濁流（Turbidity current）為常見的水下塊體運動。然而自Bouma（1962）發表探討濁流及濁流岩（Turbidite）文獻以來，大部分的研究均著重於海底的塊體運動，較少有湖相濁流之探討。石門水庫於颱洪期間數次大規模濁水現象的原因可能與濁流相關，使石門水庫成為探討湖相濁流的合適地點。本研究探討石門水庫底質沉積物之特性及分佈，希進一步了解庫底沉積物之時空分佈及成因。
本研究以3.5kHz底質剖面儀求得石門水庫表層（25公尺以內）沉積物剖面，再根據沉積物之分佈狀態，評估適合的岩心鑽探位置，而後於庫區上、中、下游鑽探總長度435公尺岩心共十五口，並將岩心局部製成厚1公分薄片供拍攝X光照片，及採樣進行雷射粒徑分析。
石門水庫底質剖面由深至淺可分成三個部分：
unit A位於庫區中、下游深度約40至45 m處，側向連續良好，有多起反射訊號；unit B在庫區上游，有多起反射訊號，但厚度較薄（約3至5 m），到庫區中、下游，反射訊號少且微弱或無反射訊號，厚度約8至10 m；unit C厚約5至6 m，有多道清晰的反射訊號，分佈於整個庫區。
底質剖面側向的變化有三種型態：
型態Ⅰ：向上突起的不規則反射訊號，分佈位置靠近岸邊；型態Ⅱ：凹陷的V形谷，凹槽內有多道清楚的反射訊號，分佈於庫區河道中央；型態Ⅲ：兩側高度落差大，高處的反射訊號數量多且沉積物較厚；低處的反射訊號數量少且較薄。以上型態可能分別代表三種地貌的沉積：岩石基盤、河道及充填物、堤岸與水道。
雷射粒徑分析儀測量CGS-03及CGS-04的21個標本，顯示庫底沉積物之平均粒徑為細粉砂或中粉砂且含泥量高。標本粒徑分佈有多峯分佈，且淘選度不佳。
觀察石門水庫歷年水位變化，可將民國85年至96年的水位變化分作三個時期：水位a期、水位b期及水位c期。此三個時期可能分別對應底質剖面unit A, unit B and unit C的沉積。
根據340個岩心X光照片，可將石門水庫沉積物分作五種岩相：
岩相Ⅰ：高密度濁流泥塊層；岩相Ⅱ：低密度濁流砂層；岩相Ⅲ：泥砂混合層；岩相Ⅳ：薄泥砂互層；岩相Ⅴ：泥層。
植物碎屑含量以庫區中游大灣坪以下的區域最多，但SM-04為例外，可能是此岩心較靠近岸邊所致；大灣坪以上的岩心中植物碎屑較少，但CGS-04為例外，此岩心位於三民溪注入口，可能由三民溪帶來較多植物碎屑。生物擾動愈往上游愈強烈，可能是上游的含氧量高，適合生物活動所致。
石門水庫的五口岩心（SM-11，SM-10，SM-08，SM-07和SM-06）中有高密度濁流岩（HDT）沉積。這些岩心主要分佈於庫區中、上游，且至少有十層高密度濁流沉積。愈往下游，泥塊愈小、圓度愈偏向次圓或圓且厚度愈薄，表示濁流的源頭在上游處。低密度濁流岩（LDT）在四口鑽井（SM-11，SM-08，SM-07和SM-04）中出現。主要分佈於庫區中、下游，較集中在下游，且至少有十二層低密度濁流沉積。
綜合底質剖面及岩心X光照片分析，顯示石門水庫有多次濁流沉積，沉積型態與分佈為：（一）厚層、粗顆粒沉積物為主的高密度濁流岩，主要分佈在庫區中、上游，（二）薄層、細粒沉積物為主的低密度濁流岩，主要分佈在庫區中、下游。此現象表示濁流可能為石門水庫中搬運較粗顆粒沉積物的主要機制。當濁流行進至大壩前時，能將底泥向上捲揚形成濁水，故庫底淤泥可能為濁水的主要來源且濁流可能為石門水庫庫水濁度劇升的機制之一。

Turbidity current is one of the most important sediment gravity flows. The deposits of turbidity currents, commonly called turbidites, were described by Arnold H. Bouma in 1962. However, most researches have focused on submarine sediment gravity flow deposits rather than those formed in lakes. During and after some of the recent typhoon seasons, tremendous amount of turbid water had been generated in the Shihmen Reservoir, which might have been triggered by turbidity currents. Therefore the Shihmen Reservoir is an appropriate place for studying lacustrine turbidites. This research analyzes the spatial and temporal variations of sediments in the Shihmen Reservoir, in an attempt to unveil the possible causes of the turbid water.
