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  • 1990-1994  (334,892)
  • 1965-1969  (20)
  • 1955-1959  (10)
  • 1940-1944  (3)
  • 1994  (334,892)
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  • 1
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    Unknown
    10Be records of sediment cores from high northern latitudes (1994)
    PANGAEA
    In:  Supplement to: Eisenhauer, Anton; Spielhagen, Robert F; Frank, Martin; Hentzschel, Günter; Mangini, Augusto; Kubik, Peter W; Dittrich-Hannen, Beate; Billen, T (1994): 10Be records of sediment cores from high northern latitudes: Implications for environmental and climatic changes. Earth and Planetary Science Letters, 124(1-4), 171-184, https://doi.org/10.1016/0012-821X(94)00069-7
    Details
    Publication Date: 2024-06-26
    Description: The 10Be records of four sediment cores forming a transect from the Norwegian Sea at 70°N (core 23059) via the Fram Strait (core 23235) to the Arctic Ocean at 86°N (cores 1533 and 1524) were measured at a high depth resolution. Although the material in all the cores was controlled by different sedimentological regimes, the 10Be records of these cores were superimposed by glacial/interglacial changes in the sedimentary environment. Core sections with high 10Be concentrations ( 〉1 * 10**9 at/g) are related to interglacial stages and core sections with low10Be concentrations ( 〈0.5 * 10**9 at/g) are related to glacial stages. Climatic transitions (e.g., Termination II, 5/6) are marked by drastic changes in the 10Be concentrations of up to one order of magnitude. The average 10Be concentrations for each climatic stage show an inverse relationship to their corresponding sedimentation rates, indicating that the 10Be records are the result of dilution with more or less terrigenous ice-rafted material. However, there are strong changes in the 10Be fluxes (e.g., Termination II) into the sediments which may also account for the observed oscillations. Most likely, both processes affected the 10Be records equally, amplifying the contrast between lower (glacials) and higher (interglacials) 10Be concentrations. The sharp contrast of high and low 10Be concentrations at climatic stage boundaries are an independent proxy for climatic and sedimentary change in the Nordic Seas and can be applied for stratigraphic dating (10Be stratigraphy) of sediment cores from the northern North Atlantic and the Arctic Ocean.
    Keywords: Antarctic Ocean; ARK-II/4; ARK-IV/3; AWI_Paleo; Fram Strait; Giant box corer; GIK21524-2 PS11/364-2; GIK21533-3 PS11/412; GIK23059-1; GIK23235-1 PS05/422; GKG; Gravity corer (Kiel type); KAL; Kasten corer; M2/2; Meteor (1986); Norwegian Sea; Paleoenvironmental Reconstructions from Marine Sediments @ AWI; Polarstern; PS05; PS11; PS1235-1; PS1524-2; PS1533-3; Quaternary Environment of the Eurasian North; QUEEN; SL; Svalbard
    Type: Dataset
    Format: application/zip, 4 datasets
    Location Call Number Expected Availability
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  • 2
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    Stable carbon isotope in bottom water and Cibicidoides wuellerstorfi on the Ontong Java Plateau and Emperor Seamount (1994)
    PANGAEA
    In:  Supplement to: McCorkle, Daniel C; Keigwin, Lloyd D (1994): Depth profiles of d13C in bottom water and core top C. wuellerstorfi on the Ontong Java Plateau and Emperor Seamounts. Paleoceanography, 9(2), 197-208, https://doi.org/10.1029/93PA03271
    Details
    Publication Date: 2024-06-26
    Description: We have measured the carbon isotopic composition of dissolved inorganic carbon in bottom waters of the Ontong Java Plateau (western equatorial Pacific) and on the northern Emperor Seamounts (northwest Pacific). Each of these locations is several hundred miles from the nearest Geochemical Ocean Sections Study (GEOSECS) stations, and the observed delta13C values at each site differ substantially from regionally averaged GEOSECS delta13C profiles. We discuss the possible causes of these differences, including horizontal variability, near-bottom effects, and problems with the Pacific GEOSECS delta13C data. We also measured the isotopic composition (C and O) of core top C. wuellerstorfi from a depth transect of cores at each location. The delta18O data are used to verify that our samples are Holocene. Comparison of foraminiferal and bottom water delta13C values shows that this species faithfully records bottom water delta13C at both sites and demonstrates that there is no depth-related artifact in the dissolved inorganic carbon-C. wuellerstorfi delta13C relationship at these sites.
