Trace element distribution and Cr(VI) speciation in Ca-HCO₃ and Mg-HCO₃ spring waters from the northern sector of the Pollino massif, southern Italy

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• 作者：S. Margiotta^a ; G. Mongelli^b ; ^{giovanni.mongelli@unibas.it} ; V. Summa^a ; M. Paternoster^b ; S. Fiore^a
• 关键词：Spring waters ; Hexavalent chromium ; Trace elements ; Serpentinites ; Apennines
• 刊名：Journal of Geochemical Exploration
• 出版年：2012
• 期刊代码：44_03756742
• 类别：ear
• 出版时间：April, 2012
• 卷：115
• 期：Complete
• 页码：1-12
• 文件大小：1613 K

摘要

Weathering of outcrops of ultramafic rocks (remnants of ancient oceanic crust) is a source of biologically toxic trace elements, particularly first row transition elements. The Cr and Ni concentrations of serpentinite and metabasite outcrops in the northern sector of the Pollino massif (Lucanian Apennines, southern Italy) are hundreds of orders of magnitude higher than those of the upper continental crust. In this region, exposed intermediate to lower crustal rocks are significantly enriched in Ni, Cr, and V relative to the average upper continental crust. We evaluate the levels and distributions of trace elements of environmental concern, including Cr (as total dissolved Cr and Cr(VI)), V, Mn, Fe, Ni, Cu, Zn, As, Pb, and U, in spring waters from the northern sector of the Pollino massif.

The major solutes in the spring waters from this region are Mg-HCO₃ and Ca-HCO₃. The Mg-HCO₃ type waters are produced mainly through the interaction of meteoric waters with serpentinites, whereas the Ca-HCO₃ type waters are produced through the interaction of meteoric waters with Ca-rich rocks (i.e., carbonate rocks, calc-schists, and metabasites). Thermodynamic evaluation indicates that in the MgO-SiO₂-Al₂O₃-H₂O system, waters flowing in serpentinites fall in the kaolinite field, close to the kaolinite-Mg-vermiculite phase boundary. This result arises because kaolinite is a relatively early reaction product, which is consumed to produce Mg-vermiculite and further Mg-saponite. In the CaO-SiO₂-Al₂O₃-H₂O system, Ca-HCO₃ type waters fall either in the field of gibbsite or kaolinite, depending on dissolved silica.

Chromium (VI) contamination associated with local mineralogy and with maximum admissible concentration > 5 渭g L^鈭?#xA0;1 was observed for nine springs (both Mg-HCO₃ and Ca-HCO₃ type waters). The Cr(VI)-rich Ca-HCO₃ springs are not located in serpentinites. However, some of these waters likely acquire their high Cr levels from interacting with serpentinite clasts, as in the case of springs flowing through conglomerates. In addition, Cr(VI) contamination is not limited to waters interacting with serpentinites or serpentinite clasts, because in one case weathering of garnet-rich gneiss is responsible for the release of significant amounts of Cr(VI) in solution.

Finally, studies are needed to address the potential health risks associated with the observed high concentrations of Cr(VI) in waters from the Pollino massif area. A mode-of-action analysis is needed to evaluate adverse health risks associated with exposure to Cr(VI) in drinking water, especially as Cr contamination is not limited to springs flowing through serpentinites.