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  • 2000-2004  (296,237)
  • 1945-1949  (4)
  • 2001  (296,237)
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  • 1
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    Late Quaternary dinoflagellate cysts at the Eurasian continental margin, Arctic Ocean (2001)
    PANGAEA
    In:  Supplement to: Matthiessen, Jens; Knies, Jochen; Nowaczyk, Norbert R; Stein, Ruediger (2001): Late Quaternary dinoflagellate cyst stratigraphy at the Eurasian continental margin, Arctic Ocean: Indications for Atlantic water inflow in the past 150,000 years. Global and Planetary Change, 31(1-4), 65-86, https://doi.org/10.1016/S0921-8181(01)00113-8
    Details
    Publication Date: 2024-06-26
    Description: Four sediment cores located at the Eurasian continental margin underlying the Atlantic layer have been studied for their dinoflagellate cyst content. Concentrations of distinct dinoflagellate cyst taxa display fluctuations in the late Quaternary, which are linked to changes in the inflow of relatively warm Atlantic surface and near-surface waters, resulting in increased local production of cysts in certain time intervals. Based on the assumption that marked changes in strength of inflow occurred synchronously at the Eurasian continental margin, concentration maxima can be used to correlate sediment cores. A dinoflagellate cyst record from the northern Barents Sea continental margin has been related to the stable oxygen isotope and paleomagnetic records to provide direct chronological information. The combination of these methods permits definition of stratigraphic sections equivalent to oxygen isotope stages in carbonate-poor sequences from the Eurasian continental margin. Previous age models of sediment cores are revised, based on dinoflagellate cyst abundance peaks and species distribution, but a firm chronostratigraphy of sedimentary sequences at the eastern Laptev Sea continental margin cannot be established because of the weak signal at the sites furthest from Fram Strait. In the past 150,000 years, the influence of Atlantic (sub-) surface waters generally decreased from west to east along the Eurasian continental margin, in particular during the glacials. Pronounced concentration maxima of cosmopolitan and temperate-subpolar dinoflagellate cysts indicate the inflow of Atlantic waters and seasonally increased production of cysts in the Holocene and Eemian. The Holocene is well-marked at the entire Eurasian continental margin but it is more difficult to assess the extent of (sub-) surface water inflow during the Eemian, which may have only reached the western Laptev Sea continental margin.
    Keywords: Arctic Ocean; ARK-III/3; ARK-IX/4; ARK-VIII/2; ARK-XI/1; AWI_Paleo; Fram Strait; Giant box corer; GIK21295-4 PS07/586; GKG; Gravity corer (Kiel type); KAL; Kasten corer; Laptev Sea; MUC; MultiCorer; Paleoenvironmental Reconstructions from Marine Sediments @ AWI; Polarstern; PS07; PS1295-4; PS19/112; PS19 EPOS II; PS2138-1; PS2458-4; PS2471-1; PS27; PS27/038; PS27/054; PS2741-1; PS2757-8; PS36; PS36/028; PS36/052; Quaternary Environment of the Eurasian North; QUEEN; SL; Svalbard
    Type: Dataset
    Format: application/zip, 7 datasets
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  • 2
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    Shell preservation of Limacina inflata in surface sediments of the Central and South Atlantic (2001)
