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  • 1995-1999  (7,819)
  • 1955-1959  (52)
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  • 1
    Publication Date: 2024-06-25
    Description: During METEOR cruise 34/4 the recovered gravity cores were subject to laboratory geophysical studies. A routine shipboard measurement of three physical parameters was carried out on the segmented sediment cores, comprising the determination of: - the compressional (P- ) wave velocity vp, - the electric resistivity Rs, and - the magnetic volume susceptibility K. These propelties are closely related to the grain size, porosity and lithology of the sediments and provide high-resolution core logs (spacing 1 cm for P-wave velocity and magnetic volume susceptibility, 2 cm for electric resistivity) available prior to all other detailed investigations. In addition, oriented samples for later shore based paleo- and rockmagnetic studies were taken at intervals of 10 cm.
    Keywords: Amazon Shelf/Fan; Atlantic Caribbean Margin; GeoB; GeoB3909-2; GeoB3910-2; GeoB3911-3; GeoB3912-1; GeoB3913-3; GeoB3914-2; GeoB3915-2; GeoB3916-2; GeoB3918-4; GeoB3920-2; GeoB3935-2; GeoB3936-1; GeoB3937-2; GeoB3938-1; GeoB3939-2; Geosciences, University of Bremen; Gravity corer (Kiel type); M34/4; Meteor (1986); Northeast Brasilian Margin; SL
    Type: Dataset
    Format: application/zip, 54 datasets
    Location Call Number Expected Availability
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  • 2
    facet.materialart.
    Unknown
    PANGAEA
    In:  Supplement to: Schlünz, Birger; Schneider, Ralph R; Müller, Peter J; Showers, William J; Wefer, Gerold (1999): Terrestrial organic carbon accumulation on the Amazon deep sea fan during the last glacial sea-level low stand. Chemical Geology, 159(1-4), 263-281, https://doi.org/10.1016/S0009-2541(99)00041-8
    Publication Date: 2024-06-25
    Description: Sediment cores from the Amazon deep sea fan recovered during R/V Meteor cruise 16-2 show in detail the modern areal distribution of sedimentary organic carbon, stable organic carbon isotopes of the organic matter (OM), as well as variations in the depositional processes. In addition, we studied up to 300 m long drilled sediment records recovered during ODP Leg 155 which allow evaluation of temporal variations on the Amazon fan. Our results reveal new evidence for a very rapid change of fan depositional processes and organic carbon source at times of sea-level change over the middle and lower Amazon fan. To estimate the amount of terrestrial organic carbon stored in sediments from the last glacial in the Amazon fan we used stable organic carbon isotopes of the OM (delta13Corg), organic carbon content (Corg), and age models based on oxygen isotopes, faunal data, and magnetic excursions. Following our results, the organic carbon accumulation on the Amazon deep sea fan is controlled by glacio-eustatic sea-level oscillations. Interglacial sea-level high stand sediments are dominated by marine OM whereas during glacial sea-level low stands terrestrial organic carbon is transported beyond the continental shelf through the Amazon canyon and deposited directly onto the Amazon deep sea fan. Glacial sediments of the Amazon fan stored approximately 73*10**15 g terrestrial Corg in 20,000 years or 3.7*10**12 g terrestrial Corg/yr (equivalent to 7-12% of the riverine organic carbon discharge; assuming constant paleo discharge), which is about the same amount of terrestrial organic carbon as deposited on the Amazon shelf today (3.1*10**12 g terrestrial Corg/yr or 6-10% of the modern riverine organic carbon discharge).
    Keywords: Amazon Fan; GeoB1511-5; GeoB1512-3; GeoB1513-1; GeoB1514-7; Gravity corer (Kiel type); M16/2; Meteor (1986); SFB261; SL; South Atlantic in Late Quaternary: Reconstruction of Budget and Currents
    Type: Dataset
    Format: application/zip, 4 datasets
    Location Call Number Expected Availability
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  • 3
    facet.materialart.
