X-ray diffraction analysis, binocular component analysis and radiocarbon dating of sediment cores from the NW Iberian shelf system
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| Natura: | Dataset Open Access |
| Lingua: | en |
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PANGAEA
2010
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| _version_ | 1867169501596876800 |
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| author | Lantzsch, Hendrik Hanebuth, Till J J Henrich, Rüdiger |
| author_facet | Lantzsch, Hendrik Hanebuth, Till J J Henrich, Rüdiger |
| collection | Datos científicos de ciencias marinas y ambientales |
| contents | Based on a well-established stratigraphic framework and 47 AMS-14C dated sediment cores, the distribution of facies types on the NW Iberian margin is analysed in response to the last deglacial sea-level rise, thus providing a case study on the sedimentary evolution of a high-energy, low-accumulation shelf system. Altogether, four main types of sedimentary facies are defined. (1) A gravel-dominated facies occurs mostly as time-transgressive ravinement beds, which initially developed as shoreface and storm deposits in shallow waters on the outer shelf during the last sea-level lowstand; (2) A widespread, time-transgressive mixed siliceous/biogenic-carbonaceous sand facies indicates areas of moderate hydrodynamic regimes, high contribution of reworked shelf material, and fluvial supply to the shelf; (3) A glaucony-containing sand facies in a stationary position on the outer shelf formed mostly during the last-glacial sea-level rise by reworking of older deposits as well as authigenic mineral formation; and (4) A mud facies is mostly restricted to confined Holocene fine-grained depocentres, which are located in mid-shelf position. The observed spatial and temporal distribution of these facies types on the high-energy, low-accumulation NW Iberian shelf was essentially controlled by the local interplay of sediment supply, shelf morphology, and strength of the hydrodynamic system. These patterns are in contrast to high-accumulation systems where extensive sediment supply is the dominant factor on the facies distribution. This study emphasises the importance of large-scale erosion and material recycling on the sedimentary buildup during the deglacial drowning of the shelf. The presence of a homogenous and up to 15-m thick transgressive cover above a lag horizon contradicts the common assumption of sparse and laterally confined sediment accumulation on high-energy shelf systems during deglacial sea-level rise. In contrast to this extensive sand cover, laterally very confined and maximal 4-m thin mud depocentres developed during the Holocene sea-level highstand. This restricted formation of fine-grained depocentres was related to the combination of: (1) frequently occurring high-energy hydrodynamic conditions; (2) low overall terrigenous input by the adjacent rivers; and (3) the large distance of the Galicia Mud Belt to its main sediment supplier. |
| format | Dataset Open Access |
| id | pangaea_https___doi_org_10_1594_PANGAEA_743922 |
| institution | PANGAEA |
| language | en |
| publishDate | 2010 |
| publisher | PANGAEA |
| record_format | pangaea |
| spellingShingle | X-ray diffraction analysis, binocular component analysis and radiocarbon dating of sediment cores from the NW Iberian shelf system Lantzsch, Hendrik Hanebuth, Till J J Henrich, Rüdiger 205-1; 205-2; 207-2; 207-3; 212-1; 212-2; 213-1; 213-2; 216-1; 216-2; Center for Marine Environmental Sciences; GC; GeoB11001-2; GeoB11001-3; GeoB11002-1; GeoB11002-3; GeoB11003-2; GeoB11003-3; GeoB11004-1; GeoB11004-2; GeoB11005-1; GeoB11005-2; GeoB11007-1; GeoB11007-2; GeoB11008-1; GeoB11008-2; GeoB11009-1; GeoB11009-2; GeoB11010-1; GeoB11010-2; GeoB11011-1; GeoB11011-2; GeoB11012-1; GeoB11012-2; GeoB11013-1; GeoB11013-2; GeoB11014-1; GeoB11014-2; GeoB11015-2; GeoB11016-1; GeoB11016-2; GeoB11017-1; GeoB11017-2; GeoB11018-1; GeoB11018-2; GeoB11019-1; GeoB11019-2; GeoB11020-1; GeoB11020-2; GeoB11022-1; GeoB11025-1; GeoB11025-2; GeoB11027-1; GeoB11027-2; GeoB11028-1; GeoB11028-2; GeoB11029-1; GeoB11029-2; GeoB11030-1; GeoB11030-2; GeoB11031-1; GeoB11031-2; GeoB11032-1; GeoB11036-1; GeoB11036-2; GeoB11037-1; GeoB11038-1; GeoB11038-2; GeoB11039-1; GeoB11039-3; GeoB11040-1; GeoB11040-2; GeoB11041-1; GeoB11041-2; GeoB11042-1; GeoB11042-2; GeoB11043-1; GeoB11043-2; GeoB11044-1; GeoB11045-1; GeoB11046-1; GeoB130205-1; GeoB130205-2; GeoB130207-2; GeoB130207-3; GeoB130212-1; GeoB130212-2; GeoB130213-1; GeoB130213-2; GeoB130216-1; GeoB130216-2; GeoB13039-5; GeoB13041-1; GeoB13041-2; GeoB13043-1; GeoB13045-1; GeoB13046-1; GeoB13046-2; GeoB13047-1; GeoB13047-2; GeoB13048-1; GeoB13048-2; GeoB13049-1; GeoB13049-2; GeoB13050-1; GeoB13050-2; GeoB13051-1; GeoB13051-2; GeoB13052-1; GeoB13052-2; GeoB13088-1; GeoB13088-2; GeoB13089-1; GeoB13089-2; Giant