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A new type of slumping-induced soft-sediment deformation structure: the envelope structure

Geology 196, 31–45. Mulder, T. & Alexander, J., 2001. The physical character of subaqueous sedimentary density currents and their deposits. Sedimentology 48, 269–299. Nemec, W. & Steel, R.J., 1984. Alluvial and coastal conglomerates: their significant features and some comments on gravelly mass-flow deposits. [In:] Koster, E.H. & Steel, R.J. (Eds.): Sedimentology of Gravels and Conglomerates. Memoir of the Canadian Society of Petroleum Geology 10, pp. 1–31. Neuwerth, R., Suter, F., Guzman, C.A. & Gorin, G.E., 2006. Soft-sediment deformation in a

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Depositional environment of a fan delta in a Vistulian proglacial lake (Skaliska Basin, north-eastern Poland)

. 2002. Quaternary geology of eastern Germany (Saxony, Saxon-Anhalt, South Brandenburg, Thuringia), type area of the Elsterian and Saalian Stages in Europe. Quatern. Sci. Rev., 21: 1275-1346. EYLES N., CLARK B.M. & CLAGUE J.J. 1987. Coarsegrained sediment gravity flow facies in a large supraglacial Lake. Sedimentology, 34: 193-216. FOLK R.L. & WARD W.C. 1957. Brazos River bar, a study in the significance of grain size parameters. J. Sediment. Petrol., 27/1: 3-26. FERNANDEZ L.P., AUGEDA J.A., CALMENDERO J.R., SALVADOR C

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Evaluation of Groundwater Quality Using Water Quality Indices in Parts of Lagos-Nigeria

Multivariate Analysis . J. Appl. Sci. Environ. Manage. 15 (1), 121-125. American Public Health Association (APHA) 1998. Standard methods for the examination of water and wastewater, (20th ed.), APHA, Washington DC, 2005-2605. Asiwaju-Bello, Y.A., Oladeji, O.S. 2001. Numerical modelling of ground water flow patterns within Lagos metropolis, Nigeria. Nigerian Journal of Mining and Geology 37 , 185-194. Bharti, N., Katyal, D. 2011.Water quality indices used for surface water vulnerability assessment. Inter. J Environ. Sci 2 (1

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OSL dating of the late Quaternary slip rate on the Gyaring co Fault in central Tibet

landforms, we mainly sampled the uplifted side of the GCF and the abandoned western edges of alluvial fans and/or preserved river terrace risers. This approach reduces the possibility that later erosion may influence our results and interpretations. OSL dating was used to study the northern segment of the GCF at the Aerqingsang and Quba sites ( Fig. 1 ). Six samples were collected from the alluvial sediments. To avoid potential exposure to daylight whilst sampling, sediments for equivalent dose ( D e ) determination were only taken from the middle part of each steel

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Optical dating of sediments from manas lake in northwestern china: Paleoenvironmental and neotectonic implications

Sampling and laboratory procedures Sampling sites Samples were collected from two sites in Manas Lake (sites 1 and 3 on Fig. 2 ). OSL samples were taken either by hammering stainless steel tubes (30-cm long with 5-cm diameter) into an exposed sedimentary section (site 1), or by taking block samples (site 3). Both ends of the tubes were then sealed immediately with tissue papers and tapes to avoid any exposure to light or loss of moisture content. For block samples, they were sealed in plastic bags and were wrapped with tapes to avoid breakage during transport

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Luminescence chronology of alluvial fan in North Bengal, India: Implications to tectonics and climate

) The study region lies in the northern part of West Bengal, India. (b) The figure shows the tectonic division of the Himalayas and the present study area, (c) The figure shows the major geomorphic features in the study area. The sampling sites are marked with red star. The northern most fault known as Gorubathan is marked by black line just below the Samsing surface. The two other E-W scarps/faults viz. Matiali and Chalsa are also shown in the figure. The NNE-SSW and nearly N-S scarps along which the Murti and Neora rivers flow respectively are also shown in the

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Identifying the degree of luminescence signal bleaching in fluvial sediments from the Inner Mongolian reaches of the Yellow River

channel, have consequently caused substantial social, economic and environmental problems ( Ta et al ., 2008 ; Wu et al ., 2006 ). Up-river, the Yellow River flows through the Chinese Loess Plateau (CLP) and the Tengger and Hedong deserts. It is bordered by the Ulan Buh and Hobq deserts, the Ten Great Gullies (through which ten tributaries enter the main stream of the Yellow River) in the south of its Inner Mongolian reaches ( Ta et al ., 2003 ). These tributaries originate from the centre of the Ordos Plateau (which is also the rainstorm centre of the Ordos Plateau

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The history of the sedimentation processes and heavy metal pollution in the Central Danube Delta (Romania)

), facilitating permeability and water exchange with the other specific limnophilous units. The phytoplankton and zooplankton levels in both lakes are high, and the development of green-blue algae is favourable ( Oosterberg et al ., 2000 ). Lake Iacob is part of the Rosu-Puiu lake complex, and has a total surface area of 2208 ha (600 ha open water, 360 ha potentially floating reed and 1248 ha inundated reed). The lake is 4.6 km long, and 1.6 km wide through a flow lake. It is 3.63 m deep and situated at an altitude of 1.8 m. The basin of Lake Iacob consists of a depression

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Luminescence dating of Holocene beach-ridge sands on the Yumigahama Peninsula, western Japan

The Yumigahama Peninsula is on the Japan Sea coast of western Japan ( Fig. 1 ). It is a sandy coastal barrier that is 20 km long and 2.8–4.3 km wide, separating the Japan Sea from the brackish lagoon of Nakaumi Bay ( Figs. 1B and 1C ). The Sakai Strait, between the northwestern end of the barrier and the Shimane Peninsula, connects Nakaumi Bay to the Japan Sea. The sandy beach along the barrier is embayed; it is oriented NNW–SSE at its northwestern end and WNW-ESE at its southeastern end. The Hino River flows into the Japan Sea at the southeastern end of the

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Post-IR IRSL dating of K-feldspar from last interglacial marine terrace deposits on the Kamikita coastal plain, northeastern Japan

dosimetry. The remaining sediment was processed to extract coarse grains of K-rich feldspar. The samples were treated with 10% HCl and 10% H 2 O 2 to dissolve carbonate and organic matter, respectively, and then screened using 180 μm and 250 μm mesh sieves. Finally, the K-rich feldspar fraction ( ρ = 2.53–2.58 g/cm 3 ; Aitken, 1998 ) was isolated by using sodium polytungstate. The feldspar grains were then mounted in aliquots with a diameter of 8.0 mm by using silicone oil on stainless steel disks with a diameter of 9.8 mm. Luminescence signals were measured with a

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