    Keywords: 6-TOW; 6-TOW-001GGC; 6-TOW-002GGC; 6-TOW-003GGC; 6-TOW-005GGC; 6-TOW-006GGC; 6-TOW-007GGC; 6-TOW-008GGC; 6-TOW-011GGC; 6-TOW-011PC; 6-TOW-012GGC; 6-TOW-013GGC; 6-TOW-014GGC; 6-TOW-015GGC; 6-TOW-016GGC; Akademik A. Vinogradov; AVI19-4; BC; Box corer; GGC; Giant gravity corer; Moana Wave; MW9109; MW9109-13BC; MW9109-16BC; MW9109-22BC; MW9109-33BC; MW9109-37BC; MW9109-3BC; MW9109-47BC; MW9109-53BC; MW9109-54BC; MW9109-58BC; MW9109-59BC; MW9109-63BC; MW9109-66BC; MW9109-70BC; MW9109-74BC; MW9109-7BC; Pacific; PC; Piston corer; RAMA; RAMA03WT; RAMA-44P; RNDB-11GGC; RNDB-11PC; RNDB-12GGC; RNDB-13GGC; RNDB-14GGC; RNDB-15GGC; RNDB-16GGC; RNDB-1GGC; RNDB-2GGC; RNDB-3GGC; RNDB-5GGC; RNDB-6GGC; RNDB-7GGC; RNDB-8GGC; Thomas Washington; Vi-26BC; Vi-35GC; Vi-37GC; VINO-26BC; VINO-35GGC; VINO-37GGC
    Type: Dataset
    Format: application/zip, 3 datasets
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  • 3
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    Carbon and Lead chemistry of sediments from the Middle Atlantic Bight (1994)
    PANGAEA
    In:  Supplement to: Anderson, Robert F; Rowe, Gilbert T; Kemp, P F; Trumbore, S; Biscaye, Pierre Eginton (1994): Carbon budget for the mid-slope depocenter of the Middle Atlantic Bight. Deep Sea Research Part II: Topical Studies in Oceanography, 41(2-3), 669-703, https://doi.org/10.1016/0967-0645(94)90040-X
    Details
    Publication Date: 2024-06-26
    Description: A mass budget was constructed for organic carbon on the upper slope of the Middle Atlantic Bight, a region thought to serve as a depocenter for fine-grained material exported from the adjacent shelf. Various components of the budget are internally consistent, and observed differences can be attributed to natural spatial variability or to the different time scales over which measurements were made. The flux of organic carbon to the sediments in the core of the depocenter zone, at a water depth of 1000 m, was measured with sediment traps to be 65 mg C m**-2 day**-1, of which 6-24 mg C m**-2 day**-1 is buried. Oxygen fluxes into the sediments, measured with incubation chambers attached to a free vehicle lander, correspond to total carbon remineralization rates of 49-70 mg C m**-2 day**-1. Carbon remineralization rates estimated from gradients of Corg within the mixed layer, and from gradients of dissolved ammonia and phosphate in pore waters, sum to only 4-6 mg C m**-2 day**-1. Most of the Corg remineralization in slope sediments is mediated by bacteria and takes place within a few mm of the sediment-water interface. Most of the Corg deposited on the upper slope sediments is supplied by lateral transport from other regions, but even if all of this material were derived from the adjacent shelf, it represents 〈2% of the mean annual shelf productivity. This value is further lowered by recognizing that as much as half of the Corg deposited on the slope is refractory, having originated by reworking from older deposits. Refractory Corg arrives at the sea bed with an average 14C age 600-900 years older than the pre-bomb 14C age of DIC in seawater, and has a mean life in the sediments with respect to biological remineralization of at least 1000 years. Labile carbon supplied to the slope, on the other hand, is rapidly and (virtually) completely remineralized, with a mean life of 〈 1 year. Carbon-14 ages of fine-grained carbonate and organic carbon present within the interstices of shelf sands are consistent with this material acting as a source for the old carbon supplied to the slope. Winnowing and export of reworked carbon may contribute to the often-described relationship between organic carbon preservation and accumulation rate of marine sediments.