    PANGAEA
    In:  Supplement to: Gerhardt, Sabine; Henrich, Rüdiger (2001): Shell preservation of Limacina inflata (Pteropoda) in surface sediments from the Central and South Atlantic Ocean: a new proxy to determine the aragonite saturation state of water masses. Deep Sea Research Part I: Oceanographic Research Papers, 48(9), 2051-2071, https://doi.org/10.1016/S0967-0637(01)00005-X
    Details
    Publication Date: 2024-06-26
    Description: Over 300 surface sediment samples from the Central and South Atlantic Ocean and the Caribbean Sea were investigated for the preservation state of the aragonitic test of Limacina inflata. Results are displayed in spatial distribution maps and are plotted against cross-sections of vertical water mass configurations, illustrating the relationship between preservation state, saturation state of the overlying waters, and overall water mass distribution. The microscopic investigation of L. inflata (adults) yielded the Limacina dissolution index (LDX), and revealed three regional dissolution patterns. In the western Atlantic Ocean, sedimentary preservation states correspond to saturation states in the overlying waters. Poor preservation is found within intermediate water masses of southern origin (i.e. Antarctic intermediate water (AAIW), upper circumpolar water (UCDW)), which are distinctly aragonite-corrosive, whereas good preservation is observed within the surface waters above and within the upper North Atlantic deep water (UNADW) beneath the AAIW. In the eastern Atlantic Ocean, in particular along the African continental margin, the LDX fails in most cases (i.e. less than 10 tests of L. inflata per sample were found). This is most probably due to extensive “metabolic” aragonite dissolution at the sediment-water interface combined with a reduced abundance of L. inflata in the surface waters. In the Caribbean Sea, a more complex preservation pattern is observed because of the interaction between different water masses, which invade the Caribbean basins through several channels, and varying input of bank-derived fine aragonite and magnesian calcite material. The solubility of aragonite increases with increasing pressure, but aragonite dissolution in the sediments does not simply increase with water depth. Worse preservation is found in intermediate water depths following an S-shaped curve. As a result, two aragonite lysoclines are observed, one above the other. In four depth transects, we show that the western Atlantic and Caribbean LDX records resemble surficial calcium carbonate data and delta13C and carbonate ion concentration profiles in the water column. Moreover, preservation of L. inflata within AAIW and UCDW improves significantly to the north, whereas carbonate corrosiveness diminishes due to increased mixing of AAIW and UNADW. The close relationship between LDX values and aragonite contents in the sediments shows much promise for the quantification of the aragonite loss under the influence of different water masses. LDX failure and uncertainties may be attributed to (1) aragonite dissolution due to bottom water corrosiveness, (2) aragonite dissolution due to additional CO2 release into the bottom water by the degradation of organic matter based on an enhanced supply of organic matter into the sediment, (3) variations in the distribution of L. inflata and hence a lack of supply into the sediment, (4) dilution of the sediments and hence a lack of tests of L. inflata, or (5) redeposition of sediment particles.
