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  • PANGAEA  (79)
  • Elsevier  (5)
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  • 1
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    Influence of environmental gradients on C and N stable isotope ratios in coral reef biota of the Red Sea, Saudi Arabia (2014)
    Elsevier
    In:  Journal of Sea Research, 85 . pp. 379-394.
    Details
    Publication Date: 2017-07-19
    Description: The Red Sea features a natural environmental gradient characterized by increasing water temperature, nutrient and chlorophyll a concentrations from North to South. The aim of this study was to assess the relationships between ecohydrography, particulate organic matter (POM) and coral reef biota that are poorly understood by means of carbon (δ13C) and nitrogen (δ15N) stable isotopes. Herbivorous, planktivorous and carnivorous fishes, zooplankton, soft corals (Alcyonidae), and bivalves (Tridacna squamosa)were a priori defined as biota guilds. Environmental samples (nutrients, chlorophyll a), oceanographic data (salinity, temperature), POMand biotawere collected at eight coral reefs between 28°31′ N and 16°31′ N. Isotopic niches of guilds separated in δ13C and δ15N isotopic niche spaces and were significantly correlated with environmental factors at latitudinal scale. Dietary end member contributionswere estimated using the Bayesian isotope mixingmodel SIAR. POMand zooplankton 15N enrichment suggested influences by urban run-off in the industrialized central region of the Red Sea. Both δ15N and their relative trophic positions (RTPs) tend to increase southwards, but urban runoff offsets the natural environmental gradient in the central region of the Red Sea toward higher δ15N and RTPs. The present study reveals that consumer δ13C and δ15N in Red Sea coral reefs are influenced primarily by the latitudinal environmental gradient and localized urban runoff. This study illustrates the importance of ecohydrography when interpreting trophic relationships from stable isotopes in Red Sea coral reefs.
    Type: Article , PeerReviewed
    Format: text
    DOI: 10.1016/j.seares.2013.07.008
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    OceanRep: Article in a Scientific Journal - peer-reviewed
  • 2
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    Relative inputs of upwelled and atmospheric nitrogen to the eastern tropical North Atlantic food web: Spatial distribution of δ15N in mesozooplankton and relation to dissolved nutrient dynamics (2013)
    Elsevier
    In:  Deep Sea Research Part I: Oceanographic Research Papers, 75 . pp. 135-145.
    Details
    Publication Date: 2019-09-23
    Description: The Eastern Tropical North Atlantic (ETNA) is characterised by a strong east to west gradient in the vertical upward flux of dissolved inorganic nitrogen to the photic zone. We measured the stable nitrogen isotope (δ15N) signatures of various zooplankton taxa covering twelve stations in the ETNA (04°–14°N, 016–030°W) in fall 2009, and observed significant differences in δ15N values among stations. These spatial differences in δ15N within zooplankton taxa exceeded those between trophic levels and revealed an increasing atmospheric input of nitrogen by N2 fixation and Aeolian dust in the open ocean as opposed to remineralised NO3− close to the NW African upwelling. In order to investigate the spatial distribution of upwelling-fuelled versus atmospheric-derived nitrogen more closely, we examined the δ15N signatures in size-fractionated zooplankton as well as in three widely distributed epipelagic copepod species on a second cruise in fall 2010 in the ETNA (02-17°35′N, 015–028°W). Copepods were sampled for δ15N and RNA/DNA as a proxy for nutritional condition on 25 stations. At the same stations, vertical profiles of chlorophyll-a and dissolved nutrients were obtained. High standing stocks of chl-a were associated with shallow mixed layer depth and thickening of the nutricline. As the nitracline was generally deeper and less thick than the phosphacline, it appears that non-diazotroph primary production was limited by N rather than P throughout the study area, which is in line with enrichment experiments during these cruises. Estimated by the δ15N in zooplankton, atmospheric sources of new N contributed less than 20% close to the African coast and in the Guinea Dome area and up to 60% at the offshore stations, depending on the depth of the nitracline. δ15N of the three different copepod species investigated strongly correlated with each other, in spite of their distinct feeding ecology, which resulted in different spatial patterns of nutritional condition as indicated by RNA/DNA. Highlights: ► We studied δ15N and RNA/DNA of eastern tropical Atlantic zooplankton along with nutrients and Chl-α. ► Zooplankton −δ15N was decreasing from east (West African Shelf) to west (oligotrophic open ocean). ► Total integrated Chl-a depended mainly on nutricline depth and was N-limited throughout the area. ► Zooplankton δ15N and nutricline depth were used to estimate atmospheric N sources to the food web. ► Estimated atmospheric nitrogen sources were less than 20% at the shelf slope and up to 60% offshore.
