Lipid biomarkers and carbon-isotopes of modern travertine deposits (Yellowstone National Park, USA): Implications for biogeochemical dynamics in hot-spring systems

Zhang, Chuanlun L.; Fouke, Bruce W.; Bonheyo, George T.; Peacock, Aaron D.; White, David C.; Huang, Yongsong; Romanek, Christopher S.

doi:10.1016/j.gca.2004.03.005

Cited by 63 publications

(32 citation statements)

References 79 publications

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“…Nitrogen isotopic values of biofilms are driven by several factors, depending upon the source of nitrogen, and whether there is nitrogen limitation or N 2 fixation. Changes can be dramatic as documented by Estep [1984] and Estep and Macko [1984], which are summarized in Figure 1 along with other carbon and nitrogen isotopic data from more recent literature sources [ van der Meer et al , 2000a; Jahnke et al , 2001; van der Meer et al , 2003; Zhang et al , 2004; van der Meer et al , 2005; van der Meer et al , 2007]. The data in Figure 1 show the fractionation of carbon isotopes and the nitrogen isotopic composition plotted against temperature for biofilms collected from hot springs in Yellowstone National Park.…”

Section: Introductionmentioning

confidence: 88%

Merging isotopes and community genomics in a siliceous sinter-depositing hot spring

et al. 2011

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[1] Thermophilic microbes in hydrothermal ecosystems have multiple metabolic strategies for taking up carbon and nitrogen, which may result in distinct stable isotopic compositions of C and N in living biomass, as well as other biosignatures that accumulate in the geologic record. Biofilms from "Bison Pool" at Yellowstone National Park display large variations in carbon and nitrogen isotopic values as a function of downstream sampling and illustrate the presence of large shifts in ecological functions as temperature decreases. This is the first study to couple isotopic data with community genomic analysis to predict dominant carbon fixation pathways that create hydrothermal biofilm signatures. The results also suggest nitrogen limitation through the chemotrophic zone and nitrogen fixation in the lower-temperature phototrophic zone.

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Section: Introductionmentioning

confidence: 88%

Merging isotopes and community genomics in a siliceous sinter-depositing hot spring

et al. 2011

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“…We assume sediment CH4 is primarily oxidized during AOM for energy and DIC is assimilated into cellular biomass [11][12][13] with an isotopic fraction of 3.75‰ , a value recently applied in a study on the Hikurangi Margin [37] and an intermediate (2.0‰ to 5.5‰) for isotopic fractionation during DIC assimilation in the reversed tricarboxylic acid cycle [63][64][65]. For estimating the DIC contribution to SOC during AOM it is assumed δ 13 CPD end-member (Equation (5) Figure 8).…”

Section: Estimation Of Ch4 Contribution To the Shallow Organic Carbonmentioning

confidence: 99%

Deep Sediment-Sourced Methane Contribution to Shallow Sediment Organic Carbon: Atwater Valley, Texas-Louisiana Shelf, Gulf of Mexico

et al. 2015

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Coastal methane hydrate deposits are globally abundant. There is a need to understand the deep sediment sourced methane energy contribution to shallow sediment carbon relative to terrestrial sources and phytoplankton. Shallow sediment and porewater samples were collected from Atwater Valley, Texas-Louisiana Shelf, Gulf of Mexico near a seafloor mound feature identified in geophysical surveys as an elevated bottom seismic reflection. Geochemical data revealed off-mound methane diffusion and active fluid advection on-mound. Gas composition (average methane/ethane ratio ~11,000) and isotope ratios of methane on the mound (average δ CSOC = −629‰) suggest deep sourced ancient carbon is incorporated into shallow sediment organic matter. Porewater and sediment data indicate inorganic carbon fixed during anaerobic oxidation of methane is a dominant contributor to on-mound shallow sediment organic carbon cycling. A simple stable carbon isotope mass balance suggests carbon fixation of dissolved inorganic carbon (DIC) associated with anaerobic oxidation of hydrate-sourced CH4 contributes up to 85% of shallow sediment organic carbon.

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“…Regarding SOC, a 13 C isotopic fractionation of −3.75‰ during CO 2 fixation was assumed, a midpoint for the 2.0‰ to 5.5‰ range expected for the reversed tricarboxylic acid cycle (rTCA) [70][71][72]. This assumption is based on extensive data gathered for rTCA in laboratory and field research where bacterial biomass results in δ 13 C values to be −2.0‰ to −12.0‰ depleted relative to the substrate through a temperature range of 30-100 °C and varying growth conditions [70][71][72][73][74]. Characterization of the microbial community diversity in sediments supports the assumption that the primary CO 2 fixation cycle is rTCA [75,76].…”

Section: Methane Contribution To Shallow Sediment Carbon Poolsmentioning

confidence: 99%

Contribution of Vertical Methane Flux to Shallow Sediment Carbon Pools across Porangahau Ridge, New Zealand

et al. 2014

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Moderate elevated vertical methane (CH 4 ) flux is associated with sediment accretion and raised fluid expulsion at the Hikurangi subduction margin, located along the northeast coast of New Zealand. This focused CH 4 flux contributes to the cycling of inorganic and organic carbon in solid phase sediment and pore water. Along a 7 km offshore transect across the Porangahau Ridge, vertical CH 4 flux rates range from 11.4 mmol·m −2 ·a −1 off the ridge to 82.6 mmol·m −2 ·a −1 at the ridge base. Stable carbon isotope ratios (δ 13 C) in pore water and sediment were variable across the ridge suggesting close proximity of heterogeneous OPEN ACCESSEnergies 2014, 7 5333 carbon sources. Methane stable carbon isotope ratios ranging from −107.9‰ to −60.5‰ and a C1:C2 of 3000 indicate a microbial, or biogenic, source. Near ridge, average δ 13 C for pore water and sediment inorganic carbon were 13 C-depleted (−28.7‰ and −7.9‰, respectively) relative to all core subsamples (−19.9‰ and −2.4‰, respectively) suggesting localized anaerobic CH 4 oxidation and precipitation of authigenic carbonates. Through the transect there was low contribution from anaerobic oxidation of CH 4 to organic carbon pools; for all cores δ 13 C values of pore water dissolved organic carbon and sediment organic carbon averaged −24.4‰ and −22.1‰, respectively. Anaerobic oxidation of CH 4 contributed to pore water and sediment organic carbon near the ridge as evidenced by carbon isotope values as low as to −42.8‰ and −24.7‰, respectively. Carbon concentration and isotope analyses distinguished contributions from CH 4 and phytodetrital carbon sources across the ridge and show a low methane contribution to organic carbon.

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Lipid biomarkers and carbon-isotopes of modern travertine deposits (Yellowstone National Park, USA): Implications for biogeochemical dynamics in hot-spring systems

Cited by 63 publications

References 79 publications

Merging isotopes and community genomics in a siliceous sinter-depositing hot spring

Merging isotopes and community genomics in a siliceous sinter-depositing hot spring

Deep Sediment-Sourced Methane Contribution to Shallow Sediment Organic Carbon: Atwater Valley, Texas-Louisiana Shelf, Gulf of Mexico

Contribution of Vertical Methane Flux to Shallow Sediment Carbon Pools across Porangahau Ridge, New Zealand

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