    Keywords: 06MT15_2; 06MT41_3; A240-ML; Amazon Fan; Angola Basin; Argentine Basin; Ascencion Island; AT_II-107_65; ATII_USA; Atlantic Ocean; Atlantis II (1963); BCR; Box corer (Reineck); Brazil Basin; Cape Basin; Ceara Rise; Continental slope off Brazil; Continental Slope off Rio Paraiba do Sul; East Brazil Basin; eastern Abrolhos Bank; Eastern Rio Grande Rise; Equatorial Atlantic; GeoB1000-1; GeoB1001-1; GeoB1004-2; GeoB1006-2; GeoB1008-6; GeoB1009-3; GeoB1010-3; GeoB1011-2; GeoB1012-1; GeoB1013-2; GeoB1014-2; GeoB1015-2; GeoB1015-3; GeoB1016-2; GeoB1017-3; GeoB1018-2; GeoB1019-2; GeoB1020-1; GeoB1021-3; GeoB1022-3; GeoB1023-2; GeoB1024-3; GeoB1025-2; GeoB1026-3; GeoB1027-2; GeoB1028-2; GeoB1029-1; GeoB1030-3; GeoB1033-3; GeoB1034-1; GeoB1035-2; GeoB1035-3; GeoB1036-3; GeoB1037-1; GeoB1039-1; GeoB1040-3; GeoB1041-1; GeoB1043-2; GeoB1044-3; GeoB1046-2; GeoB1047-3; GeoB1048-2; GeoB1101-4; GeoB1102-3; GeoB1103-3; GeoB1104-5; GeoB1106-5; GeoB1108-6; GeoB1109-4; GeoB1110-3; GeoB1111-5; GeoB1112-3; GeoB1113-7; GeoB1115-4; GeoB1116-1; GeoB1117-3; GeoB1118-2; GeoB1119-2; GeoB1120-3; GeoB1203-2; GeoB1206-1; GeoB1207-2; GeoB1208-1; GeoB1209-1; GeoB1210-3; GeoB1211-1; GeoB1213-2; GeoB1215-1; GeoB1216-2; GeoB1217-1; GeoB1218-1; GeoB1220-2; GeoB1306-1; GeoB1307-2; GeoB1308-1; GeoB1309-3; GeoB1310-1; GeoB1311-2; GeoB1312-1; GeoB1313-1; GeoB1314-2; GeoB1315-2; GeoB1401-1; GeoB1403-2; GeoB1404-8; GeoB1406-1; GeoB1414-2; GeoB1415-1; GeoB1417-2; GeoB1418-1; GeoB1419-1; GeoB1420-1; GeoB1421-1; GeoB1501-1; GeoB1506-1; GeoB1508-1; GeoB1511-6; GeoB1512-1; GeoB1513-2; GeoB1516-1; GeoB1522-1; GeoB1523-2; GeoB1612-9; GeoB1701-2; GeoB1702-7; GeoB1703-3; GeoB1704-1; GeoB1707-2; GeoB1713-6; GeoB1715-1; GeoB1717-2; GeoB1718-1; GeoB1724-4; GeoB1726-1; GeoB1726-2; GeoB1728-3; GeoB1729-1; GeoB1901-1; GeoB1903-3; GeoB1904-1; GeoB1906-1; GeoB1907-1; GeoB2002-2; GeoB2003-1; GeoB2004-1; GeoB2016-3; GeoB2018-1; GeoB2019-2; GeoB2021-4; GeoB2022-3; GeoB2102-1; GeoB2104-1; GeoB2108-1; GeoB2109-3; GeoB2111-2; GeoB2112-1; GeoB2116-2; GeoB2117-4; GeoB2118-1; GeoB2119-1; GeoB2119-2; GeoB2122-1; GeoB2123-1; GeoB2124-1; GeoB2125-2; GeoB2126-1; GeoB2127-1; GeoB2130-1; GeoB2201-1; GeoB2202-4; GeoB2202-5; GeoB2204-1; GeoB2205-4; GeoB2206-1; GeoB2207-2; GeoB2208-1; GeoB2212-1; GeoB2213-1; GeoB2215-8; GeoB2216-2; GeoB2801-1; GeoB2802-2; GeoB2803-1; GeoB2804-2; GeoB2805-1; GeoB2806-6; GeoB2807-1; GeoB2808-3; GeoB2812-3; GeoB2813-1; GeoB2814-3; GeoB2817-3; GeoB2818-1; GeoB2819-2; GeoB2820-1; GeoB2821-2; GeoB2822-3; GeoB2824-1; GeoB2825-3; GeoB2826-1; GeoB2827-2; GeoB2828-1; GeoB2829-3; GeoB2830-1; GeoB2903-1; GeoB2904-11; GeoB2905-1; GeoB2906-3; GeoB2907-1; GeoB2908-8; GeoB2909-1; GeoB2910-2; GeoB2911-2; GeoB3108-4; GeoB3116-1; GeoB3117-3; GeoB3118-1; GeoB3119-1; GeoB3131-2; GeoB3137-1; GeoB3138-2; GeoB3149-2; GeoB3150-1; GeoB3151-2; GeoB3167-1; GeoB3168-1; GeoB3174-1; GeoB3177-2; GeoB3201-2; GeoB3202-2; GeoB3203-3; GeoB3205-1; GeoB3206-2; GeoB3207-2; GeoB3208-2; GeoB3209-2; GeoB3211-1; GeoB3216-1; GeoB3216-2; GeoB3217-1; GeoB3218-1; GeoB3219-1; GeoB3220-2; GeoB3221-1; GeoB3227-1; GeoB3228-2; GeoB3229-1; GeoB3230-4; GeoB3231-2; GeoB3232-3; GeoB3233-1; GeoB3236-2; GeoB3237-1; GeoB3702-2; GeoB3703-4; GeoB3704-2; GeoB3705-2; GeoB3706-3; GeoB3707-3; GeoB3708-1; GeoB3709-