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21 results for “d13C”
Archaeological bitumen from Tell Abraq - GC-MS & d13C data
<p>This dataset belongs to a research that was carried out on bitumen excavated at Tell Abraq, a Bronze Age period site located in the United Arab Emirates.</p> <p>Several bitumen samples from various contexts were sampled and subjected to both GC-MS and Stable Carbon Isotope Analysis. <br> This dataset holds:<br> -Measured d13C values<br> -GC-MS Raw Data (registered by Agilent Software)<br> -Peak surfaces and molecular ratios (both .xlsx and .csv format, both are identical)<br> -Photos linked to the samples</p>
Figure 4. d18O and d13C in A minute ostracod (Crustacea: Cytheromatidae) from the Miocene Solim oes Formation (western Amazonia, Brazil): evidence for marine incursions?
Figure 4. d18O and d13C isotopic ratios of Cyprideis species associated with Pellucistoma curupira sp. nov. Abbreviation: no.s., number of shells used for analysis. Grey shaded polygons display the range of results obtained from fossil and Recent ostracods from the Eiruneṕe region (Gross et al. 2013). (Note: the indicated range for modern rivers and floodplain lakes is based on aragonitic mollusc shells (Wesselingh et al. 2006), which give somewhat heavier values for the same environmental parameters compared to ostracod calcite (Grossman & Ku 1986)).
Mulu Borneo stalagmite SC02 d18O and d13C 19.5-10.7 ky BP
<p>Here are presented Mulu, Borneo (4°6’N, 114°53’E) Secret Cave stalagmite SC02 d18O and d13C values over Termination 1, published in Buckingham et al. (accepted). U-Th ages were calculated using the initial detrital 230Th/232Th value of 111 ± 41 ppm. A Matlab Monte Carlo script was used to calculated the absolute age and age errors associated with each U-Th sample. The Poisson-process deposition model feature in OxCal(v4.4) was used to interpolate between the eighteen U/Th ages to produce an age model. This study reports a d18O and d13C record for the portion of SC02 104.1 to 182.4 mm distance from top of stalagmite. The d18O record spans the full deglaciation, and reveals distinct d18O variations connected with the Bølling-Allerød onset and the Younger Dryas event.</p>
Shihua cave stalagmite CS01C d18O, d13C, lamina thickness, and stalagmite SHD1311 d18O during early Holocene 11.3 - 10 ka BP
<p>Here we present results of <sup>230</sup>Th dating, stable isotope and lamina thickness data from two stalagmites (CS01C and SHD1311) from Shihua Cave (latitude 39´47°N, longitude 115´56°E; altitude 251 m a.s.l. at the entrance), northern China, during 11.32 to 10 ka BP. CS01C developed with clear annual lamina. The age model of CS01C is based on lamina counting. The age model of SHD1311 is established using the COPRA algorithm. The variability of stalagmite δ<sup>18</sup>O records is interpreted as a proxy of regional summer monsoon precipitation and/or EASM intensity. Stalagmite δ<sup>18</sup>O records show two weak summer monsoon events at 10.9 and 10.3 ka. The 10.9-ka event occurred from 10.93–10.79 ka BP for ~140 yr and features a “W”-shaped structure. The 10.3-ka event, also known as the ice-rafted debris event 7 in the North Atlantic, lasted ~260 yr with an asymmetric double-plunging structure.</p>
Tree ring, leaf mining, climate, and remote sensing data from aspen leaf miner survey sites: I - Basal area increment and d13C
This dataset contiains basal area increment (BAI) and d13C chronologies of 47 aspen cored in 2016 across four sites where leaf mining has been documented since 2004. Chronologies of BAI extend as far back as 1957 and up to 2015. Tree ring d13C chronologies extend from 2004-2015 and were measured on 23 trees from two fo the four sites.
Fungal colonization of fine roots and foliar %N, %C, d15N, d13C, and gas exchange of seedlings outplanted at Finger Mountain and the Anaktuvuk River Fire.