    Keywords: A_EN179-BC1; A_EN179-BC2; A_EN179-BC3; A_EN179-BC4; A_EN179-BC5; A_EN179-BC7; A_EN187-BC1; A_EN187-BC10; A_EN187-BC11; A_EN187-BC3; A_EN187-BC4; A_EN187-BC5; A_EN187-BC6; A_EN187-BC8; A_EN187-BC9; ADEPD; ADEPDCruises; Atlantic Data Base for Exchange Processes at the Deep Sea Floor; BC; Box corer
    Type: Dataset
    Format: application/zip, 15 datasets
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    DATA PANGAEA
  • 4
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    Respiration and dissolution in sediments of the western Atlantic (1994)
    PANGAEA
    In:  Supplement to: Hales, Burke; Emerson, Steven R; Archer, David E (1994): Respiration and dissolution in the sediments of the western North Atlantic: estimates from models of in situ microelectrode measurements of porewater oxygen and pH. Deep Sea Research Part I: Oceanographic Research Papers, 41(4), 695-719, https://doi.org/10.1016/0967-0637(94)90050-7
    Details
    Publication Date: 2024-06-26
    Description: We present in situ microelectrode measurements of sediment formation factor and porewater oxygen and pH from six stations in the North Atlantic varying in depth from 2159 to 5380 m. A numerical model of the oxygen data indicates that fluxes of oxygen to the sediments are as much as an order of magnitude higher than benthic chamber flux measurements previously reported in the same area. Model results require dissolution driven by metabolic CO2 production within the sediments to explain the pH data; even at the station with the most undersaturated bottom waters 〉60% of the calcite dissolution occurs in response to metabolic CO2. Aragonite dissolution alone cannot provide the observed buffering of porewater pH, even at the shallowest station. A sensitivity test of the model that accounts for uncertainties in the bottom water saturation state and the stoichiometry between oxygen consumption and CO2 production during respiration constrains the dissolution rate constant for calcite to between 3 and 30% day**-1, in agreement with earlier in situ determinations of the rate constant. Model results predict that over 35% of the calcium carbonate rain to these sediments dissolves at all stations, confirmed by sediment trap and CaCO3 accumulation data.
    Keywords: ADEPD; ADEPDCruises; ADEPDCruises_H_11_BOTTLE; ADEPDCruises_H_11_SC; ADEPDCruises_H_5_BOTTLE; ADEPDCruises_H_5_SC; ADEPDCruises_H_6_BOTTLE; ADEPDCruises_H_7_BOTTLE; ADEPDCruises_H_7_SC; ADEPDCruises_H_8_BOTTLE; ADEPDCruises_H_8_SC; ADEPDCruises_H_9_BOTTLE; ADEPDCruises_H_9_SC; Atlantic Data Base for Exchange Processes at the Deep Sea Floor; BC; Bottle, Niskin; Box corer; H_11_BOTTLE; H_11_SC; H_11BC-no3; H_11BC-o2; H_11-me; H_5_BOTTLE; H_5_SC; H_5BC-no3; H_5BC-o2; H_5BC-s; H_5-me; H_6_BOTTLE; H_6BC-no3; H_6BC-o2; H_6BC-s; H_7_BOTTLE; H_7_SC; H_7BC-o2; H_7BC-s; H_7-me; H_8_BOTTLE; H_8_SC; H_8BC-no3; H_8BC-o2; H_8BC-s; H_8-me; H_9_BOTTLE; H_9_SC; H_9BC-no3; H_9BC-o2; H_9BC-s; H_9-me; NIS; SC; Soil combustion
    Type: Dataset
    Format: application/zip, 33 datasets
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  • 5
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    Oxygen isotope composition of planktonic foraminifer Globigerinoides ruber in sediment core GeoB1413 from the eastern edge of the South Atlantic central gyre (1994)