    Unknown
    PANGAEA
    In:  Supplement to: Diekmann, Bernhard; Kuhn, Gerhard (1999): Provenance and dispersal of glacial-marine surface sediments in the Weddell Sea and adjoining areas, Antarctica: ice-rafting versus current transport. Marine Geology, 158(1-4), 209-231, https://doi.org/10.1016/S0025-3227(98)00165-0
    Publication Date: 2024-06-25
    Description: Mineralogical and granulometric properties of glacial-marine surface sediments of the Weddell Sea and adjoining areas were studied in order to decipher spatial variations of provenance and transport paths of terrigenous detritus from Antarctic sources. The silt fraction shows marked spatial differences in quartz contents. In the sand fractions heavy-mineral assemblages display low mineralogical maturity and are dominated by garnet, green hornblende, and various types of clinopyroxene. Cluster analysis yields distinct heavy-mineral assemblages, which can be attributed to specific source rocks of the Antarctic hinterland. The configuration of modern mineralogical provinces in the near-shore regions reflects the geological variety of the adjacent hinterland. In the distal parts of the study area, sand-sized heavy minerals are good tracers of ice-rafting. Granulometric characteristics and the distribution of heavy-mineral provinces reflect maxima of relative and absolute accumulation of ice-rafted detritus in accordance with major iceberg drift tracks in the course of the Weddell Gyre. Fine-grained and coarse-grained sediment fractions may have different origins. In the central Weddell Sea, coarse ice-rafted detritus basically derives from East Antarctic sources, while the fine-fraction is discharged from weak permanent bottom currents and/or episodic turbidity currents and shows affinities to southern Weddell Sea sources. Winnowing of quartz-rich sediments through intense bottom water formation in the southern Weddell Sea provides muddy suspensions enriched in quartz. The influence of quartz-rich suspensions moving within the Weddell Gyre contour current can be traced as far as the continental slope in the northwestern Weddell Sea. In general, the focusing of mud by currents significantly exceeds the relative and absolute contribution of ice-rafted detritus beyond the shelves of the study area.
    Keywords: Adelaide Island; Antarctic Peninsula; ANTARTIDA8611; ANT-I/2; ANT-II/3; ANT-II/4; ANT-III/3; ANT-IV/2; ANT-IV/3; ANT-IV/4; ANT-IX/2; ANT-IX/3; ANT-V/4; ANT-VI/2; ANT-VI/3; ANT-VIII/5; ANT-VIII/6; ANT-X/2; ANT-X/4; ANT-X/5; ANT-X/6; ANT-XI/2; ANT-XI/4; ANT-XIV/3; Anvers Island; Argentine Islands; Astrid Ridge; Atka Bay; AWI_Paleo; Barents Sea; BC; Box corer; Bransfield Strait; Camp Norway; Cape Fiske; Cosmonauts Sea; CTD/Rosette; CTD-RO; D-EL-1; D-ORC-011; D-ORC-013; D-ORC-015; D-ORC-017; D-ORC-023; D-ORC-024; D-ORC-025; D-ORC-142; D-PA-1; Drake Passage; Dredge; DRG; D-ST-2; D-ST-3; D-ST-4; Eastern Weddell Sea, Southern Ocean; EL-443; EL-444; EL-445; EL-446; EL-447; EL-448; EL-449; Filchner Shelf; Filchner Trough; Fram Strait; Giant box corer; GKG; Gould Bay; Gravity corer (Kiel type); Greenland Slope; GS-053; GS-076; GS-152; Halley Bay; Hope Bay; Islas Orcadas; Kapp Norvegia; King George Island, Antarctic Peninsula; KL; Lazarev Sea; Lyddan Island; Maud Rise; MG; MIC; MiniCorer; MUC; Multiboxcorer; MultiCorer; Nuevo Alcocero; ORC-301; ORC-312; ORC-313; ORC-329; Paleoenvironmental Reconstructions from Marine Sediments @ AWI; Piston corer (BGR type); Polarstern; Polarstern