    Type: Article , PeerReviewed
    Format: text
    DOI: 10.1016/j.dsr.2013.01.010
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    OceanRep: Article in a Scientific Journal - peer-reviewed
  • 3
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    A paleoclimatic evaluation of marine oxygen isotope stage 11 in the high-northern Atlantic (Nordic seas) (2000)
    Elsevier
    In:  Global and Planetary Change, 24 (1). pp. 27-39.
    Details
    Publication Date: 2017-09-13
    Description: A sediment core from the high latitude of the Northern Atlantic (Nordic seas) was intensively studied by means of biogeochemical, sedimentological, and micropaleontological methods. The proxy records of interglacial marine oxygen isotope stage (MIS) 11 are directly compared with records from the Holocene (MIS 1), revealing that many features of MIS 11 are rather atypical for an interglaciation at these latitudes. Full-interglacial conditions without deposition of ice-rafted debris existed in MIS 11 for about 10 kyr (∼398–408 ka). This time is marked by the lightest d18O values in benthic foraminifera, indicating a small global ice volume, and by the appearance of subpolar planktic foraminifera, indicating a northward advection of Atlantic surface water. A comparison with MIS 1, using the same proxies, implies that surface temperatures were lower and global ice volume was larger during MIS 11. A comparative study of the ratio between planktic and benthic foraminifera also reveals strong differences among the two intervals. These data imply that the coupling between surface and bottom bioproductivity, i.e., the vertical transportation of the amount of fresh organic matter, was different in MIS 11. This is corroborated by a benthic fauna in MIS 11, which contains no epifaunally-living species. Despite comparable values in carbonate content (%), reflectance analyses of the total sediment (greylevel) show much higher values for MIS 11 than for MIS 1. These high values are attributed to increased corrosion of foraminiferal tests, directly affecting the sediment greylevel. The reason for this enhanced carbonate corrosion in MIS 11 remains speculative, but may be linked to the global carbon cycle.
    Type: Article , PeerReviewed
    Format: text
    DOI: 10.1016/S0921-8181(99)00067-3
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    OceanRep: Article in a Scientific Journal - peer-reviewed
  • 4
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    A multiproxy reconstruction of the evolution of deep and surface waters in the subarctic Nordic seas over the last 30,000yr (2001)
    Elsevier
    In:  Quaternary Science Reviews, 20 (4). pp. 659-678.
    Details
    Publication Date: 2019-09-23
    Description: On the basis of various lithological, mircopaleontological and isotopic proxy records covering the last 30,000 calendar years (cal kyr) the paleoenvironmental evolution of the deep and surface water circulation in the subarctic Nordic seas was reconstructed for a climate interval characterized by intensive ice-sheet growth and subsequent decay on the surrounding land masses. The data reveal considerable temporal changes in the type of thermohaline circulation. Open-water convection prevailed in the early record, providing moisture for the Fennoscandian-Barents ice sheets to grow until they reached the shelf break at ∼26 cal. kyr and started to deliver high amounts of ice-rafted debris (IRD) into the ocean via melting icebergs. Low epibenthic δ18O values and small-sized subpolar foraminifera observed after 26 cal. kyr may implicate that advection of Atlantic water into the Nordic seas occurred at the subsurface until 15 cal. kyr. Although modern-like surface and deep-water conditions first developed at ∼13.5 cal. kyr, thermohaline circulation remained unstable, switching between a subsurface and surface advection of Atlantic water until 10 cal. kyr when IRD deposition and major input of meltwater ceased. During this time, two depletions in epibenthic δ13C are recognized just before and after the Younger Dryas indicating a notable reduction in convectional processes. Despite an intermittent cooling at ∼8 cal. kyr, warmest surface conditions existed in the central Nordic seas between 10 and 6 cal. kyr. However, already after 7 cal. kyr the present day situation gradually evolved, verified by a strong water mass exchange with the Arctic Ocean and an intensifying deep convection as well as surface temperature decrease in the central Nordic seas. This process led to the development of the modern distribution of water masses and associated oceanographic fronts after 5 cal. kyr and, eventually, to today's steep east–west surface temperature gradient. The time discrepancy between intensive vertical convection after 5 cal. kyr but warmest surface temperatures already between 10 and 6 cal. kyr strongly implicates that widespread postglacial surface warming in the Nordic seas was not directly linked to the rates in deep-water formation.