    PANGAEA
    In:  Supplement to: Kemle-von Mücke, Sylvia (1994): Oberflächenwasserstruktur und -zirkulation des Südostatlantiks im Spätquartär. Berichte aus dem Fachbereich Geowissenschaften der Universität Bremen, 55, 151 pp, urn:nbn:de:gbv:46-ep000106720
    Details
    Publication Date: 2024-06-26
    Description: Die Paläozeanographie versucht die Klimageschichte des Quartärs zu rekonstruieren und die Zusammenhänge zwischen Klimaänderungen und ozeanischer Zirkulation besser zu verstehen. Ein wichtiges Hilfsmittel stellen die planktischen Foraminiferen dar. Die Analyse planktischer Foraminiferengemeinschaften hat gezeigt, daß die Verbreitung dieser Protozoa durch die Umweltbedingungen in den Oberflächenwasserströmen bestimmt wird (BoLTOVSKOY, 1969; CIFELLI& BENIER, 1976; OTIENS, 1991). Durch ihre Ablagerung und Erhaltung am Meeresboden speichern sie diese Informationen und bilden einen Indikator für Wassermassen und Oberflächenwassertemperaturschichtung. Zeitliche und räumliche Veränderungen der Faunenvergesellschaftungen und der Verhältnisse stabiler Sauerstoff- und Kohlenstoffisotope einzelner Foraminiferenarten haben damit einen maßgeblichen Beitrag zur Kenntnis der spätquartären Temperatur- und Zirkulationsänderungen der Oberflächenströme geliefert (SHACKLETON & OPDYKE, 1973; BE et al., 1976; RUDDIMAN & McooYRE, 1976; VINCENT & BERGER, 1981; CLIMAP, 1981; RA VELO et al., 1990). Mit Hilfe der planktischen Foraminiferen soll diese Arbeit einen Beitrag zur Rekonstruktion der spätquartären Ozeanographie des Südatlantiks liefern. Die Oberflächenströme des Südatlantiks sind das Bindeglied im Wärmeaustausch zwischen niederen und hohen Breiten. Durch den Südäquatorialstrom (SEC) werden warme Wassermassen, die sich aufgrund der hohen Sonneneinstrahlung im tropischen Atlantik gebildet haben, in den Nordatlantik transportiert. Die Wärme wird im Nordatlantik unter Bildung des Nordatlantischen-Tiefenwassers (NADW) an die Atmosphäre abgegeben. Durch dieses Ereignis wird maßgeblich das nordeuropäische Klima beeinflußt (BROECKER & DENTON, 1989). Die Intensität des SEC wird durch den saisonal variierenden SE-, NE-Passat gesteuert, der hauptsächlich durch die Präzession der geneigten Erdachse bzw. durch die Insolation auf der Nordhalbkugel kontrolliert wird (Mc OOYRE et aI., 1989; MOLFINO & Mc INTYRE, 1990). Der SEC fließt entlang des Äquators von Ost nach West und kalte, nährstotfreiche, tiefere Wassermassen (Südatlantisches-Zentralwasser (SACW)) steigen vor allem im Osten auf und erzeugen das hochproduktive äquatoriale Auftriebsgebiet. Im Osten ist der Temperaturgradient in der Wassersäule steiler, und die Thermoklinentiefe nimmt von Ost nach West zu. Die Lage der Thermokline ist damit ein wesentlicher Faktor, der den Wärmehaushalt im Atlantik mitbestimmt. So wird z. B. im äquatorialen Auftriebsgebiet und im Auftriebsgebiet des küstennahen Benguela-Stroms, wo die Thermoklinentiefe durch aufsteigende kalte Wassermassen gering ist, eine Wärmezunahme von 100 W/qm im Wärmehaushalt erreicht (PETERSON & STRAMMA, 1991). Zur spätquartären Rekonstruktion des Wärmeflusses und der Oberflächenzirkulation im Südostatlantik ist es daher wichtig, auch die zeitlichen und räumlichen Veränderungen tieferer Wasserschichten (bis 300 m) zu erfassen.