Kuppe; PS01; PS01/154; PS01/155; PS01/156; PS01/161; PS01/162; PS01/177; PS01/184; PS01/186; PS01/189; PS04; PS04/225; PS04/254; PS04/256; PS04/257; PS04/258; PS04/260; PS04/261; PS04/262; PS04/263; PS04/264; PS04/265; PS04/266; PS04/271; PS04/273; PS04/318; PS04/334; PS04/335; PS04/340; PS04/346; PS04/351; PS04/357; PS04/367; PS04/370; PS04/380; PS04/382; PS04/389; PS04/414; PS04/423; PS04/429; PS04/433; PS04/440; PS04/447; PS04/449; PS04/472; PS04/477; PS04/481; PS04/484; PS04/495; PS04/500; PS04/508; PS04/509; PS06/288; PS06/289; PS06/301; PS06/302; PS06/303; PS06/304; PS06/306; PS06/311; PS06/313; PS06 SIBEX; PS08; PS08/284; PS08/289; PS08/321; PS08/324; PS08/327; PS08/333; PS08/335; PS08/336; PS08/338; PS08/340; PS08/344; PS08/345; PS08/346; PS08/347; PS08/350; PS08/353; PS08/354; PS08/355; PS08/356; PS08/357; PS08/358; PS08/359; PS08/360; PS08/361; PS08/364; PS08/365; PS08/366; PS08/367; PS08/368; PS08/369; PS08/374; PS08/375; PS08/379; PS08/380; PS08/381; PS08/382; PS08/384; PS08/385; PS08/386; PS08/387; PS08/394; PS08/396; PS08/397; PS08/401; PS08/402; PS08/410; PS08/428; PS08/430; PS08/432; PS08/438; PS08/439; PS08/440; PS08/442; PS08/445; PS08/449; PS08/450; PS08/452; PS08/480; PS08/481; PS08/482; PS08/483; PS08/564; PS08/585; PS08/601; PS08/607; PS08/610; PS08/621; PS08/627; PS10; PS10/668; PS10/672; PS10/673; PS10/675; PS10/678; PS10/682; PS10/684; PS10/686; PS10/688; PS10/690; PS10/694; PS10/697; PS10/699; PS10/701; PS10/703; PS10/707; PS10/711; PS10/719; PS10/725; PS10/738; PS10/740; PS10/748; PS10/757; PS10/760; PS10/762; PS10/766; PS10/768; PS10/778; PS10/782; PS10/784; PS10/794; PS10/804; PS10/813; PS10/816; PS10/818; PS10/820; PS10/824; PS1010-1; PS1011-1; PS1012-1; PS1013-1; PS1014-1; PS1016-1; PS1017-1; PS1018-1; PS1019-1; PS1138-8; PS1167-5; PS1169-1; PS1170-4; PS1171-1; PS1173-6; PS1174-2; PS1175-1; PS1176-3; PS1177-1; PS1178-4; PS1179-1; PS1184-6; PS1186-3; PS1194-1; PS1196-1; PS1197-1; PS1198-1; PS1199-1; PS12; PS12/116; PS12/117; PS12/119; PS12/122; PS12/127; PS12/128; PS12/129; PS12/130; PS12/132; PS12/133; PS12/185; PS12/186; PS12/193; PS12/194; PS12/195; PS12/196; PS12/199; PS12/200; PS12/238; PS12/242; PS12/244; PS12/247; PS12/248; PS12/250; PS12/252; PS12/260; PS12/266; PS12/271; PS12/273+276; PS12/280; PS12/284; PS12/287; PS12/289; PS12/291; PS12/298; PS12/300; PS12/302; PS12/305; PS12/308; PS12/310; PS12/312; PS12/314; PS12/316; PS12/319; PS12/321; PS12/323; PS12/325; PS12/327; PS12/333; PS12/336; PS12/338; PS12/340; PS12/342; PS12/344; PS12/346; PS12/348; PS12/350; PS12/352; PS12/354; PS12/356; PS12/358; PS12/360; PS12/364; PS12/366; PS12/368; PS12/372; PS12/374; PS12/376; PS12/378; PS12/380; PS12/382; PS12/384; PS12/387; PS12/396; PS12/418; PS12/437; PS12/458; PS12/465; PS12/472; PS12/486; PS12/490; PS12/492; PS12/503; PS12/504; PS12/510; PS12/526; PS12/534; PS12/536; PS1200-4; PS1201-1; PS1202-1; PS1203-1; PS1204-1; PS1205-1; PS1206-1; PS1207-1; PS1207-2; PS1208-1; PS1209-1; PS1210-1; PS1211-1; PS1212-1; PS1213-1; PS1214-1; PS1215-1; PS1216-1; PS1217-1; PS1219-1; PS1220-3; PS1222-1; PS1223-1; PS1272-1; PS1273-1; PS1275-1; PS1276-1; PS1277-1; PS1278-1; PS1279-1; PS1281-1; PS1282-1; PS1333-2; PS1338-1; PS1363-3; PS1364-1; PS1366-2; PS1367-1; PS1368-1; PS1369-1; PS1370-1; PS1371-1; PS1372-2; PS1373-2; PS1374-2; PS1375-2; PS1376-2; PS1377-1; PS1378-1; PS1379-1; PS1380-1; PS1381-1; PS1382-1; PS1383-1; PS1384-1; PS1385-1; PS1386-1; PS1387-1; PS1388-1; PS1389-1; PS1390-1; PS1391-1; PS1394-1; PS1395-1; PS1396