    Type: Article , PeerReviewed
    Format: text
    DOI: 10.1016/S0277-3791(00)00098-6
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  • 5
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    Carbon and nitrogen stable isotope ratios of pelagic zooplankton elucidate ecohydrographic features in the oligotrophic Red Sea (2016)
    Elsevier
    In:  Progress in Oceanography, 140 . pp. 69-90.
    Details
    Publication Date: 2019-02-01
    Description: Highlights: • The natural ecohydrographic gradient of the Red Sea translates into an isoscape. • The Red Sea isoscape features increasing zooplankton δ15 N values towards the South. • Isotopic baseline variations propagate through the pelagic food web. • Eddy-induced upwelling modifies the natural ecohydrographic North-South gradient. Abstract: Although zooplankton occupy key roles in aquatic biogeochemical cycles, little is known about the pelagic food web and trophodynamics of zooplankton in the Red Sea. Natural abundance stable isotope analysis (SIA) of carbon (δ13C) and N (δ15N) is one approach to elucidating pelagic food web structures and diet assimilation. Integrating the combined effects of ecological processes and hydrography, ecohydrographic features often translate into geographic patterns in δ13C and δ15N values at the base of food webs. This is due, for example, to divergent 15N abundances in source end-members (deep water sources: high δ15N, diazotrophs: low δ15N). Such patterns in the spatial distributions of stable isotope values were coined isoscapes. Empirical data of atmospheric, oceanographic, and biological processes, which drive the ecohydrographic gradients of the oligotrophic Red Sea, are under-explored and some rather anticipated than proven. Specifically, five processes underpin Red Sea gradients: (a) monsoon-related intrusions of nutrient-rich Indian Ocean water; (b) basin scale thermohaline circulation; (c) mesoscale eddy activity that causes up-welling of deep water nutrients into the upper layer; (d) the biological fixation of atmospheric nitrogen (N2) by diazotrophs; and (e) the deposition of dust and aerosol-derived N. This study assessed relationships between environmental samples (nutrients, chlorophyll a), oceanographic data (temperature, salinity, current velocity [ADCP]), particulate organic matter (POM), and net-phytoplankton, with the δ13C and δ15N values of zooplankton collected in spring 2012 from 16°28′ to 26°57′N along the central axis of the Red Sea. The δ15N of bulk POM and most zooplankton taxa increased from North (Duba) to South (Farasan). The potential contribution of deep water nutrient-fueled phytoplankton, POM, and diazotrophs varied among sites. Estimates suggested higher diazotroph contributions in the North, a greater contribution of POM in the South, and of small phytoplankton in the central Red Sea. Consistent variation across taxonomic and trophic groups at latitudinal scale, corresponding with patterns of nutrient stoichiometry and phytoplankton composition, indicates that the zooplankton ecology in the Red Sea is largely influenced by hydrographic features. It suggests that the primary ecohydrography of the Red Sea is driven not only by the thermohaline circulation, but also by mesoscale activities that transports nutrients to the upper water layers and interact with the general circulation pattern. Ecohydrographic features of the Red Sea, therefore, aid in explaining the observed configuration of its isoscape at the macroecological scale.
    Type: Article , PeerReviewed
    Format: text
    DOI: 10.1016/j.pocean.2015.11.003
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  • 6
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    Stable isotopes of carbon and nitrogene of chitin material of sediment core IOW211660-6 (1999)
    PANGAEA
    Details
    Publication Date: 2023-03-07
    Keywords: Baltic Sea System Study; BASYS; Calculated; Carbon/Nitrogen ratio; Depth, bottom/max; DEPTH, sediment/rock; Depth, top/min; Gotland Basin, Baltic Sea; Gulf of Riga; IOW211660-6; KAL; Kasten corer; KOT99/97/02.1; Petr Kottsov; δ13C, organic carbon; δ15N, organic matter
    Type: Dataset
    Format: text/tab-separated-values, 177 data points
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    DATA PANGAEA
  • 7
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    Carbon nitrogene and stable isotopes of sediment core IOW211660-6 (1999)
    PANGAEA
    Details
    Publication Date: 2023-03-07
