14.30 An Introduction to Dating Techniques: A Guide for Geomorphologists

Sloss, Craig R.; Westaway, Kira; Hua, Quan; Murray-Wallace, Colin V.

doi:10.1016/b978-0-12-374739-6.00399-7

Cited by 9 publications

(7 citation statements)

References 112 publications

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“…Calibration for marine fossil mollusks collected in this study and from previous research used the marine calibration curve Marine13 (Reimer et al, 2013) with a marine reservoir correction for the southern Gulf of Carpentaria (ΔR = −49 ± 102 yr; Memmott et al, 2016; Ulm, 2006; Ulm et al, 2010) to correct for the marine reservoir effect, and convert ages into sidereal years (expressed as cal. yr BP; Tables 2–5; Gillespie, 1977; Gillespie and Polach, 1979; Stuiver et al, 1998; Sloss et al, 2013; Table 2–5). Age calibration for terrestrial samples was performed using the IntCal13 calibration data (Reimer et al, 2013).…”

Section: Methodsmentioning

confidence: 99%

“…In total, there are 143 previously published radiocarbon (Tables 3 and 4), 15 uranium-thorium (U-Th; Table 2), and 4 thermoluminescence (TL) and optical-stimulated luminescence (OSL ; Table 4) Tables 2-5; Gillespie, 1977;Gillespie and Polach, 1979;Sloss et al, 2013;Table 2-5). Age calibration for terrestrial samples was performed using the IntCal13 calibration data (Reimer et al, 2013).…”

Section: Geochronologymentioning

confidence: 99%

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Holocene sea-level change and coastal landscape evolution in the southern Gulf of Carpentaria, Australia

et al. 2018

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A revised Holocene sea-level history for the southern Gulf of Carpentaria is presented based on new data from the South Wellesley Archipelago and age recalibration of previous research. Results confirm that rising sea levels during the most recent post-glacial marine transgression breached the Arafura Sill ca. 11,700 cal. yr BP. Sea levels continued to rise to ca. -30 m by 10,000 cal. yr BP, leading to full marine conditions. By 7700 cal. yr BP, sea-level reached present mean sea-level (PMSL) and continued to rise to an elevation of between 1.5 m and 2 m above PMSL. Sea level remained ca. + 1.5 between 7000 and 4000 cal. yr BP, followed by rapid regression to within ± 0.5 m of PMSL by ca. 3500 cal. yr BP. When placed into a wider regional context results from this study show that coastal landscape evolution in the tropical north of Australia was not only dependent on sea-level change but also show a direct correlation with Holocene climate variability. Specifically, the formation and preservation of beach-rock deposits, intertidal successions, beach and chenier ridge systems hold valuable sea-level and Holocene climate proxies that can contribute to the growing research into lower latitude Holocene sea-level and climate histories.

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Section: Methodsmentioning

confidence: 99%

Section: Geochronologymentioning

confidence: 99%

Holocene sea-level change and coastal landscape evolution in the southern Gulf of Carpentaria, Australia

et al. 2018

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“…A much older OSL age obtained at the base of Will03 is unreliable (S1 and S2 Figs) due to the very small acceptance rate of grains (9.0%) and therefore was not used to calculate CHAR. This anomalous age could be due to partial bleaching during sediment transport and deposition, which prevents the complete resetting of the luminescence signal and is common in fluvial systems [89, 90]. Since the partial bleaching of grains is common in fluvial systems, the minimum age model (MAM) was applied to all single-grain OSL data to isolate the grains with the smallest residual dose to minimise any age overestimation [78, 79].…”