-1; PS1397-1; PS1398-2; PS1399-1; PS1400-4; PS1401-2; PS1402-2; PS1403-1; PS1405-1; PS1406-1; PS1407-1; PS1410-1; PS1411-1; PS1412-1; PS1414-1; PS1415-1; PS1416-1; PS1417-1; PS1418-1; PS1419-1; PS1420-1; PS1421-1; PS1422-1; PS1423-1; PS1424-1; PS1425-1; PS1426-1; PS1427-1; PS1428-1; PS1451-2; PS1452-1; PS1453-1; PS1454-1; PS1455-4; PS1459-4; PS1460-1; PS1471-1; PS1472-4; PS1473-1; PS1474-1; PS1475-1; PS1476-1; PS1477-1; PS1478-1; PS1479-1; PS1480-2; PS1481-2; PS1482-2; PS1483-2; PS1484-2; PS1485-1; PS1486-2; PS1487-1; PS1488-2; PS1489-3; PS1490-2; PS1491-3; PS1492-1; PS1493-2; PS1494-2; PS1495-1; PS1496-2; PS1497-1; PS1498-1; PS1499-2; PS1500-2; PS1501-1; PS1502-1; PS1505-1; PS1506-1; PS1507-2; PS1508-2; PS1509-2; PS1537-1; PS1538-1; PS1539-1; PS1540-1; PS1542-1; PS1543-1; PS1544-1; PS1545-1; PS1546-2; PS1547-1; PS1554-1; PS1555-1; PS1557-1; PS1558-1; PS1559-1; PS1560-1; PS1563-1; PS1564-1; PS1569-1; PS1572-1; PS1573-2; PS1574-1; PS1575-1; PS1575-2; PS1576-1; PS1577-2; PS1578-1; PS1579-1; PS1581-2; PS1582-1; PS1584-1; PS1585-1; PS1586-2; PS1587-1; PS1588-2; PS1589-1; PS1590-1; PS1591-2; PS1593-1; PS1594-1; PS1595-2; PS1596-1; PS1597-1; PS1598-2; PS1599-1; PS16; PS16/403; PS16/405; PS16/410; PS16/413; PS16/415; PS16/417; PS16/419; PS16/425; PS16/427; PS16/430; PS16/432; PS16/446; PS16/472; PS16/499; PS16/507; PS16/509; PS16/510; PS16/515; PS16/516; PS16/518; PS16/525; PS16/526; PS16/528; PS16/530; PS16/534; PS16/536; PS16/540; PS16/541; PS16/547; PS16/549; PS16/552; PS16/554; PS16/557; PS1600-2; PS1601-1; PS1602-1; PS1603-2; PS1604-1; PS1605-3; PS1606-1; PS1607-1; PS1608-1; PS1609-2; PS1610-3; PS1611-1; PS1612-1; PS1613-2; PS1614-1; PS1615-2; PS1616-1; PS1617-2; PS1618-2; PS1619-1; PS1620-2; PS1621-2; PS1622-1; PS1623-2; PS1624-1; PS1625-1; PS1626-1; PS1627-1; PS1628-2; PS1629-1; PS1631-1; PS1632-1; PS1635-2; PS1636-1; PS1637-1; PS1638-1; PS1639-1; PS1640-3; PS1641-1; PS1642-1; PS1643-3; PS1645-1; PS1647-2; PS1648-2; PS1787-1; PS1788-1; PS1790-2; PS1791-1; PS1792-2; PS1793-1; PS1794-2; PS1795-1; PS1796-2; PS1797-1; PS1798-2; PS18; PS18/044; PS18/048; PS18/055; PS18/056; PS18/058; PS18/059; PS18/063; PS18/065; PS18/067; PS18/075; PS18/080; PS18/081; PS18/082; PS18/083; PS18/084; PS18/086; PS18/088; PS18/092; PS18/094; PS18/096; PS18/100; PS18/101; PS18/102; PS18/106; PS18/108; PS18/114; PS18/126; PS18/127; PS18/129; PS18/135; PS18/141; PS18/142; PS18/143; PS18/144; PS18/145; PS18/146; PS18/147; PS18/148; PS18/149; PS18/150; PS18/151; PS18/152; PS18/153; PS18/154; PS18/161; PS18/165; PS18/166; PS18/167; PS18/169; PS18/170; PS18/171; PS18/172; PS18/173; PS18/175; PS18/177; PS18/178; PS18/179; PS18/180; PS18/181; PS18/182; PS18/183; PS18/184; PS18/185; PS18/186; PS18/187; PS18/189; PS18/190; PS18/191; PS18/192; PS18/193; PS18/194; PS18/196; PS18/198; PS18/199; PS18/200; PS18/201; PS18/202; PS18/203; PS18/204; PS18/208; PS18/210; PS18/211; PS18/212; PS18/214; PS18/216; PS18/217; PS18/218; PS18/219; PS18/221; PS18/222; PS18/227; PS1800-2; PS1802-2; PS1803-2; PS1805-5; PS1806-5; PS18 06AQANTIX_2; PS1807-1; PS1811-7; PS1812-5; PS1813-5; PS1817-5; PS1818-1; PS1819-5; PS1820-5; PS1821-5; PS1822-1; PS1823-1; PS1824-2; PS1825-5; PS1826-2; PS1828-2; PS1829-1; PS1831-5; PS1953-1; PS1954-1; PS1957-1; PS1958-1; PS1960-1; PS1961-1; PS1963-1; PS1964-1; PS1965-1; PS1967-
    Type: Dataset
    Format: application/zip, 3 datasets
    Location Call Number Expected Availability
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  • 4
    facet.materialart.