This dataset contains proportion of fine root length colonized by root-associated fungi, foliar %N, %C, d15N, d13C, and maximum photosynthesis, respiration, LAI, and CUE for Picea mariana, Picea glauca, Alnus viridis, and Betula neo-alaskana seedlings inoculated with root-associated fungal communities and outplanted at Finger Mountain and the Anaktuvuk River Fire burn scars.
cGENIE Anthropocene d13C excursion
<p>we use the Earth system model cGENIE and calculate the change in carbon isotopic composition of the deep ocean in response to the current anthropogenic perturbation of the global carbon cycle. The three-dimensional cGENIE model simulates ocean, atmosphere and carbon cycle dynamics at low resolution (36 x 36 cells) (Edwards & Marsh, 2005; Ridgwell et al., 2007), which makes it an appropriate tool for resolving first-order questions on the functioning of the Earth's system like the issue at hand here. We perturb cGENIE by introducing isotopically-light CO2 (-28‰ δ13C) into the atmosphere at rates that correspond to IPCC's emission scenario A1B (Nakicenovic et al., 2000). In our simulation, we consider human-induced fluxes of carbon into the atmosphere between 2000 and 2150 AD, with an initial emission of 8.0 Gt C/year in 2000 AD, peak emissions of 16.4 Gt C/year in 2050 AD and zero-emissions from 2150 AD onwards. Starting from a pre-industrial atmospheric CO2 concentration of 278 ppm, this scenario leads to 495 ppm <i>p</i>CO2 in 2050 AD and 810 ppm <i>p</i>CO2 in 2150 AD.</p><p>The cGENIE model experimental setup used for the present study is based on GENIE16 of Archer et al. (2009). This version of cGENIE (Ridgwell & Hargreaves, 2007; Ridgwell et al., 2007) consists of a 3-dimensional C-Goldstein ocean circulation model with reduced physics and 16 depth levels in the ocean. The ocean is coupled to a 2-dimensional energy-moisture balance model of the atmosphere (Edwards & Marsh, 2005; Singarayer et al., 2008) and a 2-dimensional dynamic-thermodynamic sea-ice model (Edwards & Marsh, 2005; Ridgwell et al., 2007). Ocean temperature, salinity and the concentration of biogeochemical tracers, including carbon, are circulated and coupled through the circulation model for the ocean (Ridgwell et al., 2007). This representation of the marine geochemical cycle also accounts for carbonate precipitation and their preservation as deep-sea sediments. We also make use of the sediment diagenesis function of the model, which allows sediments to settle at each ocean grid cell as well as being dissolved during subsequent processes and which was developed by Archer et al. (2009) based on Ridgwell et al. (2007) and Archer (1996). Further details on the cGENIE model setup can be found in Archer et al. (2009) and Singarayer et al. (2008). We applied a 2-part spin-up of modern marine CaCO3 cycling as described in Ridgwell and Hargreaves (2007). In the first stage, we spun up the experiment for 50 kyr in a closed carbon system that is designed to create equilibrium between climate and ocean circulation for a predefined atmospheric CO2 concentration (here: 278 ppm <i>p</i>CO2) and ocean alkalinity. Atmospheric restoring of CO2 and δ13C is included together with carbonate weathering that exactly balances CaCO3 burial in a forced "closed system". In a second spin-up for 200 kyr, the carbonate system is opened to develop freely and includes a temperature-dependent determination of weathering rates. The CO2 emission experiment presented here is based on IPCC's A1B scenario (Nakicenovic et al., 2000). </p><p>Archer, D. (1996). A data-driven model of the global calcite lysocline. <i>Global Biogeochemical Cycles, 10</i>(3), 511-526. 10.1029/96GB01521</p><p>Archer, D., et al. (2009). Atmospheric Lifetime of Fossil Fuel Carbon Dioxide. <i>Annual Review of Earth and Planetary Sciences, 37</i>(1), 117-134. 10.1146/annurev.earth.031208.100206</p><p>Edwards, N. R., & Marsh, R. (2005). Uncertainties due to transport-parameter sensitivity in an efficient 3-D ocean-climate model. <i>Climate Dynamics, 24</i>(4), 415-433. 10.1007/s00382-004-0508-8</p><p>Nakicenovic, N., et al. (2000). <i>Special report on emissions scenarios (SRES), a special report of Working Group III of the intergovernmental panel on climate change</i>: Cambridge University Press.</p><p>Ridgwell, A., & Hargreaves, J. C. (2007). Regulation of atmospheric CO2 by deep-sea sediments in an Earth system model. <i>Global Biogeochemical Cycles, 21</i>(2). 10.1029/2006GB002764</p><p>Ridgwell, A., et al. (2007). Marine geochemical data assimilation in an efficient Earth System Model of global biogeochemical cycling. <i>Biogeosciences, 4</i>(1), 87-104. 10.5194/bg-4-87-2007</p><p>Singarayer, J. S., et al. (2008). An oceanic origin for the increase of atmospheric radiocarbon during the Younger Dryas. <i>Geophysical Research Letters, 35</i>(14). 10.1029/2008GL034074</p>
d13C Added Sugar Intake Biomarker: Determining Validity in Children
ClinicalTrials.gov study NCT02455388. IPD Sharing: Not stated. Countries: 1. Publications: 2.