    Keywords: Baltic Sea System Study; BASYS; Calculated; Carbon, organic, total; Carbon, total; Carbon/Nitrogen ratio; Depth, bottom/max; DEPTH, sediment/rock; Depth, top/min; Element analyser CHNS-O, Carlo Erba EA1108; Gotland Basin, Baltic Sea; Gulf of Riga; IOW211660-6; Isotope ratio mass spectrometry; KAL; Kasten corer; KOT99/97/02.1; Nitrogen, total; Petr Kottsov; δ13C, organic carbon; δ15N, organic matter
    Type: Dataset
    Format: text/tab-separated-values, 886 data points
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    DATA PANGAEA
  • 8
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    Lignin concentrations and delta13C of organic matter in surface sediments from the Baltic Sea (2022)
    PANGAEA
    Details
    Publication Date: 2023-02-08
    Description: The relative contribution and the composition of terrestrial organic matter were assessed by the analysis of phenolic lignin oxidation products and by the stable isotope composition of organic carbon in surface sediments of the Baltic Sea. For analyses, sub samples of lyophilized, ground and homogenized surface sediment (0-1 cm) material from the collection of surface sediments of the Institut fuer Ostseeforschung Warnemuende were used. Methods Lignin analysis: Between 500 to 2000 mg of dried and homogenised sediment were oxidized at 170°C for 2 h in the presence of 2 mol/L NaOH, CuO, and (NH)4Fe(SO4)2. After centrifugation, the supernatants were acidified to pH 2 with 6 mol/L HCl. The humic acids, which precipitated, were removed by centrifugation. The supernatant was further purified by solid phase extraction. The lignin-derived phenols were sorbed from the acidic solution on C18 material and later eluted with ethyl acetate. The solvent was removed by rotary evaporation, and the phenolic oxidation products were transferred to autosampler vials with methanol that was then removed under a flux of N2. Before analysis by GC/MS, the samples were dissolved in acetonitrile and derivatized with N,O-bis-(trimethylsilyl)trifluoroacetamid (BSTFA) for 1 h at room temperature. Thereafter, they were diluted with acetonitrile according to the expected phenol concentrations. One microliter of each sample was injected in splitless mode, and the phenols were separated in a HP 6890 gas chromatograph equipped with a HP5MS column (30 m x 250 micrometer x 0.25 micrometer). The temperature program of the gas chromatograph was 100°C isothermal for 4 min, ramp to 220°C at 4°C min^-1 with a 5-min isothermal period at 120°C, isothermal at 220°C for 3 min, ramp to 300°C at 30°C min^-1, and final isothermal period for 10 min. The transfer line to the mass spectrometer was kept at 325°C throughout the analysis. The HP 5973 mass spectrometer was operated in the EI mode at 70 eV. The ion source temperature was 230°C, and the quadrupole was kept at 150°C. Compounds were quantified by integration of the base ions and by comparison of the peak areas with those of synthetic standards. Before oxidation, ethylvanillin was added as an internal standard for the determination of recovery. To rule out possible transformations of the internal standard during the oxidation step, blanks containing only ethylvanillin and the reagents were also processed. GC-FID analysis of these blanks displayed a single peak with the retention time of ethylvanillin, and there was no evidence of any transformation of ethylvanillin during the oxidation step under the experimental conditions. The internal standard was added at the beginning of the analysis to ensure that the internal standard and the lignin oxidation products have the same history during the entire analysis. On average, 75% of the added ethylvanillin was recovered after the complete analytical procedure; the range of recoveries was from 50% to 105%. Concentrations and delta13C of total organic carbon Approximately 20 mg of the homogenized sample were weighed into tared sample vessels for elemental composition (total carbon, total nitrogen, organic carbon) and for isotope analyses (delta13C of organic carbon). Total carbon was determined in a Carlo Erba/Fisons 1108 Elemental Analyzer after combustion. A second weighed sample split in tared silver foil vessels was treated with 2N HCl to remove inorganic carbon. On this sub-sample, the concentrations of TOC and isotope ratio delta13C of organic carbon (given in permil versus V-PDB) were determined simultaneously in a Carlo Erba/Fisons 1108 Elemental Analyzer connected to an isotope-ratio mass spectrometer (Finnigan Delta S). The reference gas was pure CO2 from a cylinder calibrated against carbonate (NBS- 18, 19, 20). The standard deviation for replicate analyses of delta13C was less than 0.2 permil. The original data were corrected for the addition of anthropogenic CO2 (Suess effect) by substracting – 1.48 permil from the measured delta13C values of total organic carbon.