    Unknown
    PANGAEA
    In:  Supplement to: Kröncke, Ingrid (1998): Macrofauna communities in the Amundsen Basin, at the Morris Jesup Rise and at the Yermak Plateau (Eurasian Arctic Ocean). Polar Biology, 19(6), 383-392, https://doi.org/10.1007/s003000050263
    Publication Date: 2024-06-25
    Description: Macrofaunal communities of the western Eurasian Arctic Ocean were studied along a transect from the North Pole, across the Amundsen Basin and Gakkel Ridge towards the Morris Jesup Rise and the Yermak Plateau. Samples were collected during autumn 1991, from depths of 560±4411 m, using a box corer. Macrofaunal species numbers varied from 1 to 11 per 0.02 m**2 in the basins approaching the Morris Jesup Rise and from 44 to 81 per 0.25 m**2 at the Yermak Plateau. Abundances increased from 1 to 31 per 0.02 m**2 in the basin and on the Morris Jesup Rise to 24±60 per 0.02 m**2 on the Yermak Plateau. Biomass was low in the basin and at the Morris Jesup Rise (0.5±68.9 mg per 0.02 m**2) but increased to 116.64 mg per 0.02 m**2 at the Yermak Plateau. A total of 108 taxa were recorded. The results contradict the hypothesis that diversity decreases with increasing latitude, and the high species richness at low abundance at intermediate depths was comparable with that observed in Antarctic and tropical regions.
    Keywords: Amundsen Basin; ARK-VIII/3; Giant box corer; GKG; Morris Jesup Rise; Nansen Basin; Polarstern; PS19/196; PS19/198; PS19/200; PS19/204; PS19/206; PS19/210; PS19/214; PS19/216; PS19/218; PS19/220; PS19/222; PS19/226; PS19/239; PS19/241; PS19/245; PS19/246; PS19/249; PS19 ARCTIC91; PS2191-4; PS2192-1; PS2193-2; PS2194-1; PS2195-4; PS2196-2; PS2198-1; PS2199-5; PS2200-3; PS2201-2; PS2202-11; PS2205-7; PS2209-3; PS2210-1; PS2212-1; PS2213-1; PS2214-1; Yermak Plateau
    Type: Dataset
    Format: application/zip, 2 datasets
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  • 5
    facet.materialart.
    Unknown
    PANGAEA
    In:  Supplement to: Ó Cofaigh, Colm; Dowdeswell, Julian A; Grobe, Hannes (2001): Holocene glacimarine sedimentation, inner Scoresby Sund, East Greenland: the influence of fast-flowing ice-sheet outlet glaciers. Marine Geology, 175(1-4), 103-129, https://doi.org/10.1016/S0025-3227(01)00117-7
    Publication Date: 2024-06-25
    Description: Holocene glacimarine sedimentation associated with fast-flowing outlet glaciers draining the Greenland Ice Sheet is investigated using sedimentary and acoustic data from inner Scoresby Sund, East Greenland. Sedimentation in inner Scoresby Sund is dominated by three processes which are influenced by differences in proximity to fast-flowing outlet glaciers, extent of glacier-ice cover and fjord bathymetry: (1) sediment-gravity flow, principally in the form of turbidity currents and debris flows; (2) suspension sedimentation from turbid meltwater plumes; and (3) iceberg rafting. These processes result in texturally and sedimentologically heterogeneous lithofacies. Proportionally, fine-grained muds (laminated, stratified and massive facies) dominate cores recovered from inner Scoresby Sund, accounting for 80% of the total, whereas diamict facies account for only 15%. Abundant fine-grained muds demonstrate that meltwater flux and sedimentation is significant in this high Arctic glacimarine environment, in settings proximal to fast-flowing outlet glaciers. With increasing distance from these glacier termini, muds are replaced progressively by iceberg-rafted, coarse-grained sediment. The dominance of this iceberg-rafted sediment in outer Scoresby Sund reflects both its more distal location from fast-flowing glacier termini, and the high calving flux associated with these ice masses. Laminated muds deposited by turbidity currents and suspension settling from overflow plumes in inner Scoresby Sund are similar to lithofacies produced in temperate and subpolar glacimarine systems. This implies a similarity in sedimentation processes and resulting facies across a wide spectrum of climatically-, glaciologically- (fast-flowing and non fast-flowing ice-masses) and oceanographically-variable glacimarine settings. Recognition of laminated, fine-grained facies in the geological record therefore does not necessarily indicate a temperate palaeo-glacial setting. However, the predominance of iceberg-rafted diamict facies in ice-distal sedimentary records suggests the former presence of relatively cold environmental conditions in which iceberg-sedimentation played a dominant role.