Feather nitrogen and carbon stable isotope (d15N and d13C) values for Golden-crowned Sparrows
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Amino acid d13C dataset for nearshore marine primary producers
<p>Carbon isotope fingerprinting, or multivariate analysis using <em>δ</em><sup>13</sup>C values of individual compounds, is a powerful tool in ecological studies, particularly measurements of essential amino acids (EAA <em>δ</em><sup>13</sup>C). Despite the widespread application of this technique, there has been little methodological validation to determine (1) whether multivariate EAA <em>δ</em><sup>13</sup>C signatures (fingerprints) of primary producer groups vary across space and time, and (2) what biochemical mechanisms drive these patterns.</p> <p>Here, we evaluate the spatiotemporal consistency in EAA <em>δ</em><sup>13</sup>C fingerprints among nearshore primary producers: Chlorophyta (<em>Ulva</em> sp.), Ochrophyta (kelps), particulate organic matter (POM) and phytoplankton, and Rhodophyta. We analyzed 135 samples from 14 genera collected in Alaska, California, and Chile. The collections included historical museum samples (1896-1980 CE) of the giant kelp, <em>Macrocystis pyrifera</em>. We employed canonical analysis of principal coordinates and generalized linear models (GLMs) to respectively characterize isotopic fingerprints and evaluate the effect of taxonomy, local upwelling regimes, ecological setting, and time on individual EAA <em>δ</em><sup>13</sup>C values and associated fingerprints. We also calculated amino acid discrimination values (<em>D</em><sup>13</sup>C) to identify key biochemical pathways responsible for these patterns.</p> <p>We found remarkable consistency in EAA <em>δ</em><sup>13</sup>C fingerprints of marine algae across space and through time. Kelps and rhodophytes exhibited statistically distinct multivariate isotopic patterns regardless of geographic location, species identity, or time (kelps). In contrast, isotopic fingerprints of POM/phytoplankton and <em>Ulva</em> overlapped substantially. GLMs indicated that producer family, presumably due to the presence/absence of carbon concentrating mechanisms, and site locality are important determinants of individual amino acid <em>δ</em><sup>13</sup>C values. Taxonomy was also a key variable for EAA <em>δ</em><sup>13</sup>C fingerprints. The calculated discrimination values suggest variation in (1) metabolism of pyruvate and oxaloacetate-derived amino acids, and (2) production of storage and structural carbohydrates, are responsible for taxonomic differences in isotopic fingerprints. </p> <p>We conclude EAA <em>δ</em><sup>13</sup>C fingerprinting is a robust method for tracing the contribution of diverse primary producer taxa to coastal food webs. We show that this technique can be applied to modern and historical samples, as well as consumers collected across continental scales. The high fidelity of EAA <em>δ</em><sup>13</sup>C multivariate patterns coupled with biochemical mechanisms provides a powerful framework for future studies of carbon flow across broad biogeographical and ecological contexts.</p>
Assessment of compound-specific fatty acid d13C and d2H values to track fish residency and mobility in a small subalpine catchment
<p><span>Methods for identifying origin, movement, and foraging areas of animals are essential for understanding ecosystem connectivity, nutrient flows, and other ecological processes. Telemetric methods can provide detailed spatial coverage but are limited to minimum body size of specimen for tagging. In recent years, stable isotopes have been increasingly used to track animal migration by linking geophysical isotope landscapes called "isoscapes". However, compared to telemetric methods, the spatial resolution of bulk stable isotopes is low.</span></p> <p><span>Here we examined a novel approach by evaluating the use of compound-specific hydrogen and carbon stable isotopes of fatty acids (δ</span><sup><span>2</span></sup><span>H<sub>FA</sub> and </span><span>δ<sup>13</sup></span><span>C<sub>FA</sub>) from liver, muscle, brain, and eye tissues for identifying site-specificity of fish from a sub-alpine river catchment. We analysed 208 fish (European bullhead, rainbow trout, and brown trout) collected in 2016 and 2018 at 15 different sites.