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  • Data  (8,980)
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  • 1
    facet.materialart.
    Unknown
    Palynology of marine sediment cores from the West African coast (1982)
    PANGAEA
    In:  Supplement to: Agwu, Chiori O C; Beug, Hans-Jürgen (1982): Palynological studies of marine sediments off the West African coast. Meteor Forschungsergebnisse, Deutsche Forschungsgemeinschaft, Reihe C Geologie und Geophysik, Gebrüder Bornträger, Berlin, Stuttgart, C36, 1-30
    Details
    Publication Date: 2024-06-25
    Description: Seven sediment cores from the cruises of the "Meteor" and "Valdivia" were examined palynologically. The cores were retrieved from the lower continental slope in the area of between 33.5° N and 8° N, off the West African coast. Most of the cores contain sediments from the last Glacial and Interglacial period. In some cases, the Holocene sediments are missing. Some individual cores contain sediments also from earlier Glacial and Interglacial periods. The main reason for making this palynological study was to find out the differences between the vegetation of Glacial and Interglacial periods in those parts of West Africa which at present belong to the Mediterranean zone, the Sahara and the zones of the savannas and tropical forests. In today's Mediterranean vegetation zone at core 33.5° N, forests and deciduous forests in particular, are missing during Glacial conditions. Semi-deserts are found instead of these. In the early isotope stage 1, there is a very significant development of forests which contain evergreen oaks; this is the Mediterranean type of vegestation development. The Sahara type of vegetation development is shown in four cores from between 27° N and 19° N. The differences between Glacial and Interglacial periods are very small. It must be assumed therefore that in this latitudes, both Glacial and Interglacial conditions gave rise to desert generally. The results are in favour of a slightly more arid climate during Glacial and more humid one during Interglacial periods. The southern boundary of the Sahara and the adjacent savannas with grassland and tropical woods were situated more to the south during the Glacial periods than they were during the Interglacial ones. In front of today's savanna belt, it can be seen from the palynological results that there are considerable differences between the vegetation of Glacial and Interglacial periods. The woods are more important in Interglacial periods. During the Glacial periods these are replaced from north to south decreasingly by grassland (savanna and rainforest type of vegetation development). The southern limit of the Sahara during stage 2 was somewhat between 12° N and 8° N which is between 1.5 and 5 degrees in latitude further south than it i s today. Not only do these differences in climate and vegetation apply to the maximum of the last Glacial and for the Holocene, but they apparently apply also to the older Glacial and Interglacial periods, where they have been found in the profiles. The North African deset belt can be said to have expanded during Glacial times both towards the north and towards the south. All the available evidence of this study indicates that the grass land or the semi-desert of the Southern Europe cam einto connection with those of the N Africa; there could not have been any forest zone between them. The present study was also a good opportunity for investigating some of the basic marine palynological problems. The very well known overrepresentation of pollen grains of the genus Pinus in marine sediments can be traced as fa as 21° N. The present southern limit for the genus Pinus is on the Canaries and on the African continent as approximately 31° N. Highest values of Ephedra pollen grains even occur south of the main area of the present distribution of that genus. These does not seem to be any satisfactory explanation for this. In general, it would appear that the transport of pollen grains from the north is more important than transport from the south. The results so far, indicate strongly that further palynological studies are necessary. These should concentrate particularly on cores from between 33° N and 27° N as well as between 17° N and 10° N. It would also be useful to have a more detailed examination of sediments from the last Intergalcial period (substage 5 e). Absolute pollen counts and more general examination of surface samples would be desirable. Surface samples should be taken from the shelf down to the bottom of the continental slope in different latitudes.
