Preferential Flow in a Reclamation Cover: Hydrological and Geochemical Response

Kelln, Chris; Barbour, Lee; Qualizza, Clara

doi:10.1061/(asce)1090-0241(2007)133:10(1277)

Cited by 43 publications

(18 citation statements)

References 55 publications

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“…For example, pronounced peaks of a depleted δ 18 O signal in isotope depth profiles were found during snow melt at −1.2 to −1.3 m soil depth by Kelln et al . [] and at −2 to −2.5 m by Peralta‐Tapia et al . [].…”

Section: Processes In the Soilmentioning

confidence: 99%

Illuminating hydrological processes at the soil‐vegetation‐atmosphere interface with water stable isotopes

Sprenger

Leistert

Gimbel

et al. 2016

Reviews of Geophysics

423

382

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Water stable isotopes (18O and 2H) are widely used as ideal tracers to track water through the soil and to separate evaporation from transpiration. Due to the technical developments in the last two decades, soil water stable isotope data have become easier to collect. Thus, the application of isotope methods in soils is growing rapidly. Studies that make use of soil water stable isotopes often have a multidisciplinary character since an interplay of processes that take place in the vadose zone has to be considered. In this review, we provide an overview of the hydrological processes that alter the soil water stable isotopic composition and present studies utilizing pore water stable isotopes. The processes that are discussed include the water input as precipitation or throughfall, the output as evaporation, transpiration, or recharge, and specific flow and transport processes. Based on the review and supported by additional data and modeling results, we pose a different view on the recently proposed two water world hypothesis. As an alternative to two distinct pools of soil water, where one pool is enriched in heavy isotopes and used by the vegetation and the other pool does not undergo isotopic fractionation and becomes recharge, the water gets successively mixed with newly introduced rainwater during the percolation process. This way, water initially isotopically enriched in the topsoil loses the fractionation signal with increasing infiltration depth, leading to unfractionated isotopic signals in the groundwater.

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Section: Processes In the Soilmentioning

confidence: 99%

Illuminating hydrological processes at the soil‐vegetation‐atmosphere interface with water stable isotopes

Sprenger

Leistert

Gimbel

et al. 2016

Reviews of Geophysics

423

382

View full text Add to dashboard Cite

show abstract

“…In general, physical extraction methods are laborious and have the potential for evaporative isotopic fractionation caused by storage, multistep procedures, or by incomplete recovery of the water or evaporative loss during handling. Alternative methods for obtaining pore water isotopes from cores include radial diffusion mass-balance mixing cells (Altinier et al, 2007;Bensenouci et al, 2013;Rubel et al, 2002;Savoye et al, 2006;van der Kamp et al, 1996) or direct equilibration of the pore water in core sub-samples using helium-CO 2 or a He-H 2 catalyst mixtures with headspace gas-water equilibration (Hendry et al, 2004;Kelln et al, 2007;Koehler et al, 2000). Wassenaar et al (2008) proposed a novel method for measuring the δ 2 H and δ 18 O of pore water in saturated and unsaturated geologic (core, soil) samples by using a direct vapour equilibration and laser spectrometry (DVE-LS) approach.…”

Section: Published By Copernicus Publications On Behalf Of the Europementioning

confidence: 99%

Determining the stable isotope composition of pore water from saturated and unsaturated zone core: improvements to the direct vapour equilibration laser spectrometry method

Hendry

Schmeling

Wassenaar

et al. 2015

Hydrol. Earth Syst. Sci.

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Abstract.A method to measure the δ 2 H and δ 18 O composition of pore waters in saturated and unsaturated geologic core samples using direct vapour equilibration and laser spectrometry (DVE-LS) was first described in 2008, and has since been rapidly adopted. Here, we describe a number of important methodological improvements and limitations encountered in routine application of DVE-LS over several years. Generally, good comparative agreement, as well as accuracy, is obtained between core pore water isotopic data obtained using DVE-LS and that measured on water squeezed from the same core. In complex hydrogeologic settings, high-resolution DVE-LS depth profiles provide greater spatial resolution of isotopic profiles compared to long-screened or nested piezometers. When fluid is used during drilling and coring (e.g. water rotary or wet sonic drill methods), spiking the drill fluid with 2 H can be conducted to identify core contamination. DVE-LS analyses yield accurate formational isotopic data for fine-textured core (e.g. clay, shale) samples, but are less effective for cores obtained from saturated permeable (e.g. sand, gravels) geologic media or on chip samples that are easily contaminated by wet rotary drilling fluid. Data obtained from DVE-LS analyses of core samples collected using wet (contamination by drill water) and dry sonic (water loss by heating) methods were also problematic. Accurate DVE-LS results can be obtained on core samples with gravimetric water contents > 5 % by increasing the sample size tested. Inexpensive Ziploc ™ gassampling bags were determined to be as good as, if not better than, other, more expensive specialty bags. Sample storage in sample bags provides acceptable results for up to 10 days of storage; however, measurable water loss, as well as evaporitic isotopic enrichment, occurs for samples stored for up to 6 months. With appropriate care taken during sample collection and storage, the DVE-LS approach for obtaining high-resolution pore water isotopic data is a promising alternative to study the hydrogeology of saturated and unsaturated sediments. Eliminating analytical interferences from volatile organics remains a challenge.

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“…Several experimental case studies showed that event water in hillslope and catchment runoff is a small fraction of the total, even in cases where discharge is expected to be dominated by preferential flow (e.g., McDonnell, 1990;Burns et al, 2001;Kelln et al, 2007). On the contrary, Leaney et al (1993) estimated contribution of the pre-event soil water to stormflow to be less than 20% as event-driven macropore flow carried substantial part of hillslope runoff.…”

Section: Introductionmentioning

confidence: 99%