding to 0.6% Ro measured in coals or 0.65% Ro in adjacent shales. A proposed parameter using hopanoid ratios reveals a more consistent trend and approaches a steady value at maturity similar to the C31 homohopane isomer ratio. The results show that the onset of the main phase of petroleum generation in northwestern Taiwan takes place at maturity corresponding to VR of 0.6% Ro measured in coals or coaly shales and probably higher VR in shales. The distribution of pristane, phytane n-C17 and n-C18 confirms the validity of the conventional maturity indicators if the samples are from the same source, but shows depositional or organic-source controls. The source influence on the phytane/n-C18 ratio appears to be larger than that on the pristane/n-C17 ratio. The phytane/n-C18 ratio is also less sensitive to maturity than that of the pristane/n-C17 ratio.
The pristane/phytane ratios in the studied coals and coaly shales, in contrast to the pristane/n-C17 ratio, continue to decrease to maturities beyond the oil window up to 1.5% Ro and therefore may be applicable to high maturity sources. Thirteen desmocollinite-rich organic debrises isolated from a transgressive marine shale with a similar thermal history were characterized to study the influence of organic composition and host rocks on the variations of different maturity parameters. The results show that both maceral types of organic debrises and lithology of host rocks have little influence on the variation in vitrinite maturity. The vitrinite reflectance (0.4 to 0.55 %Ro) measured from these organic debrises, however, are slightly lower (about 0.1%Ro difference) than those from the dispersed organic matter in shale. The maturity of the organic debrises indicated by MPI-1 is consistent with that indicated by vitrinite reflectance, and the applicability of the MPI-1 indicator may be extended to maturity as low as 0.4 %Ro. The MPI-1 maturity is generally lower in samples from the siltstone than those from the shale, suggesting that the MPI-1 maturity indicator may be affected by depositional or diagenetic environments. The hopanoid index of C31 22S/(22S+22R) homohopane ratio indicates a maturity corresponding to the vitrinite reflectance measured from organic debrises. The maturities of the organic debrises indicated by three parameters (%Ro, MPI, and hapanoid ratio) are in good agreement and that the source rocks in the studied formation are very close to the onset of oil generation. The ratios of cadalene/ retene and fuoranthene/ pyrene vary significantly with the lithology: higher in samples from the siltstone than those from the shale. Coals from different formations in Northwestern Taiwan were treated with hydrous pyrolysis to get its genetic potential. Genetive volume of gas from these samples were found in this study. It can be easily calculated by hydrogen index (C1 =1.5653(HI)0.2194,C2+ = 0.4869(HI)0.3126). C1/C2 increase with hydrogen index too(C1/C2 = 8E-0.7(HI)2- 0.0017(HI)+ 4.2356 ). | en |
dc.description.provenance | Made available in DSpace on 2021-06-12T17:56:14Z (GMT). No. of bitstreams: 1 ntu-97-D89224003-1.pdf: 1978041 bytes, checksum: b0321d5f076944a893112253a9363583 (MD5) Previous issue date: 2008 | en |
dc.description.tableofcontents | 口試委員會審定書 i
致 謝 ii 摘 要 iii 目 錄 viii 圖 目 錄 x 表 目 xv 表 目 xv 引 言 1 第一章 台灣煤、煤頁岩及頁岩中生物指標在成熟度的功能及應用 3 1.1 Introduction 4 1.2 Experimental Methods 6 1.3 Results and Discussion 10 1.4 Conclusions 22 第二章 相同熱應力下海進頁岩中碳質塊體之成熟度的分析探討 28 2.1 Introduction 29 2.2 Geological Setting 32 2.3 Experimental Methods 34 2.4 Results and Discussion 37 2.5 Conclusions 48 第三章 台灣新第三紀煤系生油岩之水合熱裂分析 55 3.1 前言 56 3.2 研究方法與步驟 58 3.3 結論 60 第四章 近油窗階段的有機物成熟度與化學成份關係之探討 70 4.1 前言 72 4.2 地質概述 76 4.3 樣品分析方法及條件 77 4.4 結果 79 第五章 井下鏡煤素反射率的垂直分佈及地質意義 93 5.1 前言 94 5.2 地層概述 96 5.3 前人研究 97 5.4 樣品分佈及特性 99 5.5 樣品分析方法 100 5.6 結果 101 第六章 年輕沉積層中有機物鏡煤素反射率之分析與探討 109 6.1 前言 110 6.2 樣品分佈及特性 113 6.3 地質概述 114 6.4 樣品分析方法 116 6.5 結果 118 第七章 火山噴發岩對有機物成熟度及油氣形成的影響 125 7.1 前言 126 7.2 樣品分佈及特性 127 7.3 樣品分析方法 129 7.4 結果 131 總 結 137 | |
dc.language.iso | en | |
dc.title | 台灣新第三系有機物熱成熟指標之探討 | zh_TW |
dc.title | Organic Maturity Indices for Neogene Formations in Taiwan | en |
dc.type | Thesis | |
dc.date.schoolyear | 96-1 | |
dc.description.degree | 博士 | |
dc.contributor.oralexamcommittee | 劉聰桂,紀文榮,蔡龍珆,郭政隆,林殿順 | |
dc.subject.keyword | 煤,有機物成熟度,生物指標,天然氣生成,沉積環境, | zh_TW |
dc.subject.keyword | Coal,Shale,Biomarker,Vitrinite,Organic Maturity,Sedimentary environment, | en |
dc.relation.page | 140 | |
dc.rights.note | 有償授權 | |
dc.date.accepted | 2008-02-01 | |
dc.contributor.author-college | 理學院 | zh_TW |
dc.contributor.author-dept | 地質科學研究所 | zh_TW |
顯示於系所單位: | 地質科學系 |
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