box corer; GKG; Gravity corer; MARUM; POS342; POS366/3; Poseidon; VC; Vibro corer Based on a well-established stratigraphic framework and 47 AMS-14C dated sediment cores, the distribution of facies types on the NW Iberian margin is analysed in response to the last deglacial sea-level rise, thus providing a case study on the sedimentary evolution of a high-energy, low-accumulation shelf system. Altogether, four main types of sedimentary facies are defined. (1) A gravel-dominated facies occurs mostly as time-transgressive ravinement beds, which initially developed as shoreface and storm deposits in shallow waters on the outer shelf during the last sea-level lowstand; (2) A widespread, time-transgressive mixed siliceous/biogenic-carbonaceous sand facies indicates areas of moderate hydrodynamic regimes, high contribution of reworked shelf material, and fluvial supply to the shelf; (3) A glaucony-containing sand facies in a stationary position on the outer shelf formed mostly during the last-glacial sea-level rise by reworking of older deposits as well as authigenic mineral formation; and (4) A mud facies is mostly restricted to confined Holocene fine-grained depocentres, which are located in mid-shelf position. The observed spatial and temporal distribution of these facies types on the high-energy, low-accumulation NW Iberian shelf was essentially controlled by the local interplay of sediment supply, shelf morphology, and strength of the hydrodynamic system. These patterns are in contrast to high-accumulation systems where extensive sediment supply is the dominant factor on the facies distribution. This study emphasises the importance of large-scale erosion and material recycling on the sedimentary buildup during the deglacial drowning of the shelf. The presence of a homogenous and up to 15-m thick transgressive cover above a lag horizon contradicts the common assumption of sparse and laterally confined sediment accumulation on high-energy shelf systems during deglacial sea-level rise. In contrast to this extensive sand cover, laterally very confined and maximal 4-m thin mud depocentres developed during the Holocene sea-level highstand. This restricted formation of fine-grained depocentres was related to the combination of: (1) frequently occurring high-energy hydrodynamic conditions; (2) low overall terrigenous input by the adjacent rivers; and (3) the large distance of the Galicia Mud Belt to its main sediment supplier. |
| title | X-ray diffraction analysis, binocular component analysis and radiocarbon dating of sediment cores from the NW Iberian shelf system |
| topic | 205-1; 205-2; 207-2; 207-3; 212-1; 212-2; 213-1; 213-2; 216-1; 216-2; Center for Marine Environmental Sciences; GC; GeoB11001-2; GeoB11001-3; GeoB11002-1; GeoB11002-3; GeoB11003-2; GeoB11003-3; GeoB11004-1; GeoB11004-2; GeoB11005-1; GeoB11005-2; GeoB11007-1; GeoB11007-2; GeoB11008-1; GeoB11008-2; GeoB11009-1; GeoB11009-2; GeoB11010-1; GeoB11010-2; GeoB11011-1; GeoB11011-2; GeoB11012-1; GeoB11012-2; GeoB11013-1; GeoB11013-2; GeoB11014-1; GeoB11014-2; GeoB11015-2; GeoB11016-1; GeoB11016-2; GeoB11017-1; GeoB11017-2; GeoB11018-1; GeoB11018-2; GeoB11019-1; GeoB11019-2; GeoB11020-1; GeoB11020-2; GeoB11022-1; GeoB11025-1; GeoB11025-2; GeoB11027-1; GeoB11027-2; GeoB11028-1; GeoB11028-2; GeoB11029-1; GeoB11029-2; GeoB11030-1; GeoB11030-2; GeoB11031-1; GeoB11031-2; GeoB11032-1; GeoB11036-1; GeoB11036-2; GeoB11037-1; GeoB11038-1; GeoB11038-2; GeoB11039-1; GeoB11039-3; GeoB11040-1; GeoB11040-2; GeoB11041-1; GeoB11041-2; GeoB11042-1; GeoB11042-2; GeoB11043-1; GeoB11043-2; GeoB11044-1; GeoB11045-1; GeoB11046-1; GeoB130205-1; GeoB130205-2; GeoB130207-2; GeoB130207-3; GeoB130212-1; GeoB130212-2; GeoB130213-1; GeoB130213-2; GeoB130216-1; GeoB130216-2; GeoB13039-5; GeoB13041-1; GeoB13041-2; GeoB13043-1; GeoB13045-1; GeoB13046-1; GeoB13046-2; GeoB13047-1; GeoB13047-2; GeoB13048-1; GeoB13048-2; GeoB13049-1; GeoB13049-2; GeoB13050-1; GeoB13050-2; GeoB13051-1; GeoB13051-2; GeoB13052-1; GeoB13052-2; GeoB13088-1; GeoB13088-2; GeoB13089-1; GeoB13089-2; Giant box corer; GKG; Gravity corer; MARUM; POS342; POS366/3; Poseidon; VC; Vibro corer |
| url | https://doi.org/10.1594/PANGAEA.743922 |