    Keywords: 1; 109; 113; 150; 202; 202750; 202820; 202840; 202880; 213; 22; 220000; 220010; 220020; 220030; 220040; 220050; 220300; 220310; 220320; 220500; 220510; 220520; 220580; 220590; 220620; 220630; 220660; 220670; 220720; 220730; 220770; 220780; 220790; 220800; 220810; 220930; 223510; 223520; 223530; 223540; 223550; 223560; 223570; 223580; 223590; 223600; 223610; 223620; 223630; 223640; 223760; 223770; 223780; 223790; 223800; 223810; 223820; 223830; 223840; 223850; 223860; 223870; 223880; 223890; 223900; 223910; 223920; 223930; 223940; 223950; 223960; 223970; 223980; 223990; 224000; 224010; 224020; 224030; 224040; 224050; 224060; 224070; 224080; 224090; 224100; 224110; 224120; 224130; 224140; 224150; 224160; 224170; 224180; 224190; 224200; 271; 286; 30; 33; 360; 40/95/07; 40/98/07; 40/98/14; 40/98/16; 40/98/16_30; 40/98/16_360; 40/98/18; 40/99/11; 40/99/24; 44/95/05; 44/95/05_10; 44/97/07; 46; 99/98/01; Arhus1; Arhus2; Arhus3; Arhus4; Arhus5; Arhus6; Arkona Basin; Arkona Sea; AU_Arhus1; AU_Arhus2; AU_Arhus3; AU_Arhus4; AU_Arhus5; AU_Arhus6; Baltic Sea; Belt Sea; Bornholm Sea; Breitling; Carbon, organic, total; Danish Straits; delta13C of organic carbon; Depth, bottom/max; DEPTH, sediment/rock; Depth, top/min; E10; E12; E2; E3; E7; E9; EB-1; Elevation of event; Event label; F-2; Ferulic acid per unit sediment mass; FIMR_EB-1; FIMR_F-2; FIMR_GF-1; FIMR_SL-2S; FIMR_US-5B; Gda?sk Bay; GF-1; Gotland Sea; Gulf of Bothnia; Gulf of Finland; IOW1; IOW109; IOW113; IOW150; IOW202; IOW202750; IOW202820; IOW202840; IOW202880; IOW213; IOW214280-1; IOW22; IOW220000; IOW220010; IOW220020; IOW220030; IOW220040; IOW220050; IOW220300; IOW220310; IOW220320; IOW220500; IOW220510; IOW220520; IOW220580; IOW220590; IOW220620; IOW220630; IOW220660; IOW220670; IOW220720; IOW220730; IOW220770; IOW220780; IOW220790; IOW220800; IOW220810; IOW220930; IOW223510; IOW223520; IOW223530; IOW223540; IOW223550; IOW223560; IOW223570; IOW223580; IOW223590; IOW223600; IOW223610; IOW223620; IOW223630; IOW223640; IOW223760; IOW223770; IOW223780; IOW223790; IOW223800; IOW223810; IOW223820; IOW223830; IOW223840; IOW223850; IOW223860; IOW223870; IOW223880; IOW223890; IOW223900; IOW223910; IOW223920; IOW223930; IOW223940; IOW223950; IOW223960; IOW223970; IOW223980; IOW223990; IOW224000; IOW224010; IOW224020; IOW224030; IOW224040; IOW224050; IOW224060; IOW224070; IOW224080; IOW224090; IOW224100; IOW224110; IOW224120; IOW224130; IOW224140; IOW224150; IOW224160; IOW224170; IOW224180; IOW224190; IOW224200; IOW271; IOW286; IOW33; IOW46; IOWArkonaBasin; IOWE10; IOWE12; IOWE2; IOWE3; IOWE7; IOWE9; IOWNordperd; IOWODAS; IOWRB1; IOWTromperWiek; Kattegatt; Kleines Haff; Latitude of event; lignin alkaline Cu oxidation; Longitude of event; Nordperd; ODAS; Optional event label; PAP40/98/05; p-Coumaric acid per unit sediment mass; Professor Albrecht Penck; RB1; Skagerrak; SL-2S; Suess corrected; surface sediments; Syringaldehyde per unit sediment mass; Syringic acid per unit sediment mass; Tromper Wiek; US-5B; Vanillic acid per unit sediment mass; Vanillin per unit sediment mass; Vibration corer IOW; VKG; δ13C, total organic carbon
    Type: Dataset
    Format: text/tab-separated-values, 1211 data points
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    DATA PANGAEA
  • 9
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    Stable water isotopes of precipitation and different surface waters in southern Africa, sampled from 2016 to 2021 (2022)
    PANGAEA
    Details
    Publication Date: 2023-02-12
    Description: Water samples of precipitation and different surface waters were collected between 2016 and 2021 in southern Africa using narrow-neck bottles of 300 ml volume. The bottles were stored in a refrigerator until measurements. The stable isotope ratios of oxygen (18O/16O) and hydrogen (2H/1H) of the water samples were measured using a PICARRO L1102-i isotope analyzer (WS-CRDS). Calibration of the measurements was done with VSMOW, SLAP and GISP standards from the IAEA. A total of six replicate injections were performed for each sample and mean and standard deviations (1 sigma) were calculated, resulting in a reproducibility of the replicate measurements of generally better than 0.1 ‰ for oxygen and 0.5 ‰ for hydrogen. The aim of this data collection is to fill a gap in southern Africa, where isotopic data on precipitation and surface waters do not have sufficient spatial coverage and are mainly sampled before 2013. Regional studies of meteorology, hydrology, environmental geochemistry and paleoclimate may benefit from this dataset.