    Keywords: ARKTIS 1993; East Atlantic; GIK12309-3; GIK12310-4; GIK12329-6; GIK12392-1; KAL; Kasten corer; M12392-1; M25; M30; M30_184; M8_017-2; M8017B; Meteor (1964); PC; Piston corer; South Atlantic Ocean; SPC; Sphincter corer; VA132; VA132-18-1; Valdivia (1961); Westafrika 1973
    Type: Dataset
    Format: application/zip, 7 datasets
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  • 2
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    Unknown
    Stable isotope record of planktic foraminifera sampled by plankton haul and in surface sediments off North-West Africa (1983)
    PANGAEA
    In:  Supplement to: Ganssen, Gerald M (1983): Dokumentation von küstennahmen Auftrieb anhand stabiler Isotope in rezenten Foraminiferen vor Nordwest-Afrika. Meteor Forschungsergebnisse, Deutsche Forschungsgemeinschaft, Reihe C Geologie und Geophysik, Gebrüder Bornträger, Berlin, Stuttgart, C37, 1-46
    Details
    Publication Date: 2024-06-25
    Description: Foraminifera shells from modern sediments document the hydrography of the coastal upwelling region off Northwest-Africa (12-35° N) through the stable isotopic composition of their shells. Oxygen isotopes in planktonic foraminifers reflect sea surface temperatures (SST) during the main growing season of the differnt species: Globigerinoides ruber (pink and white) and G. sacculifer delineate the temperatures of the summer, Globorotalia inflata and Pulleniatina obliquiloculata those of the winter. Oxygen isotopes on Globigerina bulloides document temperature ranges of the upwelling seasons. d18O values in planktonic foraminifera from plankton hauls resemble those from the surface sediment samples, if the time of the plankton collection is identical with that of the main growing season of the species. The combined isotopic record of G. ruber (white) and G. inflata clearly reveals the latitudinal variations of the annual mean SST. The deviation of the d18O values from both species from their common mean is a scale for the seasonality, i.e. the maximum temperature range within one year. Thus in the summer upwelling region (north of 25° N) seasonality is relatively low, while it becomes high in the winter upwelling region south of 20° N. Furthermore, the winter upwelling region is characterized by relatively high d18O values - indicating low temperatures - in G. bulloides, the region of summer upwelling by relatively low d180 values compared with the constructed annual mean SST. Generally, carbon isotopes from the plankton hauls coincide with those from sediment surface samples. The enrichment of 13C isotopes in foraminifers from areas with high primary production can be caused by the removal of 12C from the total dissolved inorganic carbon during phytoplankton blooms. It is found that carbon isotopes from plankton hauls off Northwest-Africa are relatively enriched in 13C compared with samples from the western Atlantic Ocean. Also shells of G. ruber (pink and white) from upwelling regions are enriched in the heavier isotope compared with regions without upwelling. In the sediment, the enrichement of 13C due to high primary production can only be seen in G. bulloides from the high fertile upwelling region south of 20° N. North of this latitude values are relatively low. An enrichment of 12C is observed in shells of G. ruber (pink), G. inflata and P. obliquiloculata from summer-winter- and perennial upwelling regions respectively. Northern water masses can be distinguished from their southern counterparts by relatively high oxygen and carbon values in the „living“ (=stained) benthic foraminifera Uvigerina sp. and Hoeglundina elegans. A tongue of the Mediterranean Outflow water can be identified far to the south (20° N) by 13C-enriched shells of these benthic foraminifera. A zone of erosion (15-25° N, 300-600 m) with a subrecent sediment surface can be mapped with the help of oxygen isotopes in „dead“ benthic specimens. Comparison of d18O values in aragonitic and calcitic benthic foraminifers does not show a differential influence of temperature on the isotopic composition in the carbonate. However, carbon isotopes reflect slightly differences under the influence of temperature.