A 3.5kHz sub-bottom profiler was utilized to obtain the distribution of shallow (＜25 m) strata in the reservoir, in order to locate appropriate positions for core drilling. Fifteen cores with a total length of 435 m were then taken in the upper, middle and lower reaches in the Shihmen Reservoir. One-cm-thick slabs of sediments from the cores were photographed for X-radiographic images. The cored sediments were also measured for their size distribution by using Laser particle size analyzer.
Three units are identified in the sub-bottom profiles in the Shihmen Reservoir. From the bottom up, Unit A is recognized at the depth of 40~50 m in the middle and lower reaches. There are many laterally continuous reflectors in unit A. The overlying Unit B is thinner (about 3~5 m) and has many reflectors on the upper reaches. However, in the middle and lower reaches of the reservoir, there are fewer and weak reflectors, and they are thicker (about 8~10 m). The overlying Unit C, with a thickness of about 5~6 m, can be found throughout the whole area.
Laterally, 3 patterns of sub-bottom profiles can be identified. Pattern Type Ⅰ is irregular and protruding from the adjacent strata, and is located close to the shore. This pattern is interpreted as basement rocks. Pattern Type Ⅱ is v-shaped valley filled with many clear reflectors. This pattern is located in the central part of the reservoir and is interpreted to represent underwater valley and fill. Pattern Type Ⅲ is characterized by high relief, with more reflectors on the ridges and fewer reflectors in the basin. The sediments on the ridges are thicker than those in the basin. This pattern probably represents levee and channel deposits.
Laser particle size analysis on 21 samples (from cores CGS-03 and CGS-04) shows that the mean grain size is between fine silt to medium silt. The distribution of the particle size is multimodal and the sorting is poor.
Based on the reservoir level record taken between 1996 and 2007, three water interval periods are designated: Period a, b and c. It is suggested that sediments of the sub-bottom Units A, B and C were deposited during Period a, b and c respectively.
Five lithofacies are identified from the 340 core X-radiographic images: FaciesⅠis high-density turbidite composed of mud clasts and fine sand; Facies Ⅱ is low-density turbidite consisting of sand, silt and mud; Facies Ⅲ is composed of mixed sand and silt; Facies Ⅳ is made of alternating thin silt and mud layers; Facies Ⅴ is mud layer.
The amount of plant debris decreases downstream. Upstream from Ta Wan Ping (situated in the middle reach of the reservoir), plant debris are common (with the exception of SM-04, for the core is too close to the shore to receive much plant debris). Whereas downstream from Ta Wan Ping there are much less plant debris. But core CGS-04 is an exception, which is located close to a tributary, where more plant fragments are available. The degree of bioturbation in the upper reaches is more pervasive than that in the middle and lower reaches, possibly due to higher oxygen content in the upper reaches.
High-density turbidites (HDT) are observed in five cores: SM-11, SM-10, SM-08, SM-07 and SM-06, which are all situated in the middle and upper reaches of the reservoir, and at least 10 HDT layers have been identified. Mud clasts found in the cores become smaller, rounder and thinner downstream. The above observations indicate that the source of turbidity currents is from upstream.
Low-density turbidites (LDT) are found in four cores: SM-11, SM-08, SM-07 and SM-04, which are located mainly in the middle and lower sectors of the reservoir. There are 12 LDT layers in the cores.
X-radiographic images and 3.5kHz sub-bottom profiles indicate that turbidity currents are common in the Shihmen Reservoir. High-density turbidites (HDT) with sands and mud clasts dominate the upper and middle reaches, while low-density turbidites (LDT), composed of fine sediments are found in the middle and lower reaches.
It is possible that when turbidity currents moved downstream towards the Shihmen Dam, it reactivated and agitated the muds deposited previously, hence generated turbid waters during and after some of the typhoons. Thus, turbidity currents might be a major mechanism triggering the turbid water, and the reservoir bottom mud could be the main source of turbid water in the Shihmen Reservoir.

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