利用地電阻影像法計算水文地質參數：以屏東平原為例

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朱佾蓁(Yi-Chen Chu) 查詢紙本館藏

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地球科學學系

論文名稱

利用地電阻影像法計算水文地質參數：以屏東平原為例
(Estimation of hydraulic parameter using electrical resistivity tomography（ERT : A case study in the Pingtung Plain, Taiwan)

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摘要(中)

地電阻法已被廣泛用於確定層狀介質的厚度和電阻率，本研究於屏東平原進行地電阻施測，此研究目的為透過地電阻法了解屏東平原區域水文特性與計算其水文地質參數，希望此研究能夠作為水文地質評估參考並提升數值模擬能力。本研究地點有二，其一位於大樹區大樹國小，於校區內建置一井地地電阻監測測線；其二研究地點位於大寮區臺灣中油大寮水源站，先於2017年進行地電阻一次性施測期間進行抽水作業，同時收集不同抽水時段地電阻資料，接著於2019年建置一地表地電阻監測測線，期間內進行例行抽水作業，可藉此來了解地下水抽取與地電阻的關聯性。大樹區域之地電阻剖面結果顯示，降雨前後測量之地電阻剖面有明顯的電阻率分佈變化，變化範圍根據現地水位資料顯示，為地下水位以下為飽和帶，此電阻率反映影響原因可能為受到雨水(室溫)慢慢入滲至地下時(地下水水溫約15oC )，造成地下水層溫度的改變，進而影響地層電阻率改變，根據深度與時間，可推估其水力傳導係數為1.73*10-4 m/ s。大寮區域 2017 年 8 月前導實驗結果隨著抽水事件水位洩降約 10 米。接著於2019 年進行地電阻監測期間，隨著抽水事件，計算區域相對飽和度變化，其飽和度變化範圍於深度10~20 米，此結果更驗證出此區域抽水洩降範圍。將大寮區域之電阻率利用Kozeny-Carman-Bear equation 可推算出水力傳導係數約為10−4~10−3m/s 且孔隙率約為15%~30%。將此方程式利用屏東平原第四紀沖積層鄰近嶺口礫岩之區域水文地質參數基本資料代入，其結果顯示粒徑小之砂岩泥岩對應之井測電阻率較小，透水係數也有較小的趨勢，且受壓密作用影響，隨深度越深，孔隙率有變小的趨勢。屏東平原西側為嶺口礫岩與全新世台地堆積層與第四紀沖積層，粒徑大小較一致，其井測電阻率值範圍廣，深度分布廣，但透水係數範圍皆落在10−3~10−4 m/s。

摘要(英)

Electrical resistivity surveying methods have been widely used to determine the thickness and resistivity of layered media for the purpose of assessing groundwater potential in fractured unconfined aquifers. In this study, we used Electrical Resistivity Tomography (ERT)
monitoring system at two study sites in the Pingtung Plain. One is the surface-borehole survey line at the Dashu, Kaohsiung City, Taiwan, and the other is the surface survey line at the Daliao, Kaohsiung City, Taiwan. We analyzed the change in the electrical properties of the gravel layer during the rainfall season at the Dashu site and analyzed the groundwater level change
by ERT method during the pumping event at the Daliao site which is the pumping station to understand the groundwater replenishment situation. The ERT results of Dashu site show that there is a significant change in the resistivity distribution of the ground resistance profile measured before and after rainfall. The resistivity can be calculated Relative Water Saturation (RWS) of the shallow formation fluid, and it reveal the permeability of the gravel layer and the hydrogeological characteristics of the sites. Affected by rainwater infiltration, the vertical infiltration of shallow aquifers is obvious, while the deep aquifers may be subject to vertical and horizontal infiltration to produce relative saturation changes. Due to the obvious vertical infiltration of shallow aquifers, depending on the depth and time , The hydraulic conductivity can be estimated as 1.73*10-4 m/ s . In August 2017, the ERT results of Daliao site show that it dropped about 10 meters with the water level of the pumping event, which is in line with theoretical estimates. During the ground resistance monitoring in 2019, with the pumping event, the relative saturation change of the area is calculated,
and its saturation change range is at a depth of 10 ~ 20 meters. Using the Kozeny-Carman-Bear equation of the resistivity of the Daliao area, the hydraulic conductivity can be estimated to be about 10−4~10−3m/s and the porosity is about 15% ~ 30%, as a reference for
hydrogeological parameters. Furthermore, we use the hydraulic conductivity coefficient theoretical trend line to analyze the data of WRA’s 34 wells in western Pingtung Plain. The results show that the sandstone and mudstones with small variables have smaller well-measured resistivity and a lower hydraulic conductivity. Affected by compaction, the porosity tends to decrease with increasing depth. On the west side of the Pingtung Plain, the particle sizes are relatively consistent, and the hydraulic conductivity is 10−4~10−3m/s .

關鍵字(中)

★ 地電阻法
★ 水文地質參數
★ 相對飽和度
★ 水力傳導係數

關鍵字(英)

論文目次

中文摘要 i
Abstract ii
誌謝 iv
目錄 v
圖目錄 vii
表目錄 x
第一章緒論 1
1-1 研究動機與目的 1
1-2 前人研究 2
1-3 研究區域概述 4
1-4 本文介紹 17
第二章研究原理與方法 19
2-1 地電阻影像剖面法簡介 19
2-2 儀器簡介 21
2-3 電極陣列 23
2-3-1 傳統陣列 23
2-3-2 混編陣列 23
2-4 水文地質概念 25
2-4-1 地表下水之流向 25
2-4-2 影響半徑 25
第三章資料處理與分析方法 27
3-1 原始資料處理 27
3-1-1 移除自然電位計算 27
3-1-2 阻抗解算 28
3-2 篩選資料 29
3-2-1 重複施測誤差 30
3-2-2 穩定電極配對資料篩選 30
3-3 逆推地電阻剖面 31
3-3-1 逆推理論 31
3-3-2 逆推資料 33
3-3-3 逆推資料門檻 33
3-3-4 逆推方法與設定 34
3-3-5 逆推過程 35
3-4 水文地質參數計算與分析方法 37
3-4-1 相對飽和度 37
3-4-2 地層電阻率與水力傳導係數 38
第四章研究結果 41
4-1 大樹區域地電阻監測 41
4-1-1 資料收集與處理 41
4-1-2 地電阻剖面分析 42
4-1-3 降雨效應分析 42
4-2 大寮區域地電阻一次性施測 50
4-2-1 資料收集與處理 50
4-2-2 抽水效應分析 50
4-3 大寮區域地電阻監測 58
4-3-1 資料收集與處理 58
4-3-2 抽水效應分析 60
4-3-3 降雨效應分析 62
第五章討論與結論 94
5-1 電阻率影響因素 94
5-2 降雨效應之影響 95
5-2-1 大樹區域 95
5-2-2 大寮區域 96
5-3 抽水效應之影響 101
5-3-1 抽水洩降範圍與電阻率空間變異 101
5-3-2 抽水效應之地電阻反應延遲 101
5-3-3 鄰近抽水井之視電阻率擾動 102
5-4 水力傳導係數推算 103
5-4-1 大樹區域 103
5-4-2 大寮區域 104
5-4-3 屏東平原 104
5-5 結論 112
參考文獻 114

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指導教授

陳建志(Chien-Chih Chen)

審核日期

2020-8-12

推文