    Keywords: AGE; GeoB; GeoB1413-4; Geosciences, University of Bremen; Globigerinoides ruber white, δ18O; Gravity corer (Kiel type); interpolated; M16/1; Meteor (1986); SL; West Angola Basin
    Type: Dataset
    Format: text/tab-separated-values, 444 data points
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  • 6
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    Swath sonar bathymetry during SONNE cruise SO94 with links to multibeam raw data files (1994)
    PANGAEA
    In:  Mineralogisches Institut, TU Bergakademie Freiberg
    Details
    Publication Date: 2024-06-26
    Keywords: CT; DATE/TIME; Depth, bathymetric; EDISON PACIFIC; LATITUDE; LONGITUDE; New-Ireland Fore-Arc, Papua New Guinea; SO94; SO94-track; Sonne; Swath-mapping system Atlas Hydrosweep DS; Underway cruise track measurements; Uniform resource locator/link to file
    Type: Dataset
    Format: text/tab-separated-values, 5858 data points
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  • 7
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    Pb concentrations, Pb isotopic composition, and amount of metalliferous components in pelagic sediments from the Pacific Ocean (1994)
    PANGAEA
    In:  Supplement to: Peucker-Ehrenbrink, Bernhard; Hofmann, Albrecht W; Hart, Stanley R (1994): Hydrothermal lead transfer from mantle to continental crust: the role of metalliferous sediments. Earth and Planetary Science Letters, 125(1-4), 129-142, https://doi.org/10.1016/0012-821X(94)90211-9
    Details
    Publication Date: 2024-06-26
    Description: The amount of lead annually transferred from oceanic crust to metalliferous sediments was estimated in order to test the hypothesis that a non-magmatic flux of lead causes the Pb surplus in the continental crust. A Pb surplus has been inferred from global crust-mantle lead mass balances derived from lead concentration correlations with other trace elements and from lead isotope systematics in oceanic basalts. DSDP/ODP data on the amount of metalliferous sediments in the Pacific Ocean and along a South Atlantic traverse are used to calculate the mean worldwide thickness of 3 (+/-1) m for purely metalliferous sediment componens. Lead isotope ratios of 39 metalliferous sediments from the Pacific define mixing lines between continent-derived (seawater) and mantle-derived (basaltic) lead, with the most metal-rich sediments usually having the most mantle-like Pb isotope composition. We used this isotope correlation and the Pb content of the 39 metalliferous sediments to derive an estimate of 130 (+/-70) µg/g for the concentration of mantle-derived lead in the purely metalliferous end-member. Mass balance calculations show that at least 12 (+/-8)% of the lead, annually transferred from upper mantle to oceanic crust at the ocean ridges, is leached out by hydrothermal processes and re-deposited in marine sediments. If all of the metalliferous lead is ultimately transferred to the continental crust during subduction, the annual flux of this lead from mantle to continental crust is 2.6 (+/-2.0) * 10**6 kg. Assuming this transfer rate to be proportional to the rate of oceanic plate production, one can fit the lead transfer to models of plate production rate variations through time. Integrating over 4 Ga, hydrothermal lead transfer to the continental crust accounts for a significant portion of the Pb surplus in the continental crust. It therefore appears to be one of the main reasons for the anomalous behavior of lead in the global crust-mantle system.