    Keywords: ARK-VII/1; ARK-VII/3b; AWI_Paleo; Giant box corer; GKG; Gravity corer (Kiel type); Greenland Shelf; Greenland Slope; Paleoenvironmental Reconstructions from Marine Sediments @ AWI; Polarstern; PS17; PS17/244; PS17/251; PS17/252; PS17/257; PS17/258; PS17/260; PS17/262; PS17/264; PS17/265; PS17/266; PS17/271; PS17/272; PS17/273; PS17/274; PS17/275; PS17/276; PS17/277; PS17/281; PS17/282; PS17/283; PS17/285; PS17/288; PS17/290; PS1921-1; PS1927-1; PS1928-1; PS1929-2; PS1930-1; PS1930-2; PS1931-1; PS1932-1; PS1932-2; PS1933-1; PS1934-1; PS1935-1; PS1936-1; PS1937-2; PS1938-1; PS1939-1; PS1939-2; PS1940-1; PS1941-1; PS1942-1; PS1943-1; PS1944-1; PS1945-1; PS1946-1; PS1949-2; PS1951-1; Quaternary Environment of the Eurasian North; QUEEN; Scoresby Sund; SL
    Type: Dataset
    Format: application/zip, 8 datasets
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  • 6
    facet.materialart.
    Unknown
    PANGAEA
    In:  Supplement to: Nowaczyk, Norbert R; Antonow, Martin (1997): High-resolution magnetostratigraphy of four sediment cores from the Greenland Sea - I. Identification of the Mono Lake excursion, Laschamp and Biwa I/Jamaica geomagnetic polarity events. Geophysical Journal International, 131(2), 310-324, https://doi.org/10.1111/j.1365-246X.1997.tb01224.x
    Publication Date: 2024-06-25
    Description: High-resolution magnetostratigraphic analysis of three sediment cores from the base of the volcanic seamount Vesteris Banken in the Greenland Basin and one core from the Jan Mayen Fracture Zone revealed records of three pronounced geomagnetic events within the last 200 ka. Dating by stable carbon and oxygen isotope analysis, AMS14C measurements and biostratigraphic data (foraminifera abundances) yielded ages of 28-27 ka for the Mono Lake excursion, 37-33 ka for the Laschamp event, and 189-179 ka for the Biwa I event. In at least one of the cores the Laschamp event exhibits a full reversal of the local geomagnetic field vector. The same is true of the Biwa I event, documented in one of the cores.
    Keywords: ARK-V/2; ARK-VII/1; AWI_Paleo; Giant box corer; GIK21702-2 PS13/132; GIK21707-1 PS13/149; GIK21707-2 PS13/149; GIK21878-3 PS17/050; GIK21882-2 PS17/056; GIK21892-3 PS17/067; GKG; Greenland Sea; Jan Mayen Fracture Zone; KAL; Kasten corer; Norwegian Sea; Paleoenvironmental Reconstructions from Marine Sediments @ AWI; Polarstern; PS13; PS17; PS1702-2; PS1707-1; PS1707-2; PS1878-3; PS1882-2; PS1892-3; Vesteris Banken
    Type: Dataset
    Format: application/zip, 15 datasets
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  • 7
    facet.materialart.