1; GeoB3710-1; GeoB3711-1; GeoB3712-1; GeoB3713-1; GeoB3807-1; GeoB3826-2; GeoB3910-3; GeoB3911-1; GeoB3912-1; GeoB3912-2; GeoB4305-1; GeoB4313-1; GeoB4314-2; GeoB4315-1; GeoB4401-3; GeoB4407-2; GeoB4411-1; GeoB4414-2; GeoB4418-2; GeoB4420-1; GeoB4421-2; GeoB5002-1; GeoB5004-2; GeoB5006-1; GeoB5007-1; GeoB5008-3; GeoB5110-5; GeoB5112-5; GeoB5115-2; GeoB5116-1; GeoB5117-2; GeoB5120-1; GeoB5121-2; GeoB5130-1; GeoB5132-2; GeoB5133-3; GeoB5134-1; GeoB5135-1; GeoB5136-2; GeoB5137-1; GeoB5138-2; GeoB5139-1; GeoB5140-3; GeoB5142-2; Giant box corer; GIK17836-1; GIK17851-1; GIK17866-1; GIK17884-1; GKG; Gravity corer (Kiel type); Guayana continental slope; Guinea Basin; Hunter Channel; JOPSII-6; JOPSII-8; Kongo delta; Kongo sediment fan; M12/1; M15/2; M16/1; M16/2; M20/1; M20/2; M23/1; M23/2; M23/3; M29/2; M29/3; M34/2; M34/3; M34/4; M35/1; M35002-1; M35003-6; M35004-1; M35005-3; M35006-6; M35008-1; M35010-2; M35012-6; M35013-3; M35014-1; M35015-1; M35018-1; M35019-1; M35020-2; M35023-3; M35024-6; M35025-1; M35026-2; M35030-1; M35031-2; M35033-1; M35034-3; M35035-1; M35039-1; M35052-5; M35053-3; M35054-1; M38/1; M38/2; M41/2; M41/3; M6/6; M9/4; Meteor (1986); MIC; Midatlantic Ridge; Mid Atlantic Ridge; Mid-Atlantic Ridge; MiniCorer; MUC; MultiCorer; Multiple revolver box corer; Namibia Continental Margin; Namibia continental slope; NE-Brazilian continental margin; Niger Sediment Fan; Northeast Brasilian Margin; Northern Brasil-Basin; Northern Cape Basin; Northern Guinea Basin; Northern Rio Grande Rise; Northwestern Vema Channel; off Kunene; off Macaé; off Rio Doce; off Rio Paraiba do Sul; PC; Piston corer; RC11; RC1112; RC11-21; RC11-26; Rio Grande Rise; RKG; Robert Conrad; Romanche fracture zone; Santos Plateau; SFB261; Sierra Leone Rise; SL; SO84; Sonne; South African margin; South Atlantic in Late Quaternary: Reconstruction of Budget and Currents; south of Abrolhos Bank; South of Cape Verde Islands; ST. HELENA HOTSPOT; Uruguay continental margin; V15; V15-157; V20; V20-227; V20-228; V22; V22-38; V24; V24-237; V24-240; V25; V25-56; V26; V26-63; V26-82; van Veen Grab; Vema; VGRAB; Victor Hensen; Walvis Ridge; West Angola Basin; Western Equatorial Atlantic
    Type: Dataset
    Format: application/zip, 3 datasets
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  • 3
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    Sea-surface temperature reconstruction of the South China Sea (2001)
    PANGAEA
    In:  Supplement to: Kienast, Markus; Steinke, Stephan; Stattegger, Karl; Calvert, Stephen E (2001): Synchronous tropical South China Sea SST change and Greenland warming during deglaciation. Science, 291(5511), 2132-2134, https://doi.org/10.1126/science.1057131
    Details
    Publication Date: 2024-06-26
    Description: The tropical ocean plays a major role in global climate. It is therefore crucial to establish the precise phase between tropical and high-latitude climate variability during past abrupt climate events in order to gain insight into the mechanisms of global climate change. Here we present alkenone sea surface temperature (SST) records from the tropical South China Sea that show an abrupt temperature increase of at least 1°C at the end of the last glacial period. Within the recognized dating uncertainties, this SST increase is synchronous with the Bølling warming observed at 14.6 thousand years ago in the Greenland Ice Sheet Project 2 ice core.