    Keywords: 16-161A; 16-162; 19-183; 34-319; 35-323; 5-37; 5-39; 85-574C; 8-74; 8-75; 91-596; 92-597; 9-77B; Antarctic Ocean/PLAIN; Components indeterminata; Deep Sea Drilling Project; Distance, relative; DRILL; Drilling/drill rig; DSDP; DSDP/ODP/IODP sample designation; Elevation of event; Event label; Glomar Challenger; Latitude of event; Lead; Lead-206/Lead-204 ratio; Lead-207/Lead-204 ratio; Lead-208/Lead-204 ratio; Leg16; Leg19; Leg34; Leg35; Leg5; Leg8; Leg85; Leg9; Leg91; Leg92; Longitude of event; Mass spectrometer Finnigan MAT 251; North Pacific/CONT RISE; North Pacific/HILL; North Pacific/PLAIN; North Pacific/TROUGH; Sample code/label; South Pacific; South Pacific/BASIN; South Pacific/CONT RISE
    Type: Dataset
    Format: text/tab-separated-values, 312 data points
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  • 8
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    Radionuclides in the Weddell Sea (1994)
    PANGAEA
    In:  Supplement to: Rutgers van der Loeff, Michiel M (1994): 228Ra and 228Th in the Weddell Sea. In: Johannessen, O M; Muench, R D & Overland, J E (eds.), The polar oceans and their role in shaping the global environment. Geophysical Monograph Series, American Geophysical Union, 540 pages, ISBN 0-87590-042-9, 85, 177-186
    Details
    Publication Date: 2024-06-26
    Description: 228Ra and its granddaughter 228Th were measured on a N-S transect from 45's to the Antarctic continent across the Antarctic Circumpolar Current (ACC) and the Weddell Sea. The distributions of 230Th, 228Th and 228Ra show that southward transport across the ACC of Circumpolar Deep Water (CDW), the source of Warm Deep Water (WDW) in the Weddell Sea, occurs on a time scale between 8 and 30 years, in qualitative agreement with estimates of the upwelling rate of WDW. The distribution of 228Ra in deep waters is controlled by advection and isopycnal mixing rather than diapycnal mixing. In the Weddell Sea, deep-water 228Ra activities reach 15-20 dpm/m**3. Enrichment in deep water is controlled by the production in the deep-sea floor, favoured by low biogenic sediment accumulation rates and consequently high 232Th contents in the surface sediment (3 to 5 dpm/g). The highest 228Ra value (73 dpm/m**3) was observed near the sea floor in a channel where an eastern outflow of Weddell Sea Bottom Water (WSBW) is suspected. It is not yet known whether this value is produced in-situ by accumulation in the stratified bottom water, or contains a Signal of enrichment in shelf- and Ice Shelf Water. High 228Ra activities on the south-eastem shelf (22 dpm/m**3) and low activities offshore yield an estimated residente time of 1.5 years on this shelf and imply slow exchange with offshore waters.
    Keywords: Agulhas Basin; ANT-IX/3; ANT-VIII/3; ANT-X/6; Atlantic Ridge; AWI_MarGeoChem; AWI_Paleo; DIVERSE; Filchner Trough; Halley Bay; Lazarev Sea; Marine Geochemistry @ AWI; Maud Rise; Meteor Rise; MULT; Multiple investigations; Paleoenvironmental Reconstructions from Marine Sediments @ AWI; Polarstern; PS16; PS16/267; PS16/281; PS16/294; PS16/311; PS16/321; PS16/342; PS16/362; PS16/370; PS1751-8; PS1755-2; PS1759-5; PS1768-2; PS1772-2; PS1777-8; PS1782-7; PS1785-1; PS18; PS18/126; PS18/127; PS18/141; PS18/153; PS18/163; PS18/196; PS18/199; PS18/200; PS18/202; PS18/227; PS1999; PS2011; PS2049; PS2051; PS2052; PS2054; PS2072; PS22; PS22/862; PS22/865; PS22/866; PS22/908; PS22/911; PS22/917; Sampling gear, diverse; Shona Ridge; South Atlantic Ocean; South Sandwich Basin; South Sandwich Trough; Water sample; Weddell Sea; WS
    Type: Dataset
    Format: application/zip, 3 datasets