    Unknown
    PANGAEA
    In:  Alfred Wegener Institute, Helmholtz Centre for Polar and Marine Research, Bremerhaven
    Publication Date: 2024-06-25
    Description: During the "Polarstern"-expeditions ARK-IX/4 (1993) and ARK-XI/1 (1995), organised by the Alfred Wegener Institute (AWI), acoustic subbottom profiles (Parasound) have been collected in the Laptev Sea Shelf, Siberia. These data have been interpreted as an indicator of ice scours frequency and off-shore permafrost patterns. An additional acoustic profile data-base was available by the results of the expedition of the Federal Institute for Geosciences and Natural Resources (BGR) of the year 1994. The area of the expedition was located closer to the shelf, therefore supports a better understanding of ice scours frequency in shallower marine environments. The data-file consists of a 2930 km Parasound-traverse and has been subdivided into 586 working profiles. They are characterised by their location, number of ice scours, interpreted patterns of reflection and their extension and morphology. The data have been evaluated statistically and graphically and were presented in a map. Different patterns of sea floor reflection were established by different environments, outer influences (e.g. size of the icebergs, direction of the drift of icebergs) and the climatic history of the region. In the north-westerly region of the Laptev Sea at the continental slope of Severnaya Zemlya the sea floor in shallower depths has been ploughed intensely by recent icebergs. In some regions (40-60m), as an effect of intensely ploughing, the sea floor is hardly defined in acoustic profiles come along with relocation of marine deposits. Glacial diamiet deposits prevented the development of deep scours. Up to 355m deeper scours result from lower sea levels. The marginal north-easterly region of the Laptev Sea is characterised exclusively by this type of scour. Morphology and depth of these scours can be compared with those of the westerly Vilkitsky-Street so that similar conditions of development may be expected. Both, the north-easterly Laptev Sea and the Vilkitsky-Street, are not dominated by patterns ofrecent icebergs. In contrary the shelf-regions north-easterly ofthe Taimyr peninsula and north-westerly of the New Siberian Islands have been modified evidently by recent icebergs, which drifted with prevalent currents anticlockwise along the shelf edge of the Laptev Sea and cause the deepest scours of the whole region. The off-shore permafrost at the inner shelf regions has an important influence on the scours intensity. The permafrost layer can be recognised by the maximum depth of ice scours. It is represented by a Parasound reflector that can be made up for distances. The age of the ice scours cannot be determined absolutely by Parasound data but a relative order can be estimated whenever two scours are situated close to each other. When the Parasound-traverse ofthe expedition ARK-IX/4 (1993) (77°24'N 133°30'E-77°30'N 133°40'E) was repeated partially in expedition ARK-XI/l (1995) the ice scours of 1993 remained unchanged and uneroded and no new ice scours had been detected. It can be concluded that scours persist for a long time in the Laptev Sea, though after all with an average of 3 ice scours per kilometer there are not many at all in the Laptev Sea.
    Keywords: ARK-IX/4; ARK-IX/4_LaptevSea; AWI_Paleo; Laptev Sea; Paleoenvironmental Reconstructions from Marine Sediments @ AWI; ParaSound; Polarstern; PS; PS27
    Type: Dataset
    Format: application/zip, 2 datasets
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  • 8
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    PANGAEA
    In:  Supplement to: Vidal, Laurence; Schneider, Ralph R; Marchal, Olivier; Bickert, Torsten; Stocker, Thomas F; Wefer, Gerold (1999): Link between the North and South Atlantic during the Heinrich events of the last galcial period. Climate Dynamics, 15(12), 909-919, https://doi.org/10.1007/s003820050321
    Publication Date: 2024-06-25
    Description: High resolution benthic oxygen isotope records combined with radiocarbon datings, from cores retrieved in the North, Equatorial, and South Atlantic are used to establish a reliable cronostratigraphy for the last 60 ky. This common temporal framework enables us to study the timing of the sub-Milankovitch climate variability in the entire surface Atlantic during this period, as reflected in planktonic oxygen isotope records. Variations in sea surface temperatures in the Equatorial and South Atlantic reveal two warm periods during the mid-stage 3 which are correlated to the warming observed in the North Atlantic after Heinrich events (HL) 5 and 4. However, the records show that the warming started about 1500 y earlier in the South Atlantic. A zonally averaged ocean circulation model simulates a similar north-south thermal antiphasing between the latitudes of our coring sites, when pertubated by a freshwater flux anomaly. We infer that the observed phase relationship between the northern and the southern Atlantic is related to periods of reduced NADW production in the North Atlantic, such as during HL5 and HL4.