    Keywords: GIK18252-3; GIK18287-3; Gravity corer (Kiel type); SL; SO115; SO115_05; SO115_40; Sonne; SUNDAFLUT; Sunda Shelf; Vietnam shelf
    Type: Dataset
    Format: application/zip, 2 datasets
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  • 4
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    Benthic foraminifera of the Red Sea (2001)
    PANGAEA
    In:  Supplement to: Edelman-Furstenberg, Yael; Scherbacher, Maria; Hemleben, Christoph; Almogi-Labin, Ahuva (2001): Deep-sea benthic foraminifera from the central Red Sea. Journal of Foraminiferal Research, 31(1), 48-59, https://doi.org/10.2113/0310048
    Details
    Publication Date: 2024-06-26
    Description: The distribution of living (Rose Bengal-stained), dead and fossil benthic foraminifera was investigated in six short cores (multicores, 30-32 cm total length) recovered from the central Red Sea. The ecological preferences as well as the relationship between the live and dead/fossil assemblages (preserved down-core) were examined. The sites, located along a W-E profile and between the depth of 366 and 1782 m, extend from the center of the oxygen minimum zone (OMZ, ~200-650 m), through its margin at ~600 m, and down to the well-aerated deep-water environment. Live (Rose-Bengal stained) and coexisting dead foraminifera were studied in the upper 5 cm of each of the sites, and the fossil record was studied down to ~32 cm. Q-mode Principal Component Analysis was used and four distinct foraminiferal fossil assemblages were determined. These assemblages follow different water mass properties. In the center of the OMZ, where the organic carbon content is highest and the oxygen concentration is lowest (〈=0.5 ml O2/l), the Bolivina persiensis-Bulimina marginata-Discorbinella rhodiensis assemblage dominates. The slightly more aerated and lower organic-carbon-content seafloor, at the margin of the OMZ, is characterized by the Neouvigerina porrecta-Gyroidinoides cf. G. soldanii assemblage. The transitional environment, between 900-1200 m, with its well-aerated and oligotrophic seafloor, is dominated by the Neouvigerina ampullacea-Cibicides mabahethi assemblage. The deeper water (〉1500 m), characterized by the most oxygenated and oligotrophic seafloor conditions, is associated with the Astrononion sp. A-Hanzawaia sp. A assemblage. Throughout the Red Sea extremely high values of temperature and salinity are constant below ~200 m depth, but the flux of organic matter to the sea floor varies considerably with bathymetry and appears to be the main controlling factor governing the distribution pattern of the benthic foraminifera. Comparison between live and the dead/fossil assemblages reveals a large difference between the two. Processes that may control this difference include species-specific high turnover rates, and preferential predation and loss of fragile taxa (either by chemical or microbial processes). Significant variations in the degree of loss of the organic-cemented agglutinants were observed down core. This group is preserved down to 5-10 cm at the shallow OMZ sites and down to greater depths at well-aerated and oligotrophic sites. The lower rate of disintegration of these forms, in the deeper locations of the Red Sea, may be related to low microbial activity. This results in the preservation of increasing numbers of organic-cemented shells down-core.
