Uk Hwan Byun, A.J. Tom van Loon, Yi Kyun Kwon and Kyoungtae Ko
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Duo Wang, Gong-Ming Yin, Xu-Long Wang, Chun-Ru Liu, Fei Han and Jin-Hua Du
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
Sampling and laboratory procedures
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
Atul K. Singh, Manoj K. Jaiswal, Jitendra K. Pattanaik and Maha Dev
) 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
Fuqiang Li, Baotian Pan, Zhongping Lai, Hongshan Gao and Xianjiao Ou
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
Róbert-Csaba Begy, Szabolcs Kelemen, Hedvig Simon and Claudiu Tănăselia
), 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
Toru Tamura, Kazumi Ito, Takahiko Inoue and Tetsuya Sakai
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
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