Section: Discussionmentioning

confidence: 99%

Macro-charcoal accumulation in floodplain wetlands: Problems and prospects for reconstruction of fire regimes and environmental conditions

et al. 2019

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Floodplain wetland ecosystems respond dynamically to flooding, fire and geomorphological processes. We employed a combined geomorphological and environmental proxy approach to assess allochthonous and autochthonous macro-charcoal accumulation in the Macquarie Marshes, Australia, with implications for the reconstruction of fire regimes and environmental conditions in large, open-system wetlands. After accounting for fluvial macro-charcoal flux (1.05 ± 0.32 no. cm-2 a-1), autochthonous macro-charcoal in ~1 m deep sediment profiles spanning ~1.7 ka were highly variable and inconsistent between cores and wetlands (concentrations from 0 to 438 no. cm-3, mean accumulation rates from 0 to 3.86 no. cm-2 a-1). A positive correlation existed between the number of recent fires, satellite-observed ignition points, and macro-charcoal concentrations at the surface of the wetlands. Sedimentology, geochemistry, and carbon stable isotopes (δ13C range -15 to -25 ‰) were similar in all cores from both wetlands and varied little with depth. Application of macro-charcoal and other environmental proxy techniques is inherently difficult in large, dynamic wetland systems due to variations in charcoal sources, sediment and charcoal deposition rates, and taphonomic processes. Major problems facing fire history reconstruction using macro-charcoal records in these wetlands include: (1) spatial and temporal variations in fire activity and ash and charcoal products within the wetlands, (2) variations in allochthonous inputs of charcoal from upstream sources, (3) tendency for geomorphic dynamism to affect flow dispersal and sediment and charcoal accumulation, and (4) propensity for post-depositional modification and/or destruction of macro-charcoal by flooding and taphonomic processes. Recognition of complex fire-climate-hydrology-vegetation interactions is essential. High-resolution, multifaceted approaches with reliable geochronologies are required to assess spatial and temporal patterns of fire and to reconstruct in order to interpret wetland fire regimes.

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“…As bleaching opportunities are more difficult in colluvial environments due to rapid deposition of sediments (Rhodes, 2011; Sloss et al ., 2013; Nelson et al ., 2015), fieldwork campaigns were conducted to identify colluvial deposits that have ideal sampling conditions for OSL dating. Colluvial deposits were scrutinized in the field before selection for OSL sampling.…”

Section: Methodsmentioning

confidence: 99%

Geochronological and paleoenvironmental reconstruction of colluvial deposits in a cuesta landscape in south‐eastern Brazil

Pinton

Lupinacci

2021

J Quaternary Science

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The classic models of cuesta evolution in south‐eastern Brazil have temporal gaps in their denudation chronology. Here, we analyzed the colluvial deposits located on the rim of the Serra Geral escarpments in the Paraná Basin to propose a model with an absolute age range of minor landform evolution within this cuesta morphology. Correlation of the optically stimulated luminescence ages with the regional paleoclimatic conditions demonstrates that the successive phases of colluviation reflect either short‐term intervals of variability in moisture availability or dry periods in the Holocene. The potential effects of other contributing factors (vegetation changes, local geomorphic settings and human activity) add complexity to the denudation responsible for the development of the investigated geomorphic chronosequences. The proposed model consists of five stages of hillslope sediment remobilization that were responsible for further remodeling of the minor vertical steps during the following chronological distribution: (i) 9.13 ± 1.2–7.09 ± 0.96 ka; (ii) 5.66 ± 0.86–4.5 ± 0.75 ka; (iii) 3.94 ± 0.605–3.45 ± 0.6 ka; (iv) 2.66 ± 0.315–2.3 ± 0.4 ka; and (v) after 1960 to the present day.

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14.30 An Introduction to Dating Techniques: A Guide for Geomorphologists

Cited by 9 publications

References 112 publications

Holocene sea-level change and coastal landscape evolution in the southern Gulf of Carpentaria, Australia

Holocene sea-level change and coastal landscape evolution in the southern Gulf of Carpentaria, Australia

Macro-charcoal accumulation in floodplain wetlands: Problems and prospects for reconstruction of fire regimes and environmental conditions

Geochronological and paleoenvironmental reconstruction of colluvial deposits in a cuesta landscape in south‐eastern Brazil

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