    Keywords: 17KL; 1KL; 21KL; 42KL; 82KL; 83KL; 92KL; Atlantic Ocean; BCR; Bottle, Niskin; Box corer (Reineck); East Atlantic; FBG; FGGE-Equator 79 - First GARP Global Experiment; Giant box corer; GIK/IfG; GIK12301-5; GIK12302-3; GIK12303-3; GIK12304-3; GIK12305-2; GIK12306-2; GIK12307-3; GIK12308-2; GIK12309-1; GIK12310-1; GIK12313-2; GIK12314-2; GIK12315-1; GIK12316-1; GIK12317-1; GIK12322-2; GIK12323-1; GIK12324-1; GIK12325-4; GIK12326-2; GIK12327-2; GIK12328-1; GIK12329-2; GIK12338-1; GIK12339-2; GIK12340-3; GIK12341-2; GIK12342-1; GIK12343-1; GIK12344-2; GIK12345-3; GIK12346-1; GIK12347-1; GIK12349-3; GIK13220-1; GIK13221-1; GIK13222-1; GIK13223-3; GIK13224-2; GIK13225-2; GIK13230-1; GIK13231-1; GIK13232-1; GIK13233-1; GIK13234-1; GIK13235-2; GIK13236-1; GIK13237-1; GIK13238-1; GIK13273-1; GIK13274-1; GIK13275-1; GIK13276-1; GIK13279-3; GIK13280-1; GIK13282-1; GIK13283-2; GIK13289-1; GIK13290-1; GIK13526-4; GIK13527-1; GIK13528-2; GIK13529-1; GIK13530-1; GIK13532-2; GIK13533-1; GIK13534-1; GIK13536-2; GIK13557-1; GIK13583-1; GIK13584-2; GIK13585-1; GIK13586-3; GIK13587-1; GIK13588-2; GIK15626-1; GIK15627-2; GIK15627-5; GIK15628-4; GIK15629-1; GIK15630-1; GIK15631-1; GIK15632-1; GIK15634-1; GIK15635-2; GIK15637-3; GIK15638-2; GIK15639-1; GIK15640-1; GIK15641-2; GIK15642-1; GIK15643-1; GIK15644-1; GIK15645-1; GIK15646-1; GIK15647-1; GIK15648-1; GIK15651-3; GIK15651-4; GIK15652-2; GIK15654-1; GIK15657-1; GIK15658-1; GIK15658-2; GIK15659-1; GIK15660-1; GIK15663-1; GIK15664-1; GIK15666-8; GIK15666-9; GIK15667-1; GIK15669-2; GIK15670-1; GIK15672-2; GIK15673-2; GIK15676-2; GIK15677-1; GIK15678-1; GIK15678-3; GIK15679-2; GIK16002-1; GIK16003-1; GIK16005-1; GIK16012-3; GIK16024-1; GIK16032-1; GKG; Grab (Shipek); Institute for Geosciences, Christian Albrechts University, Kiel; M25; M51; M51-13; M53; M53_005; M53_006; M53_008; M53_009; M53_010; M53_011; M53_014; M53_020; M53_022; M53_158; M53_164; M53_166; M53_167; M53_169; M53_170-1; M53_172-1; M53_173-2; M60; Meteor (1964); MG; MSN; Multiboxcorer; Multiple opening/closing net; NIS; Northeast Atlantic; off West Africa; Photo grab; PLA; Plankton net; SHIPEK; SPC; Sphincter corer; SUBTROPEX 82; VA-10/3; VA-28/2; VA79-10NET; VA79-17KLa; VA79-1KLa; VA79-21KLa; VA79-42KLa; VA79-82KLa; VA79-83KLa; VA79-92KLa; Valdivia (1961); van Veen Grab; VGRAB
    Type: Dataset
    Format: application/zip, 11 datasets
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  • 3
    facet.materialart.
    Unknown
    Occurrence of hiatuses PH and NH 1 through NH 7 in DSDP holes (1983)
    PANGAEA
    In:  Supplement to: Keller, Gerta; Barron, John A (1983): Paleoceanographic implications of Miocene deep-sea hiatuses. Geological Society of America Bulletin, 94(5), 590-613, https://doi.org/10.1130/0016-7606(1983)94%3C590:PIOMDH%3E2.0.CO;2
    Details
    Publication Date: 2024-06-25
    Description: Miocene paleoceanographic evolution exhibits major changes resulting from the opening and closing of passages, the subsequent changes in oceanic circulation, and development of major Antarctic glaciation. The consequences and timing of these events can be observed in variations in the distribution of deep-sea hiatuses, sedimentation patterns, and biogeographic distribution of planktic organisms. The opening of the Drake Passage in the latest Oligocene to early Miocene (25-20 Ma) resulted in the establishment of the deep circumpolar current, which led to thermal isolation of Antarctica and increased global cooling. This development was associated with a major turnover in planktic organisms, resulting in the evolution of Neogene assemblages and the eventual extinction of Paleogene assemblages. The erosive patterns of two widespread hiatuses (PH, 23.0-22.5 Ma; and NH 1, 20-18 Ma) indicate that a deep circumequatorial circulation existed at this time, characterized by a broad band of carbonate-ooze deposition. Siliceous sedimentation was restricted to the North Atlantic and a narrow band around Antarctica. A major reorganization in deep-sea sedimentation and hiatus distribution patterns occurred near the early/middle Miocene boundary, apparently resulting from changes in oceanic circulation. Beginning at this time, deep-sea erosion occurred throughout the Caribbean (hiatus NH 2, 16-15 Ma), suggesting disruption of the deep circumequatorial circulation and northward deflection of deep currents, and/or intensification of the Gulf Stream. Sediment distribution patterns changed dramatically with the sudden appearance of siliceous-ooze deposition in the marginal and east equatorial North Pacific by 16.0 to 15.5 Ma, coincident with the decline of siliceous sedimentation in the North Atlantic. This silica switch may have been caused by the introduction of Norwegian Overflow Water into the North Atlantic acting as a barrier to outcropping of silica-rich Antarctic Bottom Water. The main aspects of the present oceanic circulation system and sediment distribution pattern were established by 13.5 to 12.5 Ma (hiatus NH 3), coincident with the establishment of a major East Antarctic ice cap. Antarctic glaciation resulted in a broadening belt of siliceous-ooze deposition around Antarctica, increased siliceous sedimentation in the marginal and east equatorial North Pacific and Indian Oceans, and further northward restriction of siliceous sediments in the North Atlantic. Periodic cool climatic events were accompanied by lower eustatic sea levels and widespread deep-sea erosion at 12 to 11 Ma (NH 4), 10 to 9 Ma (NH 5), 7.5 to 6.2 Ma (NH 6), and 5.2 to 4.7 Ma (NH 7).
