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Autochthonous Versus Allochthonous Organic Matter in Recent Soil C Accumulation Along a Floodplain Biogeomorphic Gradient: An Exploratory Study

forest conservation in a regulated large Mediterranean River. River Research and Applications 28, 71-80. DOI: 10.1002/rra.1436 Hughes, F.M.R. 1997. Floodplain biogeomorphology. Progress in Physical Geography 21, 501-529. DOI: 10.1177/030913339702100402 Hupp, C.R. 2000. Hydrology, geomorphology and vegetation of Coastal Plain rivers in the South-eastern USA. Hydrological processes 14, 2991-3010. DOI: 10.1002/1099-1085(200011/12)14:16/17<2991::aid-hyp131>3.0.co;2-h IPCC: Working Group III Report “Mitigation of

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ESR geochronology of the Minjiang River terraces at Wenchuan, eastern margin of Tibetan Plateau, China

and Hutton JT, 1994. Cosmic ray contributions to dose rates for luminescence and ESR dating: Large depths and long-term time variations. Radiation Measurements 23(2–3): 497–500, DOI 10.1016/1350-4487(94)90086-8. http://dx.doi.org/10.1016/1350-4487(94)90086-8 [34] Rink WJ, Bartoll J, Schwarcz HP, Shane P and Ber-Yosef O, 2007. Testing the reliability of ESR dating of optically exposed buried quartz sediments. Radiation Measurements 42(10): 1618–1626, DOI 10.1016/j.radmeas.2007.09.005. http://dx.doi.org/10.1016/j.radmeas.2007

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

of the sediment cores was sub-sampled into 1–3 cm slices. The sub-samples (2–5 g) of the sliced core sections were used for measuring the physical characteristics of the sediment sample, including bulk density, water content and porosity, as described in Saravana Kumar et al ., 1999 . The porosity was calculated from the fluid capacity of the interconnected pores. By dividing the pore volume by the bulk volume, the porosity in percent terms can be determined ( Manger et al ., 1963 ). The remaining quantity of each sub-sample was dried in a drying oven at 75°C

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A 333-year record of the mean minimum temperature reconstruction in the Western Tianshan Mountains, China

diverged ( Zhang et al., 2009 ; Shen et al., 2016 ; Wang et al., 2016 ). However, Picea crassifolia in the northeastern part of the Tibetan Plateau has a relatively stable response to climate ( Zhang and Wilmking, 2010 ). Studies on divergent responses in the Tianshan Mountains are relatively scarce, but Larix sibirica has an unstable response to climate change in the eastern Tianshan Mountains ( Jiao et al., 2015 ). Therefore, whether Schrenk spruce also results from a divergent response in the western Tianshan Mountains remains to be further tested. Because of

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A continuous stable isotope record of last interglacial age from the Bulgarian Cave Orlova Chuka

several requirements. First, speleothem calcite should precipitate under isotopic equilibrium conditions. Hendy tests are the classical tests used to ascertain whether equilibrium conditions were achieved during calcite precipitation ( Hendy and Wilson, 1968 ; Hendy, 1971 ). However, Hendy’s criteria have been revised ( Dorale and Liu 2009 ). The concept of criterion (1) of the Hendy Test, sampling along a single growth layer may be flawed in both theory and practice. But the assumption that growing axis (central part of stalagmite) has higher probability for

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Pleistocene glaciations of the SE Altai, Russia, based on geomorphological data and absolute dating of glacial deposits in Chagan reference section

dating has been demonstrated for various sedimentary environments ( Wagner, 1998 and references therein), mainly focused on those that have experienced sufficient exposure to daylight enabling a complete resetting of the luminescence signal. Luminescence dating of glacial and associated sediments is difficult, mainly due to insufficient bleaching during transportation and deposition of the sediments ( Fuchs and Owen, 2008 and references therein). In addition to the problem of zeroing of the luminescence signal, there is also a great regional diversity in physical

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Assessing the maximum limit of SAR-OSL dating using quartz of different grain sizes

quartz was used (inset to Fig. 3a ). The equivalent data for 63–90 μm grains from M#6# are given in the inset to Fig. 3b . The OSL signal used for analyses was the initial 0 to 0.308 s of the decay curve minus a background from the 1.69–2.30 s interval. LM-OSL signals of 4–11 μm and 63–90 μm grains from sample M#6# were also examined (see Fig. S1 ). Fig. 3 Representative SAR dose response curves and decay curves for fine and coarse quartz. (a) SAR dose response curve for an aliquot of 4–11 μm quartz extracted from sample M#6# and test results. Inset shows a

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Application of long time artificial optical bleaching of the E1’ centre to sediment ESR dating

SiO 2 Physical Review B 27(4): 2285–2293, DOI 10.1103/PhysRevB.27.2285. 10.1103/PhysRevB.27.2285 Jani MG Bossoli RB Halliburton 1983 Further characterization of the E 1 ’ centre in crystalline SiO 2 Physical Review B 27 4 2285 2293 10.1103/PhysRevB.27.2285 Jin SZ, Deng Z and Huang PH, 1991. A response study of E 1 ’ centre of loess quartz to light. Chinese Science Bulletin 36(10): 741–744. (in Chinese) Jin SZ Deng Z Huang PH 1991 A response study of E 1 ’ centre of loess quartz to light Chinese Science

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Koonalda Cave, Nullarbor Plain, South Australia – issues in optical and radiometric dating of deep karst caves

providing reliable dating for Koonalda continues to provide a significant challenge for the interpretation of Aboriginal presence in the site. In turn this has prevented a reliable chronology for the sedimentology, physical formation and palaeoenvironment of the cave ( Jennings, 1961 ; Wright, 1971 and Gillespie, 2002 ). 2 Sampling history Gallus dug three archaeological trenches into the main chamber of the northwest passage between 1960 and 1973 ( Gallus, 1968a ; 1971 and 1973 ). Extensions to the third trench were dug by Richard Wright in 1967 in response

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Meta-analysis of dendrochronological dating of mass movements

.11.017 [26] Decaulne A and Sæmundsson Þ, 2008. Dendrogeomorphology as a tool to unravel snow-avalanche activity: Preliminary results from the Fnjóskadalur test site, Northern Iceland. Norwegian Journal of Geography 62(2): 55–65, DOI 10.1080/00291950802094742. [27] Dorren LKA and Berger F, 2006. Stem breakage of trees and energy dissipation during rockfall impacts. Tree Physiology 26(1): 63–71, DOI 10.1093/treephys/26.1.63. http://dx.doi.org/10.1093/treephys/26.1.63 [28] Dubé S, Filion L and Hétu B, 2004. Tree

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