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14 results for “d18O”
Stable oxygen isotope ratios of water (H2O-d18O) from river, lagoon, and open ocean sites along the Alaska Beaufort Sea coast, 2019-ongoing
Multiple water types (river, lagoon, ocean) from the North Slope of Alaska and nearshore Beaufort Sea are sampled seasonally by the Beaufort Lagoon Ecosystems LTER (BLE LTER) Core Program to investigate biogeochemical linkages between terrestrial, lagoon, and open ocean ecosystems. Water samples are collected during full ice cover (April), ice break-up (mid-June to early July), and open water (late July and August) periods, and analyzed for delta 18O (ratio of oxygen-18 to oxygen-16) to use in mixing models for source water contribution.
Time series of stable water isotopes (d18O, d2H) from Carvins Cove Reservoir in Southwestern Virginia, USA 2024-2025
Samples of stable water isotopes (delta 18O and delta 2H) were collected from surface waters and depth profiles in Carvins Cove Reservoir (Roanoke, Virginia, USA). Carvins Cove Reservoir is owned operated by the Western Virginia Water Authority as a primary drinking water source for Roanoke, Virginia. Samples were collected approximately monthly at two sites along a primary tributary and depth profiles at multiple transects within Carvins Cove Reservoir from May 2024 - April 2025. Additional isotope samples were analyzed from precipitation collected at the Carvins Cove Reservoir dam in 2024. Samples were analyzed using cavity ringdown spectroscopy and reported as deviation of concentration from that of Vienna standard mean ocean water. An Rmarkdown file to visualize the dataset accompanies the package.
2707 water samples from Vallon de Nant analyzed for stable water isotopes (dD, d17O, d18O) and electric conductivity
<p>Database gathering 2707 water samples from the Vallon de Nant (Westerm Swiss Alps) analyzed for stable isotopes of water (dD, d17O, d18O, d-excess, LC-excess, 17O-excess) and electric conductivity.</p> <p>The "VDN_database.csv" file includes the following columns:<br> - time [dd/mm/yyyy HH:MM, UTC]<br> - latitude [decimal degrees, WGS84]<br> - longitude [decimal degrees, WGS84]<br> - elevation [masl]<br> - point: point name<br> - dD [‰]<br> - d17O [‰]<br> - d18O [‰]<br> - d-excess [‰]<br> - LC-excess [‰]<br> - 17O-excess [per meg]<br> - conductivity [µS/cm]</p> <p>Water is sampled from:<br> - 2 points of main stream (Avançon de Nant) at HyS1 and HyS2<br> - 5 different springs at GRAS, AUBG, ROCK, BRDG and ICEC<br> - 3 piezometers at PZ1, PZ2 and PZ3<br> - 2 weather stations for rain at Auberge and Chalet<br> - various locations (GPS points) for the Snowpack<br> - various locations (GPS points) for the Glacier</p> <p>The points with regular sampling are shown on the map "VDN_sampling_points.png".</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>
Benthic d18O records Earth's energy imbalance
<p>Data include previously published data that were used to produce reconstructions of global energy anomalies and Earth's energy imbalance, as well as the aforementioned reconstructions. Previously published data include 1) a global reconstruction of benthic d18O for the last 150,000 years, 2) ice core noble gas - based reconstructions of mean ocean temperature and the atmospheric noble gas ratios used for these reconstructions for the last 25,000 years, and 3) two eustatic sea level reconstructions from coral and tidal indicators combined with glacio-isostatic adjustment models for the last 25,000 years. From these previously published data we derive 1) the estimated contributions of temperature (or the equilibrium isotope effect) and ice volume (or d18O of seawater) to the total benthic d18O signal, 2) reconstructions of global energy change, and 3) reconstructions of Earth's energy imbalance.</p>
North Atlantic benthic d18O stack data
<p>Files containing the data for our speleothem-tied North Atlantic benthic d18O stack, including: ages, d18O values, d18O err, age samples output by BIGMACS, and the composite depth scale used for this stack (based on IODP site U1308).</p> <p>Please read for information on what each file contains:<br>'NA-stack_age-samples.txt' = 1000 sets of age model samples generated during stack construction, each column contains a unique age model.</p> <p>'NA-stack_age-d18O.txt' = the median age model output by BIGMACS after stack construction with their corresponding d18O data points (this age model closely aligns with that of the LR04 stack since the LR04 stack was used as our initial alignment target).</p> <p>'NA-stack_depth_composite.txt' = the composite depths used to reduce bias in our stack's age model.</p> <p>'NA-stack_untuned_age_model.txt' = the stack ages after mapping them onto the composite depth scale of Site U1308. This is the data plotted in Fig. 3 of the paper. This file was added on February 3, 2025 to allow users to download this data directly without having to apply the extra step of interpolating the median age model onto the depth scale themselves.</p>
