Alluvial sediment sources in a glaciated catchment: the voidomatis basin, Northwest Greece

Woodward, Jamie C. and Lewin, John and Macklin, Mark G. (1992) Alluvial sediment sources in a glaciated catchment: the voidomatis basin, Northwest Greece. Earth Surface Processes and Landforms, 17 (3). pp. 205-216. ISSN 0197-9337

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Item Type:Article
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Abstract

diffraction (XRD) of the fine matrix component of four alluvial units and modern channel sediments in the Voidomatis River Basin of northwest Greece shows that fine sediment sources have changed considerably during the late Quaternary. The matrix fraction of the modern channel sediments is derived predominantly from erosion of local flysch rocks and soils. During the last glaciation, however, the fine sediment load of the Voidomatis River was dominated by glacially-ground, finely comminuted limestone materials. Limestone-derived fine sediment is not produced in significant amounts under modern climatic conditions. By combining this XRD work with a detailed programme of clast lithologic 1 analysis we have reconstructed former bedload and fine sediment load composition. The lithological properties of both the coarse (8-256 mm) and fine (< 63 μm) elements of the sediment load have varied markedly during the late Quaternary. A simple, semiquantitative assessment of fine sediment mineralogy, using diffractogram peak-height data, has provided a valuable complement to the information gathered from more traditional clast lithological techniques. Together, in favourable geological settings, fine fraction mineralogy and clast lithological analysis can provide a valuable tool for the reconstruction of late Quaternary alluvial environments.

Keywords:alluvial environment, alluvial sediment, channel sediment, glaciated catchment, Glaciation, lithological analysis, Quaternary, sediment source, X-ray diffraction, XRD, Greece, Voidomatis Basin
Subjects:F Physical Sciences > F840 Physical Geography
Divisions:College of Science > School of Geography
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ID Code:25158
Deposited On:26 Nov 2016 16:53

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