    Keywords: 10-90; 10-97; 11-101; 11-102; 11-103; 11-104; 12-111; 12-116; 12-119; 14-141; 14-142; 15-149; 15-150; 15-151; 15-153; 15-154; 16-155; 16-157; 16-158; 16-159; 16-160; 16-161; 16-162; 16-163; 17-164; 17-165; 17-166; 17-168; 17-170; 17-171; 18-172; 18-173; 19-183; 19-192; 20-199; 20-200; 20-202; 21-205; 21-206; 21-207; 21-208; 21-209; 21-210; 22-212; 22-213; 22-214; 22-215; 22-216; 22-218; 23-220; 23-221; 23-223; 23-224; 24-231; 24-234; 24-236; 24-237; 24-238; 26-251; 26-253; 26-254; 26-255; 26-256; 26-257; 26-258; 27-259; 28-264; 28-265; 28-266; 28-273; 28-274; 29-275; 29-276; 29-277; 29-278; 29-279; 29-280; 29-281; 29-282; 29-283; 29-284; 30-285; 30-286; 30-287; 30-288; 30-289; 31-290; 31-292; 31-296; 3-14; 3-15; 3-17; 3-20; 32-304; 32-305; 32-306; 32-307; 32-308; 32-310; 32-311; 32-313; 33-315; 33-316; 33-317; 33-318; 34-319; 36-327; 36-328; 36-329; 37-334; 38-336; 38-338; 38-339; 38-352; 39-354; 39-355; 39-356; 39-357; 39-359; 40-360; 40-362; 40-363; 40-364; 41-366; 41-368; 41-369; 42-372; 4-25; 4-29; 4-30; 43-386; 44-391; 45-396; 47-397; 47-398; 48-400; 48-404; 48-405; 48-406; 49-407; 49-408; 49-410; 5-34; 5-36; 5-38; 5-39; 5-40; 5-41; 5-42; 55-430; 55-431; 55-432; 55-433; 56-436; 57-438; 57-439; 57-440; 58-443; 58-444; 58-445; 59-447; 59-448; 59-449; 59-450; 59-451; 61-462; 62-463; 62-464; 62-465; 62-466; 63-467; 63-468; 63-469; 63-470; 63-471; 63-472; 6-45; 6-46; 6-47; 6-48; 6-49; 6-50; 6-51; 6-52; 6-53; 6-55; 6-56; 67-495; 68-503; 7-61; 7-62; 7-63; 7-64; 7-65; 7-66; 7-67; 8-68; 8-69; 8-70; 8-71; 8-72; 8-73; 8-74; 8-75; 9-77; 9-78; 9-79; 9-83; 9-84; Antarctic Ocean; Antarctic Ocean/BASIN; Antarctic Ocean/CONT RISE; Antarctic Ocean/PLATEAU; Antarctic Ocean/RIDGE; Antarctic Ocean/Tasman Sea; Antarctic Ocean/Tasman Sea/CONT RISE; Antarctic Ocean/Tasman Sea/PLATEAU; Antarctic Ocean/Tasman Sea/RIDGE; Caribbean Sea/BASIN; Caribbean Sea/GAP; Caribbean Sea/RIDGE; Deep Sea Drilling Project; DRILL; Drilling/drill rig; DSDP; Glomar Challenger; Gulf of Mexico/BANK; Gulf of Mexico/PLAIN; Indian Ocean//BASIN; Indian Ocean//FAN; Indian Ocean//FRACTURE ZONE; Indian Ocean//PLATEAU; Indian Ocean//RIDGE; Indian Ocean/Arabian Sea/HILL; Indian Ocean/Arabian Sea/PLAIN; Indian Ocean/Arabian Sea/RIDGE; Indian Ocean/Gulf of Aden/BASIN; Leg10; Leg11; Leg12; Leg14; Leg15; Leg16; Leg17; Leg18; Leg19; Leg20; Leg21; Leg22; Leg23; Leg24; Leg26; Leg27; Leg28; Leg29; Leg3; Leg30; Leg31; Leg32; Leg33; Leg34; Leg36; Leg37; Leg38; Leg39; Leg4; Leg40; Leg41; Leg42; Leg43; Leg44; Leg45; Leg47; Leg48; Leg49; Leg5; Leg55; Leg56; Leg57; Leg58; Leg59; Leg6; Leg61; Leg62; Leg63; Leg67; Leg68; Leg7; Leg8; Leg9; Mediterranean Sea/BASIN; North Atlantic/BASIN; North Atlantic/CONT RISE; North Atlantic/CONT SLOPE; North Atlantic/DIAPIR; North Atlantic/KNOLL; North Atlantic/Norwegian Sea; North Atlantic/Norwegian Sea/DIAPIR; North Atlantic/Norwegian Sea/PLATEAU; North Atlantic/PLAIN; North Atlantic/PLATEAU; North Atlantic/RIDGE; North Atlantic/SEAMOUNT; North Atlantic/SEDIMENT POND; North Pacific; North Pacific/ABYSSAL FLOOR; North Pacific/BASIN; North Pacific/CONT RISE; North Pacific/ESCARPMENT; North Pacific/FAN; North Pacific/FLANK; North Pacific/GAP; North