    Keywords: GeoTü; M5/2; M5/2_100MC; M5/2_107MC; M5/2_88MC; M5/2_91MC; M5/2_93MC; M5/2_98MC; Meteor (1986); MUC; MultiCorer; Paleoceanography at Tübingen University
    Type: Dataset
    Format: application/zip, 29 datasets
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  • 5
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    Cycladophora davisiana events in sediments of the subantarctic Atlantic Ocean (2001)
    PANGAEA
    In:  Supplement to: Brathauer, Uta; Abelmann, Andrea; Gersonde, Rainer; Niebler, Hans-Stefan; Fütterer, Dieter K (2001): Calibration of Cycladophora davisiana events versus oxygen isotope stratigraphy in the subantarctic Atlantic Ocean - a stratigraphic tool for carbonate-poor Quaternary sediments. Marine Geology, 175(1-4), 167-181, https://doi.org/10.1016/S0025-3227(01)00141-4
    Details
    Publication Date: 2024-06-26
    Description: We calibrated the Cycladophora davisiana abundances versus oxygen isotope stratigraphy back to 220 ka for the subantarctic Atlantic Ocean. The relative abundances of C. davisiana and delta18O measurements of benthic and planktic foraminifera have been determined in two sediment cores. Oxygen isotope stratigraphy has been used to date the C. davisiana records and to assign SPECMAP ages to the C. davisiana events. Comparisons with an existing calibration from the subantarctic Indian Ocean show, that the C. davisiana events 'b2, c1, c2, d, e1, e2, e3, f, h, i1 and i2' occur synchronous within the errors of the oxygen isotope stratigraphy in the Indian and the Atlantic sectors of the Southern Ocean. Larger deviations occur only for events 'b1' and 'g'. Furthermore, the long-term fluctuations in C. davisiana abundances have been studied in a sediment core covering the last 700 kyr. Based on biostratigraphic extinction levels, ages for early Brunhes C. davisiana events have been estimated. Major C. davisiana abundance maxima occur approximately every 100 ka in conjunction with glacial/interglacial cycles over the entire record.
    Keywords: Agulhas Basin; ANT-IX/4; ANT-VIII/3; ANT-XI/2; AWI_Paleo; Gravity corer (Kiel type); Paleoenvironmental Reconstructions from Marine Sediments @ AWI; Polarstern; PS16; PS16/271; PS1752-1; PS18; PS18/238; PS2082-1; PS2498-1; PS28; PS28/304; SL; South Atlantic
    Type: Dataset
    Format: application/zip, 5 datasets
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  • 6
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    Temperature reconstruction of sediment cores from the northeastern Arabian Sea (2001)
    PANGAEA
    In:  Supplement to: Doose-Rolinski, Heidi; Rogalla, U; Scheeder, Georg; Lückge, Andreas; von Rad, Ulrich (2001): High resolution temperature and evaporation changes during the late Holocene in the northeastern Arabian Sea. Paleoceanography, 16(4), 358-367, https://doi.org/10.1029/2000PA000511
    Details
    Publication Date: 2024-06-26
    Description: In order to reconstruct the monsoonal variability during the late Holocene we investigated a complete, annually laminated sediment record from the oxygen minimum zone (OMZ) off Pakistan for oxygen isotopes of planktic foraminifera and alkenone-derived sea surface temperatures (SST). Significant SST changes of up to 3°C which cannot be explained by changes in the alkenone-producing coccolithophorid species (inferred from the Gephyrocapsa oceanica / Emiliania huxleyi ratio) suggest that SST changes are driven by changes in the monsoon strength. Our high-(decadal)-resolution data indicate that the late Holocene in the northeastern Arabian Sea was not characterized by a stable uniform climate, as inferred from the Greenland ice cores, but by variations in the dominance of the SW monsoon conditions with significant effects on temperatures. Highest SST fluctuations of up to 3.0°C and 2.5°C were observed for the time interval from 4600 to 3300 years B.P. and during the past 500 years. The significant, short-term SST changes during the past 500 years might be related to climatic instabilities known from the northern latitudes ("Little Ice Age") and confirm global effects. Surface salinity values, reconstructed from delta18O records after correction for temperature-related oxygen isotope fractionation, suggest that in general, the past 5000 years were characterized by higher-than-recent evaporation and more intense SW monsoon conditions. However, between 4600 and 3700 years B.P., evaporation dropped, SW monsoon weakened, and NE monsoon conditions were comparatively enhanced. For the past 1500 years we infer strongly fluctuating monsoon conditions. Comparisons of reconstructed salinity records with ice accumulation data from published Tibetan ice core and Tibetan tree ring width data reveal that during the past 2000 years, enhanced evaporation in the northeastern Arabian Sea correlates with periods of increased ice accumulation in Tibet, and vice versa. This suggests a strong climatic relationship between both monsoon-controlled areas.