    Keywords: Amazon Fan; GeoB; GeoB1515-1; GeoB1515-2; GeoB1711; GeoB1711-4; Geosciences, University of Bremen; Giant box corer; GKG; Gravity corer (Kiel type); M16/2; M20/2; Meteor (1986); Namibia continental slope; SL
    Type: Dataset
    Format: application/zip, 5 datasets
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  • 9
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    PANGAEA
    In:  Supplement to: Rühlemann, Carsten; Mulitza, Stefan; Müller, Peter J; Wefer, Gerold; Zahn, Rainer (1999): Warming of the tropical Atlantic Ocean and slowdown of thermohaline circulation during the last deglaciation. Nature, 402(6761), 511-514, https://doi.org/10.1038/990069
    Publication Date: 2024-06-25
    Description: Evidence for abrupt climate changes on millennial and shorter timescales is widespread in marine and terrestrial climate records (Dansgard et al., 1993, doi:10.1038/364218a0; Bond et al., 1993, doi:10.1038/365143a0; Charles et al., 1996, doi:10.1016/0012-821X(96)00083-0, Bard et al., 1997, doi:10.1038/385707a0). Rapid reorganization of ocean circulation is considered to exert some control over these changes (Broecker et al., 1985, doi:10.1038/315021a0), as are shifts in the concentrations of atmospheric greenhouse gases (Broecker, 1994, doi:10.1038/372421a0). The response of the climate system to these two influences is fundamentally different: slowing of thermohaline overturn in the North Atlantic Ocean is expected to decrease northward heat transport by the ocean and to induce warming of the tropical Atlantic (Crowley, 1992, doi:10.1029/92PA01058; Manabe and Stouffer, 1997, doi:10.1029/96PA03932), whereas atmospheric greenhouse forcing should cause roughly synchronous global temperature changes (Manabe et al., 1991, doi:10.1175/1520-0442(1991)004〈0785:TROACO〉2.0.CO;2). So these two mechanisms of climate change should be distinguishable by the timing of surface-water temperature variations relative to changes in deep-water circulation. Here we present a high-temporal-resolution record of sea surface temperatures from the western tropical North Atlantic Ocean which spans the past 29,000 years, derived from measurements of temperature-sensitive alkenone unsaturation in sedimentary organic matter. We find significant warming is documented for Heinrich event H1 (16,900-15,400 calendar years bp) and the Younger Dryas event (12,900-11,600 cal. yr bp), which were periods of intense cooling in the northern North Atlantic. Temperature changes in the tropical and high-latitude North Atlantic are out of phase, suggesting that the thermohaline circulation was the important trigger for these rapid climate changes.
    Keywords: Gravity corer (Kiel type); M35/1; M35003-4; Meteor (1986); SL
    Type: Dataset
    Format: application/zip, 2 datasets
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  • 10
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    Unknown
    PANGAEA
    In:  Supplement to: Breitzke, Monika; Grobe, Hannes; Kuhn, Gerhard; Müller, Peter J (1996): Full waveform ultrasonic transmission seismograms: a fast new method for the determination of physical and sedimentological parameters of marine sediment cores. Journal of Geophysical Research: Solid Earth, 101(B10), 22123-22142, https://doi.org/10.1029/96JB01891
    Publication Date: 2024-06-25
    Description: Detailed information about the sediment properties and microstructure can be provided through the analysis of digital ultrasonic P wave seismograms recorded automatically during full waveform core logging. The physical parameter which predominantly affects the elastic wave propagation in water-saturated sediments is the P wave attenuation coefficient. The related sedimentological parameter is the grain size distribution. A set of high-resolution ultrasonic transmission seismograms (ca. 50-500 kHz), which indicate downcore variations in the grain size by their signal shape and frequency content, are presented. Layers of coarse-grained foraminiferal ooze can be identified by highly attenuated P waves, whereas almost unattenuated waves are recorded in fine-grained areas of nannofossil ooze. Color-encoded pixel graphics of the seismograms and instantaneous frequencies present full waveform images of the lithology and attenuation. A modified spectral difference method is introduced to determine the attenuation coefficient and its power law a = kfn. Applied to synthetic seismograms derived using a "constant Q" model, even low attenuation coefficients can be quantified. A downcore analysis gives an attenuation log which ranges from ca. 700 dB/m at 400 kHz and a power of n = 1-2 in coarse-grained sands to few decibels per meter and n 〈= 0.5 in fine-grained clays. A least squares fit of a second degree polynomial describes the mutual relationship between the mean grain size and the attenuation coefficient. When it is used to predict the mean grain size, an almost perfect coincidence with the values derived from sedimentological measurements is achieved.
    Keywords: Brazil Basin; GeoB1510-2; GeoB2821-1; Gravity corer (Kiel type); M16/2; M29/2; Meteor (1986); Rio Grande Rise; SFB261; SL; South Atlantic in Late Quaternary: Reconstruction of Budget and Currents
    Type: Dataset
    Format: application/zip, 3 datasets
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