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  • 9
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    Stable isotope ratios on planktonic foraminifer N. pachyderma of surface sediments from the Arctic Ocean (Table 1) (1994)
    PANGAEA
    In:  Supplement to: Spielhagen, Robert F; Erlenkeuser, Helmut (1994): Stable oxygen and carbon isotopes in planktic foraminifers from Arctic Ocean surface sediments: Reflection of the low salinity surfac water layer. Marine Geology, 119(3-4), 227-250, https://doi.org/10.1016/0025-3227(94)90183-X
    Details
    Publication Date: 2024-06-26
    Description: Planktic foraminifers Neogloboquadrina pachyderma (sin.) from 87 eastern and central Arctic Ocean surface sediment samples were analyzed for stable oxygen and carbon isotope composition. Additional results from 52 stations were taken from the literature. The lateral distribution of delta18O (18O/16O) values in the Arctic Ocean reveals a pattern of roughly parallel, W-E stretching zones in the Eurasian Basin, each ~0.5 per mil wide on the delta18O scale. The low horizontal and vertical temperature variability in the Arctic halocline waters (0-100 m) suggests only little influence of temperature on the oxygen isotope distribution of N. pachyderma (sin.). The zone of maximum delta18O values of up to 3.8 per mil is situated in the southern Nansen Basin and relates to the tongue of saline (〉 33%.) Atlantic waters entering the Arctic Ocean through the Fram Strait. delta18O values decrease both to the Barents Shelf and to the North Pole, in accordance with the decreasing salinities of the halocline waters. In the Nansen Basin, a strong N-S delta18O gradient is in contrast with a relatively low salinity change and suggests contributions from different freshwater sources, i.e. salinity reduction from sea ice meltwater in the south and from light isotope waters (meteoric precipitation and river-runoff) in the northern part of the basin. North of the Gakkel Ridge, delta18O and salinity gradients are in good accordance and suggest less influence of sea ice melting processes. The delta13C (13C/12C) values of N. pachyderma (sin.) from Arctic Ocean surface sediment samples are generally high (0.75-0.95 per mil). Lower values in the southern Eurasian Basin appear to be related to the intrusion of Atlantic waters. The high delta13C values are evidence for well ventilated surface waters. Because the perennial Arctic sea ice cover largely prevents atmosphere-ocean gas exchange, ventilation on the seasonally open shelves must be of major importance. Lack of delta13C gradients along the main routes of the ice drift from the Siberian shelves to the Fram Strait suggests that primary production (i.e. CO2 consumption) does probably not change the CO2 budget of the Arctic Ocean significantly.
    Keywords: 125SGC; 83-101; 83-104; 83-106; 83-109; 83-110; 83-201; 83-202; 83-203; 83-204; 83-205; Alpha Ridge, Arctic Ocean; Amerasian Basin; Amundsen Basin; Antarctic Ocean; Arctic Ocean; ARK-III/3; ARK-IV/3; ARK-IX/4; ARK-VIII/2; ARK-VIII/3; Barents Sea; CESAR; CESAR_83-101; CESAR_83-104; CESAR_83-106; CESAR_83-109; CESAR_83-110; CESAR_83-201; CESAR_83-202; CESAR_83-203; CESAR_83-204; CESAR_83-205; D.St.A.2; DEPTH, sediment/rock; Elevation of event; Event label; FL-433; FL-523; Fram-I; FramI/4; FramI/7; FramII/1; FramII/3; FramII/4; FramII/5; FramIII/1; FramIII/2; FramIII/3; FramIII/7; FramIII/8; FramIV/1; FramIV/7; FramIV/9; Fram Strait; Gakkel Ridge, Arctic Ocean; GC; GEOMAR; Giant box corer; GIK21308-3 PS07/601; GIK21310-4 PS07/603; GIK21312-3 PS07/606; GIK21314-3 PS07/608; GIK21319-2 PS07/617; GIK21513-9 