Pacific/GUYOT; North Pacific/HILL; North Pacific/Philippine Sea/BASIN; North Pacific/Philippine Sea/CONT RISE; North Pacific/Philippine Sea/RIDGE; North Pacific/PLAIN; North Pacific/PLATEAU; North Pacific/RIDGE; North Pacific/SEAMOUNT; North Pacific/SEDIMENT POND; North Pacific/SLOPE; North Pacific/TERRACE; North Pacific/TRENCH; North Pacific/VALLEY; South Atlantic; South Atlantic/BANK; South Atlantic/BASIN; South Atlantic/CONT RISE; South Atlantic/HILL; South Atlantic/PLATEAU; South Atlantic/RIDGE; South Atlantic/SEAMOUNT; South Atlantic/SYNCLINE; South Atlantic/VALLEY; South Pacific; South Pacific/BASIN; South Pacific/CONT RISE; South Pacific/Coral Sea; South Pacific/Coral Sea/BASIN; South Pacific/Coral Sea/PLATEAU; South Pacific/PLATEAU; South Pacific/RIDGE; South Pacific/Tasman Sea/BASIN; South Pacific/Tasman Sea/CONT RISE
    Type: Dataset
    Format: application/zip, 3 datasets
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  • 4
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    Unknown
    Physical properties measured on 54 sediment cores from METEOR cruise M34/4 (1996)
    PANGAEA
    Details
    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
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  • 5
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    Unknown
    Carbon geochemistry of sediments from the Amazon deep sea fan (1999)
    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
    Details
    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
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  • 6
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    Unknown
    Sedimentology of surface samples from the Weddell Sea, Antarctica (1999)
    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
    Details
    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
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  • 7
    facet.materialart.
    Unknown
    Macrofauna communities in surface sediments in the Amundsen Basin, at the Morris Jesup Rise and at the Yermak Plateau (Eurasian Arctic Ocean) (1998)
    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
    Details
    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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  • 8
    facet.materialart.
    Unknown
    Oceanographic profiles and ice rafted debris in sediments from the Scoresby Sund, Greenland (1996)
    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
    Details
    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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  • 9
    facet.materialart.
    Unknown
    Magnetostratigraphy of sediment cores from the Greenland Sea (1997)
    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
    Details
    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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  • 10
    facet.materialart.
    Unknown
    Ice furrow mapping in the Laptev Sea (1998)
    PANGAEA
    In:  Alfred Wegener Institute, Helmholtz Centre for Polar and Marine Research, Bremerhaven
    Details
    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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