</span></p> <p><span>δ<sup>13</sup></span><span>C<sub>FA</sub> values of these fish tissues correlated more amongst each other than those of </span><span><span>δ</span><sup><span>2</span></sup><span>H<sub>FA</sub></span> values. Both </span><span><span>δ</span><sup><span>2</span></sup><span>H<sub>FA</sub></span> and </span><span><span>δ<sup>13</sup></span><span>C<sub>FA</sub></span> values showed tissue-dependent isotopic fractionation, while fish taxa had only small effects. The highest site-specificity was for </span><span>δ<sup>13</sup></span><span>C<sub>DHA</sub> values, while the </span><span>δ<sup>2</sup></span><span>H isotopic difference between LIN and ALA resulted in the highest site-specificity. Using linear discrimination analysis of FA isotope values, over 90 % of fish could be assigned to their location of origin, however, the accuracy dropped to about 56 % when isotope data from 2016 were used to predict the sites for samples collected in 2018, suggesting temporal shifts in site specificity of </span><span><span>δ</span><sup><span>2</span></sup><span>H<sub>FA</sub></span> and </span><span>d</span><span>13</span><span>CFA. However, predictive results were still higher than site specificity compared to bulk tissue isotopes for a single time point. In summary, compound-specific isotope analysis of fatty acids may become a highly effective tool for assessing fine and large-scale movement and foraging areas of animals.</span></p>
d13C and d15N of Pacific halibut skeletal muscle tissue from the Gulf of Alaska, 2018
<p>In 2018, white muscle samples were collected from the lateral musculature of a random sample of up to 4 fish from each survey station of the International Pacific Halibut Commission's Fishery Independent Setline Survey (total n = 1653). Muscle samples were stored at -20°C, thawed, oven-dried to a constant mass at 42°C, and ground to a fine powder. Approximately 0.5 to 1.0 mg of each powdered sample was loaded into a tin capsule for stable isotope analysis. d<sup>13</sup>C and d<sup>15</sup>N values were determined using a Carlo Erba 1110 Elemental Analyzer (Carlo Erba Reagents, CE Instruments, ThermoQuest Italia S.p.A. Milan, Italy) coupled to a Thermo Delta Plus XP IRMS (Thermo Finnigan, Bremen, German) at the University of Wyoming's Stable Isotope Facility (Laramie, Wyoming, USA). Long-term analyses of quality control standards have yielded precisions of 0.3‰ for d<sup>13</sup>C and 0.4‰ for d<sup>15</sup>N. Stable isotope data are presented in ‰ relative to Pee Dee Belemnite for <sup>13</sup>C and atmospheric nitrogen for <sup>15</sup>N.</p>
14C, d13C and d15N for bones from the Femern project
<p>This file contains basic information (species, 14C age, d13C and d15N) for animal bones analysed in the Femern project, as well as average d13C values for wood samples.</p> <p>This is supplementary data for Philippsen, B. (2023) Changing diet in a changing world. In: Groß, D. and Rothstein, M. (eds) Changing Identities in a Changing World.</p>
d13C and d15N of Pacific halibut skeletal muscle tissue from the Gulf of Alaska, 2018
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Assessment of compound-specific fatty acid d13C and d2H values to track fish residency and mobility in a small subalpine catchment
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Amino acid d13C dataset for nearshore marine primary producers
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Wyoming hummingbird breath d13C
<p>Here, we present data from two experiments conducted n the Rocky Mountains of Wyoming, USA to assess the relative use of feeder and flower nectar by Broad-tailed and Rufous hummingbirds using two distinct methods to measure the δ<sup>13</sup>C values of exhaled CO<sub>2</sub> – manual sample collection (2010) and automated analysis (2018). </p>
Wyoming hummingbird breath d13C
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Future Changes in d13C of Dissolved Inorganic Carbon in the Ocean
<p>This repository contains model simulation output (DIC and DI<sup>13</sup>C) for various SSP scenarios described in the paper "Future Changes in δ<sup>13</sup>C of Dissolved Inorganic Carbon in the Ocean" by Graven et al., <em>Earth's Future</em> (2021).</p>
Mg/Ca and Stable isotopes (d18O and d13C) measured on G. bulloides and G. inflata of sediment core PS75/056-1
<p>Geochemical measurements of G. bulloides and G. inflata from core PS75/056-1</p>
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