    Keywords: Arabian Sea; BCR; Box corer (Reineck); KAL; Kasten corer; PAKOMIN; SO90; SO90_39KG; SO90_56KA; Sonne
    Type: Dataset
    Format: application/zip, 4 datasets
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  • 7
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    Sea-surface temperature reconstruction for sediment core GIK18287-3 in the tropical South China Sea (2001)
    PANGAEA
    In:  Supplement to: Steinke, Stephan; Kienast, Markus; Pflaumann, Uwe; Weinelt, Mara; Stattegger, Karl (2001): A High-Resolution Sea-Surface Temperature Record from the Tropical South China Sea (16,500–3000 yr B.P.). Quaternary Research, 55(3), 352-362, https://doi.org/10.1006/qres.2001.2235
    Details
    Publication Date: 2024-06-26
    Description: The timing and magnitude of sea-surface temperature (SST) changes in the tropical southern South China Sea (SCS) during the last 16,500 years have been reconstructed on a high-resolution, 14C-dated sediment core using three different foraminiferal transfer functions (SIMMAX28, RAM, FP-12E) and geochemical (Uk'37) SST estimates. In agreement with CLIMAP reconstructions, both the FP-12E and the Uk'37 SST estimates show an average late glacial-interglacial SST difference of 2.0°C, whereas the RAM and SIMMAX28 foraminiferal transfer functions show only a minor (0.6°C) or no consistent late glacial-interglacial SST change, respectively. Both the Uk'37 and the FP-12E SST estimates, as well as the planktonic foraminiferal delta18O values, indicate an abrupt warming (ca. 1°C in 〈200 yr) at the end of the last glaciation, synchronous (within dating uncertainties) with the Bølling transition as recorded in the Greenland Ice Sheet Project 2 (GISP2) ice core, whereas the RAM-derived deglacial SST increase appears to lag during this event by ca. 500 yr. The similarity in abruptness and timing of the warming associated with the Bølling transition in Greenland and the southern SCS suggest a true synchrony of the Northern Hemisphere warming at the end of the last glaciation. In contrast to the foraminiferal transfer function estimates that do not indicate any consistent cooling associated with the Younger Dryas (YD) climate event in the tropical SCS, the Uk'37 SST estimates show a cooling of ca. 0.2-0.6°C compared to the Bølling-Allerød period. These Uk'37 SST estimates from the southern SCS argue in favor of a Northern Hemisphere-wide, synchronous cooling during the YD period.