Stable isotope composition (d18O) of seawater from stations in the Palmer LTER Study Site
The west Antarctic Peninsula (WAP) is a region of marked climatic variability, exhibiting strong changes in sea ice extent, retreat of the majority of its glaciers, and shifts in the amount and form of precipitation. These changes can have significant impacts on the oceanic freshwater budget and marine biogeochemical processes; it is thus important to ascertain the relative balance of the drivers, and the spatial scales over which they operate. We present a new 7-year summer-season (October to March; 2011 to 2018) series of oxygen isotopes in seawater (δ18O), augmented with some winter sampling, collected adjacent to Anvers Island at the WAP. These data are used to attribute oceanic freshwater changes to sea ice and meteoric sources, and to deduce information on the spatial scales over which the changes are driven. Sea ice melt shows strong seasonality (~9% range) and marked interannual changes, with pronounced maxima in seasons 2013/14 and 2016/17. Both of these extrema are driven by anomalous winds, but reflect strongly contrasting dynamic and thermodynamic sea ice responses. Meteoric water also shows marked seasonality (~7% range), with interannual variability reflecting changes in the input of accumulated precipitation and glacial melt to the ocean. Unlike sea ice melt, meteoric water extremes are especially pronounced in thin (<10m) surface layers close to Marr Ice Piedmont, associated with enhanced ocean stratification. Isotopic tracers help to deconvolve the complex spatio-temporal scales inherent in the coastal freshwater budget, and hence improve knowledge of the separate and cumulative physical and ecological impacts.
Supplementary dataset for the paper "A time window averaging method to mitigate the impact of shell growth trends on Tridacna d18O records".
<p>Data and code for the paper "A time window averaging method to mitigate the impact of shell growth trends on Tridacna δ18O records". We have included an example in the pseudo-Tridacna package v2.1 to demonstrate how users can generate pseudo-Tridacna series.</p>
Sources of oceanic freshwater content along the western Antarctic Peninsula (PAL-LTER Study Region) determined by the stable isotope composition (d18O) of seawater.
The oceanic distribution of d18O is determined largely by the same processes that control salinity. Surface d18O reflects the magnitude and spatial distribution of freshwater inputs, and it is a conservative tracer in the ocean interior. The great benefit of d18O is obtained from the circumstances under which it exhibits behavior different to that of salinity. One such circumstance derives from the salinity and d18O values in precipitation, with salinity being constant with latitude (typically zero), while in general d18O in precipitation becomes progressively isotopically lighter toward the poles. This results in glacial ice (which derives from high-latitude precipitation) being very isotopically light, enabling d18O to be a useful tracer of glacial discharge to the ocean (e.g., Schlosser et al. 1990; Weiss et al. 1979). Another difference occurs in regions influenced by sea ice, which greatly affects salinity during its formation/melt cycle but has only minimal impact on d18O. This decoupling of the two tracers allows them to be used in tandem to quantitatively separate freshwater inputs from sea ice melt and those from meteoric sources (precipitation plus glacial discharge). For this, a simple three-endmember mass balance can be used. For details please see Meredith, M. P., H. J. Venables, A. Clarke, H. W. Ducklow, M. Erickson, M. J. Leng, J. T. M. Lenaerts, and M. R. van den Broeke. 2013. The freshwater system west of the Antarctic Peninsula: Spatial and temporal changes. Journal of Climate 26:1669-1684.
Water tagging experiments for the interpretation of Asian speleothem d18O
<p>These simulation results are from the water-tagging experiments in the paper "Deciphering Oxygen Isotope Records From Chinese Speleothems With an Isotope‐Enabled Climate Model" published on Paleoceanography and Paleoclimatology (<a href="https://agupubs.onlinelibrary.wiley.com/doi/full/10.1029/2019PA003741">https://agupubs.onlinelibrary.wiley.com/doi/full/10.1029/2019PA003741</a>). Readme.txt provides detailed descriptions of variables in all NetCDF files, and tagging_region_names.pdf shows the abbreviations of all tagging region names. </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>
Plio-Pleistocene benthic d18O, d13C and sand-accumulation rates for Site 849
<p>Plio-Pleistocene benthic d18O, d13C and sand-accumulation rates for Site 849</p>
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