    Keywords: 18K1; 18K10; 18K11; 18K12; 18K13; 18K2; 18K3; 18K4; 18K5; 18K6; 18K7; 18K8; 18K9; 19KHJA1; 19KHJA2; 19KHJA3; 19KHJA4; 19KHS1W; 19KHS2W; 19KHS3W; 19KHS4W; 19KHS5W; 19KHS6W; 19KHW01; 19KHW02; 19KHW03; 19KHW04; 19KHW05; 19KHW06; 19KHW07; 19KHW08; 19KHW09; 19KHW10; 19KHW11; 19KHW12; 19KHW13; 19KHW14; 19KHW15; 19KHW16; 19KHW17; 19KHW18; 19KHW19; 19KHW20; 19KHW21; 19KHW22; 19KHW23; 19KHW24; 19KHW25; 19KHW26; 19KHW27; 19KHW28; 19KHW29; 19KHW30; 19KHW31; 19KHW32; 19KHW33; 19KHW34; 19KHW35; 19KHW36; 19KHW37; 19KHW38; 19KHW39; 19KHW40; 19KHW41; 19KHW42; 19LESSA10W; 19LESSA11W; 19LESSA12W; 19LESSA13W; 19LESSA14W; 19LESSA15W; 19LESSA16W; 19LESSA17W; 19LESSA18W; 19LESSA19W; 19LESSA1W; 19LESSA20W; 19LESSA21W; 19LESSA22W; 19LESSA23W; 19LESSA24W; 19LESSA25W; 19LESSA26W; 19LESSA27W; 19LESSA28W; 19LESSA29W; 19LESSA2W; 19LESSA30W; 19LESSA31W; 19LESSA32W; 19LESSA33W; 19LESSA34W; 19LESSA35W; 19LESSA36W; 19LESSA3W; 19LESSA4W; 19LESSA5W; 19LESSA6W; 19LESSA7W; 19LESSA8W; 19LESSA9W; 20KHW1; 20KHW10; 20KHW11; 20KHW12; 20KHW13; 20KHW14; 20KHW15; 20KHW16; 20KHW17; 20KHW18; 20KHW19; 20KHW2; 20KHW3; 20KHW4; 20KHW5; 20KHW6; 20KHW7; 20KHW8; 20KHW9; 21KHW1; 21KHW10; 21KHW11; 21KHW12; 21KHW13; 21KHW14; 21KHW15; 21KHW16; 21KHW17; 21KHW18; 21KHW19; 21KHW2; 21KHW20; 21KHW21; 21KHW22; 21KHW23; 21KHW24; 21KHW25; 21KHW26; 21KHW27; 21KHW28; 21KHW29; 21KHW3; 21KHW30; 21KHW31; 21KHW32; 21KHW33; 21KHW34; 21KHW35; 21KHW36; 21KHW37; 21KHW38; 21KHW39; 21KHW4; 21KHW5; 21KHW6; 21KHW7; 21KHW8; 21KHW9; ANW1; ANW2; ANW3; ANW4; ANW5; ANW6; ANW7; ANW8; DATE/TIME; DBW1; DBW2; DBW3; DBW4; DBW5; DBW6; Event label; GABORONEW3; GABORONEW5; GABORONEW6; GABORONEW7; GABORONEW8; LATITUDE; LO1; LONGITUDE; MAHALAPYERIVERW4; MOREMIGORGEW1; MOREMIGORGEW2; Picarro L1102-i instrument; Sample comment; Sample ID; Sample type; SLW1; SLW10; SLW11; SLW12; SLW13; SLW14; SLW15; SLW16; SLW17; SLW18; SLW19; SLW2; SLW20; SLW21; SLW22; SLW23; SLW24; SLW25; SLW26; SLW27; SLW28; SLW29; SLW3; SLW30; SLW31; SLW32; SLW33; SLW34; SLW35; SLW36; SLW37A; SLW37B; SLW38; SLW4; SLW5; SLW6; SLW7; SLW8; SLW9; Southern Africa; SSW1; SSW10; SSW11; SSW12; SSW13; SSW14; SSW15; SSW16; SSW17; SSW2; SSW3; SSW4; SSW5; SSW6; SSW7; SSW8; SSW9; stable water