台灣嘉南平原地下水含有異常高濃度的砷(> 0.35 ppm)，其來源至今仍無定論。因地下水與含水層與阻水層沉積物有密切的地質相關性，這些沉積物應是地下水中砷最可能的來源。因此本研究分析位於台南縣錦湖之鑽井岩芯(165個)與嘉南地區河口及河岸(38個)沉積物樣本之礦物組成，並量測其砷、Al2O3、 CaO、 MnO、 TiO2、 Fe2O3、總碳及總有機碳含量與鍶和釹同位素比值。於含砷量高的岩芯沉積物區段行高解析之密集分析，以討論台灣西南部沉積物砷含量分佈變化，並推測高含砷量之沉積物與地下水之間的關連。
嘉南平原沉積物由砂、粉砂及黏土組成，無礫石。主要礦物為石英、長石及黏土礦物(伊萊石與綠泥石)。所有河口及河岸沉積物樣本及大部分岩芯沉積物樣本的砷含量皆低於 20 ppm (平均為 8.9 ppm)，與一般地殼物質相似(5-10 ppm)。但在錦湖岩芯中有6個黃色沉積物與5個灰黑色沉積物樣本的砷含量為30-435 ppm，這些皆屬阻水層沉積物，其深度分別位於嘉南平原第三與第四含水層內，由這些樣本之化學特性可推測兩種砷於沉積物中富集的機制。
第三含水層中含約2公尺厚的黃色沉積物，其中6個高砷樣本具相似之87Sr/86Sr與143Nd/144Nd比值，其砷含量由頂部及底部向此層中心遞減，形成此現象之可能機制為砷由含水層與阻水層交界處往阻水層內部遷移。在此模式中，地下水擷取含水層的砷，將其釋入至阻水層中，而阻水層中可擷取砷的介質可能是黏土礦物或是X光繞射無法偵測的鐵氫氧化物。
第四含水層中高砷沉積物樣本具相同143Nd/144Nd值，指示其碎屑成分源共同源區；但87Sr/86Sr值卻有顯著差異，且與砷含量呈現負相關，表示沉積物中有自生礦物生成，而這些自生礦物可富集砷，所以當自生礦物含量增加，87Sr/86Sr比值降低且砷含量增加。僅此類砷含量高之樣本含有石膏，表示當時的沉積環境為氧化環境，因而最可能富集砷的介質，是X光繞射無法偵測的鐵氫氧化物，但無法完全排除黏土礦物或有機物亦為砷之寄主。
綜合以上論述，第三含水層沉積物之砷局部富集現象為地下水砷與沉積物反應後沉澱所致；而第四含水層中之砷富集則是於氧化環境下沉積過程中形成。這些高砷沉積物的砷可能因地下水特性的改變，如有機物含量增加而釋出，使地下水中砷含量增高。依此推論，沉積物為地下水砷主要來源，而地下水的砷含量則與其化學特性有密切關連。

The source of arsenic in the high-arsenic groundwater from the Chainan plain in SW Taiwan has been an issue of debate. Because of their close association with the groundwater, aquifer and aquitard sediments should be firstly considered before postulating any other alternative sources. In this study, 165 sediment samples from a drill core from the Jin-Hu town and 40 alluvial and river bank sediment samples were analyzed for constituting minerals and concentrations of arsenic, Al2O3, CaO, MnO, TiO2, total iron oxides, total carbon, and total organic carbon (TOC) as well as 87Sr/86Sr and 143Nd/144Nd isotope ratios. Detailed high resolution analyses were carried out at the high-arsenic zones. These data reveal the distribution of arsenic in sediment at SW Taiwan and provide critical information for evaluating the relationship between high-arsenic sediments and high-arsenic groundwater.
The Chainan plain sediments are composed of sand, silt and clay without gravel. Their major constituting minerals include quartz, feldspar and clay minerals dominated by chlorite and illite. All the alluvial and river bank sediment samples and the majority of the core samples have arsenic contents below 20 ppm with an average of 8.9 ppm, typical of crustal materials. However, 6 yellowish samples and 5 grey-blackish samples from the Jin-Hu core contain 30-435 ppm arsenic. They are all aquitard sediments with the former and later being respectively intercalated in the depth ranges of the third and fourth aquifers beneath the Chainan plain. The geochemical characteristics of these high-arsenic samples lead to two contrasting mechanisms for observed arsenic-enrichment.
As indicated by their homogeneous 87Sr/86Sr and 143Nd/144Nd ratios, the 6 yellowish high-arsenic samples are from the top and bottom of a ~2 meter thick aquitard layer, in which arsenic concentration decrease systematically toward its center. These geochemical features are explained by inward arsenic-migration from the aquitar-aquifer contacts into the aquitard layer. In this model, the groundwater extracted arsenic from the aquifer sediments, then release arsenic into the associated aquitard layer, which contain relatively abundant arsenic up-taking minerals; in this case, clay minerals and/or XRD un-identified iron-oxy-hydroxides.
The high-arsenic samples from the depth range of the fourth aquifer have similar 143Nd/144Nd ratio, indicating derivation from a common detrital sources. However, their 87Sr/86Sr ratio varies well beyond analytical uncertainty, reflecting the addition of authigenic components. The inverse correlation between 87Sr/86Sr ratio and arsenic concentration is consistent with arsenic-enrichment caused by the involvement of low 87Sr/86Sr authigenic sediments. All these high-arsenic samples are distinct from other samples for containing gypsum, arguing unambiguously for an oxidized sedimentation environment. It can then be inferred that arsenic is concentrated in XRD un-identified iron-oxy-hydroxides, although the role of clay minerals and organic matters cannot be completely precluded.
In summary, the arsenic-enrichment in the third aquifers was caused by interaction with groundwater after sedimentation, while that in the fourth aquifer occurred during sedimentation under an oxidized environment. The arsenic in these high-arsenic sediments could be released into groundwater with proper chemical constituents, probably high contents of organic matters. In such a scenario, the source of arsenic in the high-arsenic groundwater from the Chainan plain is attributed to high-arsenic aquitard sediments; therefore, there is no need to postulate alternative sources distal from the groundwater. This model is strengthened by the low arsenic contents in the alluvial and river bank sediments.

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