PS11/276-9; GIK21515-10 PS11/280-10; GIK21519-11 PS11/296-11; GIK21520-10 PS11/310-10; GIK21522-19 PS11/358-19; GIK21523-15 PS11/362-15; GIK21524-1 PS11/364-1; GIK21525-2 PS11/365-2; GIK21527-10 PS11/371-10; GIK21528-7 PS11/372-7; GIK21529-7 PS11/376-7; GIK21533-3 PS11/412; GIK21534-6 PS11/423-6; GKG; Gravity corer; Gravity corer (Kiel type); Helmholtz Centre for Ocean Research Kiel; Ice drift station; Laptev Sea; Laptev Sea, Taymyr Island; Latitude of event; Lomonosov Ridge, Arctic Ocean; Longitude of event; LOREX; LOREX1; LOREX10; LOREX11; LOREX2; LOREX3; LOREX6; LOREX8; LOREX9; Makarov Basin; Mass spectrometer Finnigan MAT 251; MIC; MiniCorer; Morris Jesup Rise; MUC; MultiCorer; Nansen Basin; Neogloboquadrina pachyderma sinistral, δ13C; Neogloboquadrina pachyderma sinistral, δ18O; Polarstern; PS07; PS11; PS1308-3; PS1310-4; PS1312-3; PS1314-3; PS1319-2; PS1513-9; PS1515-10; PS1519-11; PS1520-10; PS1522-19; PS1523-15; PS1524-1; PS1525-2; PS1527-10; PS1528-7; PS1529-7; PS1533-3; PS1534-6; PS19/111; PS19/113; PS19/114; PS19/148; PS19/150; PS19/152; PS19/154; PS19/155; PS19/157; PS19/158; PS19/159; PS19/160; PS19/161; PS19/164; PS19/165; PS19/166; PS19/167; PS19/171; PS19/172; PS19/173; PS19/175; PS19/176; PS19/178; PS19/181; PS19/182; PS19/183; PS19/184; PS19/185; PS19/186; PS19/189; PS19/190; PS19/192; PS19/194; PS19/198; PS19/200; PS19/204; PS19/206; PS19/210; PS19/214; PS19/216; PS19/218; PS19/222; PS19/226; PS19/228; PS19/234; PS19/239; PS19/241; PS19/245; PS19/246; PS19/249; PS19 ARCTIC91; PS19 EPOS II; PS2137-1; PS2139-1; PS2140-1; PS2156-1; PS2157-4; PS2159-4; PS2161-4; PS2162-1; PS2163-2; PS2164-4; PS2165-3; PS2166-2; PS2167-2; PS2168-1; PS2170-1; PS2171-1; PS2172-1; PS2174-4; PS2175-3; PS2176-4; PS2177-1; PS2178-2; PS2179-1; PS2180-1; PS2181-1; PS2181-2; PS2182-1; PS2183-1; PS2183-2; PS2184-1; PS2185-1; PS2185-3; PS2186-5; PS2187-1; PS2189-1; PS2190-3; PS2192-1; PS2193-2; PS2194-1; PS2195-4; PS2196-2; PS2198-1; PS2199-4; PS2200-2; PS2202-2; PS2205-3; PS2206-4; PS2208-1; PS2209-1; PS2210-1; PS2212-1; PS2212-5; PS2213-1; PS2214-1; PS2441-3; PS2442-4; PS2443-2; PS2444-1; PS2445-3; PS2446-3; PS2447-4; PS2449-3; PS2455-3; PS2456-2; PS2458-3; PS2459-2; PS2464-2; PS2465-3; PS2466-3; PS2468-3; PS2469-3; PS2470-4; PS2471-3; PS2472-3; PS2473-3; PS2474-2; PS2475-1; PS2476-3; PS2482-3; PS2483-2; PS2484-2; PS27; PS27/007; PS27/014; PS27/016; PS27/017; PS27/019; PS27/020; PS27/024; PS27/027; PS27/033; PS27/034; PS27/038; PS27/039; PS27/046; PS27/047; PS27/048; PS27/050; PS27/052; PS27/053; PS27/054; PS27/056; PS27/058; PS27/059; PS27/060; PS27/062; PS27/069; PS27/070; PS27/071; Quaternary Environment of the Eurasian North; QUEEN; Reference/source; Sampling/drilling from ice; Sampling/drilling ice; SL; Svalbard; T-3; T3-66; T3-67-11; T3-67-5; Y80_125SGC; Yermak Plateau; Ymer; YMER-80
    Type: Dataset
    Format: text/tab-separated-values, 330 data points
    Location Call Number Expected Availability
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  • 10
    facet.materialart.
    Unknown
    Age model of sediment core PS1506-1 (1994)
    PANGAEA
    Details
    Publication Date: 2024-06-26
    Keywords: Age model; ANT-V/4; AWI_Paleo; DEPTH, sediment/rock; Eastern Weddell Sea, Southern Ocean; Gravity corer (Kiel type); Paleoenvironmental Reconstructions from Marine Sediments @ AWI; Polarstern; PS10; PS10/816; PS1506-1; SFB261; SL; South Atlantic in Late Quaternary: Reconstruction of Budget and Currents
    Type: Dataset
    Format: text/tab-separated-values, 28 data points
    Location Call Number Expected Availability
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