    Keywords: GIK/IfG; GIK18287-3; Gravity corer (Kiel type); Institute for Geosciences, Christian Albrechts University, Kiel; SL; SO115; SO115_40; Sonne; SUNDAFLUT; Sunda Shelf
    Type: Dataset
    Format: application/zip, 7 datasets
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  • 8
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    Organic carbon flux and remineralization in surface sediments (2001)
    PANGAEA
    In:  Supplement to: Sauter, Eberhard-Jürgen; Schlüter, Michael; Suess, Erwin (2001): Organic carbon flux and remineralization in surface sediments from the northern North Atlantic derived from pore-water oxygen microprofiles. Deep Sea Research Part I: Oceanographic Research Papers, 48(2), 529-553, https://doi.org/10.1016/S0967-0637(00)00061-3
    Details
    Publication Date: 2024-06-26
    Description: Organic carbon fluxes through the sediment/water interface in the high-latitude North Atlantic were calculated from oxygen microprofiles. A wire-operated in situ oxygen bottom profiler was deployed, and oxygen profiles were also measured onboard (ex situ). Diffusive oxygen fluxes, obtained by fitting exponential functions to the oxygen profiles, were translated into organic carbon fluxes and organic carbon degradation rates. The mean Corg input to the abyssal plain sediments of the Norwegian and Greenland Seas was found to be 1.9 mg C/m**2/d. Typical values at the seasonally ice-covered East Greenland continental margin are between 1.3 and 10.9 mg C/m**2/d (mean 3.7 mg C/m**2/d), whereas fluxes on the East Greenland shelf are considerably higher, 9.1-22.5 mg C/m**2/d. On the Norwegian continental slope Corg fluxes of 3.3-13.9 mg C/m**2/d (mean 6.5 mg C/m**2/d) were found. Fluxes are considerably higher here compared to stations on the East Greenland slope at similar water depths. By repeated occupation of three sites off southern Norway in 1997 the temporal variability of diffusive O2 fluxes was found to be quite low. The seasonal signal of primary and export production from the upper water column appears to be strongly damped at the seafloor. Degradation rates of 0.004-1.1 mg C/cm**3/a at the sediment surface were calculated from the oxygen profiles. First-order degradation constants, obtained from Corg degradation rates and sediment organic carbon content, are in the range 0.03-0.6/a. Thus, the corresponding mean lifetime of organic carbon lies between 1.7 and 33.2 years, which also suggests that seasonal variations in Corg flux are small. The data presented here characterize the Norwegian and Greenland Seas as oligotrophic and relatively low organic carbon deep-sea environments.
    Keywords: 12; 13; 14; 16; 20; 25; 26; 30; ARK-X/1; ARK-XI/2; ARK-XIII/1b; Giant box corer; GKG; Global Environmental Change: The Northern North Atlantic; M36/3; M36/3_201; M36/3_246-2; M36/3_249-2; Meteor (1986); MOOR; Mooring; MUC; MULT; MultiCorer; Multiple investigations; North Greenland Sea; Norwegian continental margin; O2PRO; Oxygen profiler; Polarstern; PS31; PS31/007-4; PS31/014-13; PS31/017-8; PS31/089-5; PS31/092-1; PS37; PS37/012; PS37/013; PS37/014; PS37/016; PS37/020; PS37/025; PS37/026; PS37/030; PS44; PS44/022-4; PS44/023-5; SFB313; SVT12; SVT14; SVT15; SVT8; Voering Plateau; VP6
    Type: Dataset
    Format: application/zip, 2 datasets
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  • 9
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    Age model of sediment core PS1451-1 (2001)
    PANGAEA
    Details
    Publication Date: 2024-06-26
    Keywords: Age, comment; Age model; Age model, paleomagnetic; ANT-IV/4; AWI_Paleo; Gravity corer (Kiel type); Maud Rise; Paleoenvironmental Reconstructions from Marine Sediments @ AWI; Polarstern; PS08; PS08/564; PS1451-1; SL
    Type: Dataset
    Format: text/tab-separated-values, 18 data points
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  • 10
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    Unknown
    Ice rafted debris (〉 2 mm gravel) distribution in sediment core PS2674-1 (2001)
    PANGAEA
    In:  Alfred Wegener Institute, Helmholtz Centre for Polar and Marine Research, Bremerhaven
    Details
    Publication Date: 2024-06-26
    Keywords: ANT-XII/4; AWI_Paleo; DEPTH, sediment/rock; Gravity corer (Kiel type); Ice rafted debris, number of gravel; IRD-Counting (Grobe, 1987); Paleoenvironmental Reconstructions from Marine Sediments @ AWI; Polarstern; PS2674-1; PS35/054; PS35 06AQANTXII_4; SL; Southeast Pacific
    Type: Dataset
    Format: text/tab-separated-values, 680 data points
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