Dittmers, Klaus Hauke; Niessen, Frank; Stein, Ruediger (2008): Late Weichselian fluvial evolution of the southern Kara Sea. PANGAEA, https://doi.org/10.1594/PANGAEA.738340, Supplement to: Dittmers, KH et al. (2008): Late Weichselian Fluvial Evolution on the Southern Kara Sea Shelf, North Siberia. Global and Planetary Change, 60(3-4), 327-350, https://doi.org/10.1016/j.gloplacha.2006.12.006
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Glaciations had a profound impact on the global sea-level and particularly on the Arctic environments. One of the key questions related to this topic is, how did the discharge of the Siberian Ob and Yenisei rivers interact with a proximal ice sheet? In order to answer this question high-resolution (1-12 kHz), shallow-penetration seismic profiles were collected on the passive continental margin of the Kara Sea Shelf to study the paleo-drainage pattern of the Ob and Yenisei rivers. Both rivers incised into the recent shelf, leaving filled and unfilled river channels and river canyons/valleys connecting to a complex paleo-drainage network.
These channels have been subaerially formed during a regressive phase of the global sea-level during the Last Glacial Maximum. Beyond recent shelf depths of 120 m particle transport is manifested in submarine channel-levee complexes acting as conveyor for fluvial-derived fines. In the NE area, uniform draping sediments are observed. Major morphology determining factors are (1) sea-level fluctuations and (2) LGM ice sheet influence. Most individual channels show geometries typical for meandering rivers and appear to be an order of magnitude larger than recent channel profiles of gauge stations on land.
The Yenisei paleo-channels have larger dimensions than the Ob examples and could be originated by additional water release during the melt of LGM Putoran ice masses.
Asymmetrical submarine channel-levee complexes with channel depths of 60 m and more developed, in some places bordered by glacially dominated morphology, implying deflection by the LGM ice masses. A total of more than 12,000 km of acoustic profiles reveal no evidence for an ice-dammed lake of greater areal extent postulated by several workers. Furthermore, the existence of the channel-levee complexes is indicative of unhindered sediment flow to the north. Channels situated on the shelf above 120-m water depth exhibit no phases of ponding and or infill during sea-level lowstand. These findings denote the non-existence of an ice sheet on large areas of the Kara Sea shelf.
Dittmers, Klaus Hauke (2006): Late Weichselian to Holocene sedimentation in the inner Kara Sea: Qualification and Quantification of Processes. Berichte zur Polar- und Meeresforschung = Reports on Polar and Marine Research, 523, 185 pp, https://doi.org/10.2312/BzPM_0523_2006
Median Latitude: 75.491299 * Median Longitude: 77.161987 * South-bound Latitude: 72.520000 * West-bound Longitude: 66.420000 * North-bound Latitude: 77.910000 * East-bound Longitude: 89.360000
Datasets listed in this publication series
- Dittmers, KH; Niessen, F; Stein, R (2005): Geometry and morphology of Channel-levee complexes. https://doi.org/10.1594/PANGAEA.338931
- Dittmers, KH; Niessen, F; Stein, R (2005): Geometry and morphology of buried channels (Typ I). https://doi.org/10.1594/PANGAEA.338932
- Dittmers, KH; Niessen, F; Stein, R (2005): Geometry and morphology of the paleo-Ob River channels (Typ II). https://doi.org/10.1594/PANGAEA.338934
- Dittmers, KH; Niessen, F; Stein, R (2005): Geometry and morphology of the paleo-Yenisei River channels (Typ II). https://doi.org/10.1594/PANGAEA.338933