isotopes; UW1; UW2; UW3; UW4; UW5; WaterSA_18K1; WaterSA_18K10; WaterSA_18K11; WaterSA_18K12; WaterSA_18K13; WaterSA_18K2; WaterSA_18K3; WaterSA_18K4; WaterSA_18K5; WaterSA_18K6; WaterSA_18K7; WaterSA_18K8; WaterSA_18K9; WaterSA_19KHJA1; WaterSA_19KHJA2; WaterSA_19KHJA3; WaterSA_19KHJA4; WaterSA_19KHS1W; WaterSA_19KHS2W; WaterSA_19KHS3W; WaterSA_19KHS4W; WaterSA_19KHS5W; WaterSA_19KHS6W; WaterSA_19KHW01; WaterSA_19KHW02; WaterSA_19KHW03; WaterSA_19KHW04; WaterSA_19KHW05; WaterSA_19KHW06; WaterSA_19KHW07; WaterSA_19KHW08; WaterSA_19KHW09; WaterSA_19KHW10; WaterSA_19KHW11; WaterSA_19KHW12; WaterSA_19KHW13; WaterSA_19KHW14; WaterSA_19KHW15; WaterSA_19KHW16; WaterSA_19KHW17; WaterSA_19KHW18; WaterSA_19KHW19; WaterSA_19KHW20; WaterSA_19KHW21; WaterSA_19KHW22; WaterSA_19KHW23; WaterSA_19KHW24; WaterSA_19KHW25; WaterSA_19KHW26; WaterSA_19KHW27; WaterSA_19KHW28; WaterSA_19KHW29; WaterSA_19KHW30; WaterSA_19KHW31; WaterSA_19KHW32; WaterSA_19KHW33; WaterSA_19KHW34; WaterSA_19KHW35; WaterSA_19KHW36; WaterSA_19KHW37; WaterSA_19KHW38; WaterSA_19KHW39; WaterSA_19KHW40; WaterSA_19KHW41; WaterSA_19KHW42; WaterSA_19LESSA10W; WaterSA_19LESSA11W; WaterSA_19LESSA12W; WaterSA_19LESSA13W; WaterSA_19LESSA14W; WaterSA_19LESSA15W; WaterSA_19LESSA16W; WaterSA_19LESSA17W; WaterSA_19LESSA18W; WaterSA_19LESSA19W; WaterSA_19LESSA1W; WaterSA_19LESSA20W; WaterSA_19LESSA21W; WaterSA_19LESSA22W; WaterSA_19LESSA23W; WaterSA_19LESSA24W; WaterSA_19LESSA25W; WaterSA_19LESSA26W; WaterSA_19LESSA27W; WaterSA_19LESSA28W; WaterSA_19LESSA29W; WaterSA_19LESSA2W; WaterSA_19LESSA30W; WaterSA_19LESSA31W; WaterSA_19LESSA32W; WaterSA_19LESSA33W; WaterSA_19LESSA34W; WaterSA_19LESSA35W; WaterSA_19LESSA36W; WaterSA_19LESSA3W; WaterSA_19LESSA4W; WaterSA_19LESSA5W; WaterSA_19LESSA6W; WaterSA_19LESSA7W; WaterSA_19LESSA8W; WaterSA_19LESSA9W; WaterSA_20KHW1; WaterSA_20KHW10; WaterSA_20KHW11; WaterSA_20KHW12; WaterSA_20KHW13; WaterSA_20KHW14; WaterSA_20KHW15; WaterSA_20KHW16; WaterSA_20KHW17; WaterSA_20KHW18; WaterSA_20KHW19; WaterSA_20KHW2; WaterSA_20KHW3; WaterSA_20KHW4; WaterSA_20KHW5; WaterSA_20KHW6; WaterSA_20KHW7; WaterSA_20KHW8; WaterSA_20KHW9; WaterSA_21KHW1; WaterSA_21KHW10; WaterSA_21KHW11; WaterSA_21KHW12; WaterSA_21KHW13; WaterSA_21KHW14; WaterSA_21KHW15; WaterSA_21KHW16; WaterSA_21KHW17; WaterSA_21KHW18; WaterSA_21KHW19; WaterSA_21KHW2; WaterSA_21KHW20; WaterSA_21KHW21; WaterSA_21KHW22; WaterSA_21KHW23; WaterSA_21KHW24; WaterSA_21KHW25; WaterSA_21KHW26; WaterSA_21KHW27; WaterSA_21KHW28; WaterSA_21KHW29; WaterSA_21KHW3; WaterSA_21KHW30; WaterSA_21KHW31; WaterSA_21KHW32; WaterSA_21KHW33; WaterSA_21KHW34; WaterSA_21KHW35; WaterSA_21KHW36; WaterSA_21KHW37; WaterSA_21KHW38; WaterSA_21KHW39; WaterSA_21KHW4; WaterSA_21KHW5; WaterSA_21KHW6; WaterSA_21KHW7; WaterSA_21KHW8; WaterSA_21KHW9; WaterSA_ANW1; WaterSA_ANW2; WaterSA_ANW3; WaterSA_ANW4; WaterSA_ANW5; WaterSA_ANW6; WaterSA_ANW7; WaterSA_ANW8; WaterSA_DBW1; WaterSA_DBW2; WaterSA_DBW3; WaterSA_DBW4; WaterSA_DBW5; WaterSA_DBW6; WaterSA_GABORONEW3; WaterSA_GABORONEW5; WaterSA_GABORONEW6; WaterSA_GABORONEW7; WaterSA_GABORONEW8; WaterSA_LO1; WaterSA_MAHALAPYERIVERW4; WaterSA_MOREMIGORGEW1; WaterSA_MOREMIGORGEW2; WaterSA_SLW1; WaterSA_SLW10; WaterSA_SLW11; WaterSA_SLW12; WaterSA_SLW13; WaterSA_SLW14; WaterSA_SLW15; WaterSA_SLW16; WaterSA_SLW17; WaterSA_SLW18; WaterSA_SLW19; WaterSA_SLW2; WaterSA_SLW20; WaterSA_SLW21; WaterSA_SLW22; WaterSA_SLW23; WaterSA_SLW24; WaterSA_SLW25; WaterSA_SLW26; WaterSA_SLW27; WaterSA_SLW28; WaterSA_SLW29; WaterSA_SLW3; WaterSA_SLW30; WaterSA_SLW31; WaterSA_SLW32; WaterSA_SLW33; WaterSA_SLW34; WaterSA_SLW35; WaterSA_SLW36; WaterSA_SLW37A; WaterSA_SLW37B; WaterSA_SLW38; WaterSA_SLW4; WaterSA_SLW5; WaterSA_SLW6; WaterSA_SLW7; WaterSA_SLW8; WaterSA_SLW9; WaterSA_SSW1; WaterSA_SSW10; WaterSA_SSW11; WaterSA_SSW12; WaterSA_SSW13; WaterSA_SSW14; WaterSA_SSW15; WaterSA_SSW16; WaterSA_SSW17; WaterSA_SSW2; WaterSA_SSW3; WaterSA_SSW4; WaterSA_SSW5; WaterSA_SSW6; WaterSA_SSW7; WaterSA_SSW8; WaterSA_SSW9; WaterSA_UW1; WaterSA_UW2; WaterSA_UW3; WaterSA_UW4; WaterSA_UW5; WaterSA_WindhoekRain1a; WaterSA_WindhoekRain1b; Water sample; Water sample, precipitation; WindhoekRain1a; WindhoekRain1b; WS; WSP; δ18O; δ18O, water; δ18O, water, standard deviation; δ2H; δ Deuterium, water; δ Deuterium, water, standard deviation
    Type: Dataset
    Format: text/tab-separated-values, 1715 data points
    Location Call Number Limitation Availability
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    DATA PANGAEA
  • 10
    facet.materialart.
    Unknown
    Age and alkenone-derived Holocene sea-surface temperature records of sediment core IOW225514
    PANGAEA
    In:  Leibniz Institute for Baltic Sea Research, Warnemünde
    Details
    Publication Date: 2023-05-12
    Keywords: 225514; AGE; Calculated from UK'37 (Müller et al, 1998); DEPTH, sediment/rock; GC; Gravity corer; IOW225514; Sea surface temperature, annual mean
    Type: Dataset
    Format: text/tab-separated-values, 84 data points
    Location Call Number Limitation Availability
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    DATA PANGAEA
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