Fluvial incision and channel downcutting as a response to Late-glacial and Early Holocene climate change: the lower reach of the River Meuse (Maas), The Netherlands

Tebbens, L.A.; Veldkamp, A.; Westerhoff, W.E.; Kroonenberg, S.B.

doi:10.1002/(sici)1099-1417(199902)14:1<59::aid-jqs408>3.0.co;2-z

Cited by 71 publications

(39 citation statements)

References 25 publications

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“…We know that climatic changes during the P-H transition triggered sweeping changes in the river systems of northwestern Europe by altering effective moisture, vegetation cover, sediment supply, and permafrost conditions (Frenzel, 1995;Collins et al, 1996;Huisink, 1997;Tebbens et al, 1999;Bridgland, 2000); however, there are no previous studies of how climate change affected fluvial geomorphology on Alaska's North Slope during the P-H transition. Hamilton (1980Hamilton ( , 1982Hamilton ( , 1984 mapped fluvial terraces along the northern front of the Brooks Range, related them to glacial advances of Tertiary and Pleistocene age, and described several stratigraphic sections, 14 C dates from which are incorporated in Appendix C. Dinter et al (1990) mapped fluvial deposits of Cenozoic age on the Arctic Coastal Plain and related episodes of terrace building to times of sea-level high stands.…”

Section: Paleohydrologymentioning

confidence: 74%

Responses of an arctic landscape to Lateglacial and early Holocene climatic changes: the importance of moisture

Mann

Peteet

Reanier³

et al. 2002

Quaternary Science Reviews

117

132

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Many of the physical and biological processes that characterize arctic ecosystems are unique to high latitudes, and their sensitivities to climate change are poorly understood. Stratigraphic records of land-surface processes and vegetation change in the Arctic Foothills of northern Alaska reveal how tundra landscapes responded to climatic changes between 13,000 and 8000 14 C yr BP. Peat deposition began and shrub vegetation became widespread ca. 12,500 14 C yr BP, probably in response to the advent of warmer and wetter climate. Increased slope erosion caused rapid alluviation in valleys, and Populus trees spread northward along braided floodplains before 11,000 14 C yr BP. Lake levels fell and streams incised their floodplains during the Younger Dryas (YD) (11,000-10,000 14 C yr BP). A hiatus in records of Populus suggest that its geographic range contracted, and pollen records of other species suggest a cooler and drier climate during this interval. Basal peats dating to the YD are rare, suggesting that rates of paludification slowed. Immediately after 10,000 14 C yr BP, lake levels rose, streams aggraded rapidly again, intense solifluction occurred, and Populus re-invaded the area. Moist acidic tundra vegetation was widespread by 8500 14 C yr BP along with wet, organic-rich soils. Most of these landscape-scale effects of climatic change involved changes in moisture. Although low temperature is the most conspicuous feature of arctic climate, shifts in effective moisture may be the proximate cause for many of the impacts that climate change has in arctic regions. r

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Section: Paleohydrologymentioning

confidence: 74%

Responses of an arctic landscape to Lateglacial and early Holocene climatic changes: the importance of moisture

Mann

Peteet

Reanier³

et al. 2002

Quaternary Science Reviews

117

132

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“…It is uncertain how many Middle Pleniglacial and older levels are present in the data. In the eastern part of the Maaskant, the level can be followed upstream to Pleniglacial and older levels found in the Meuse Valley (Huisink, 1999b;Tebbens et al, 1999). Downstream in the central Maaskant area, pre-Weichselian fluvial deposits locally form the higher terrace level.…”

Section: Reconstruction Of Late Weichselian Palaeogeographymentioning

confidence: 77%

“…Therefore our age control for the four recognized terrace levels is based on stratigraphic correlation. Upstream in the Meuse valley a very similar series of four terraces is found (Huisink, 1997(Huisink, , 1999aTebbens et al, 1999) and well dated. Our age estimates are based on the very similar lithostratigraphy of the terraces in that region.…”

Section: Reconstruction Of Late Weichselian Palaeogeographymentioning

confidence: 99%

“…The Meuse fluvial pattern changed from braided during the Late Pleniglacial to meandering in the Bølling-Allerød interstadial, to braided during the Younger Dryas stadial, and back again to meandering in the Early Holocene (Huisink, 1997;Tebbens et al, 1999). Similar changes are reported for the Rhine Valley and are inferred from deposits in the subsurface of the RhineMeuse delta, although the fluvial style of Lateglacial rivers in the western part of the delta has never been established with certainty.…”

Section: The Rhine-meuse Delta In the Late Weichselian And The Holocenementioning

confidence: 99%

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Fluvial deposits as a record for Late Quaternary neotectonic activity in the Rhine-Meuse delta, The Netherlands

Cohen

Stouthamer

Berendsen

2002

Netherlands Journal of Geosciences

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Neotectonic movements have caused differential subsidence in the Lower Rhine Embayment during the Quaternary. The Late Weichselian and Holocene Rhine-Meuse fluvial archive in the central Netherlands was used to quantify neotectonic movements in a setting that was primarily controlled by sea-level rise and climate change. Evidence for neotectonic activity in the central Netherlands is reviewed. Sedimentary evidence shows that fluvial deposits of Late Weichselian and Holocene Rhine and Meuse (Maas) distributaries are vertically displaced along the northern shoulder of the Roer Valley Graben system. Elevation differences in the longitudinal profiles of Late Weichselian terrace deposits were used to quantify tectonic displacements. New results for the southeastern Rhine-Meuse delta (Maaskant area) show that displacements in the top of the Pleniglacial terrace along the Peel Boundary Fault are up to 1.4 m. The maximum displacement between the Peel Horst and the Roer Valley Graben is 2.3 m. This is equivalent to relative tectonic movement rates of 0.09-0.15 mm/yr, averaged over the last 15,000 years.

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“…Berendsen et al, 1995;Kasse et al, 1995;Huisink, 1997;Tebbens et al, 1999;Erkens et al, 2011). This is particularly true for those Rhine valleys that were abandoned at the start of the Holocene: the valley of the local river Oude IJssel and the valley of the Niers, on either side of the modern Rhine (Fig.…”

mentioning

confidence: 99%

Climate-driven fluvial development and valley abandonment at the last glacial-interglacial transition (Oude IJssel-Rhine, Germany)

Janssens

Kasse

Bohncke

et al. 2012

Netherlands Journal of Geosciences

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Although numerous studies have been performed on fluvial system change over the last glacial-interglacial transition, the response of river systems to allogenic (climate) and autogenic forcing mechanisms and timing of this response are still not completely understood (e.g. Starkel, 1983;Vandenberghe et al., 1995;Rose, 1995;Blum & Törnqvist, 2000;Gibbard & Lewin, 2002;Vandenberghe, 2008;Erkens, 2009). The valleys of the Rhine and the Maas in the Lower Rhine Embayment have a long research history on this topic (Pons,1957;Van de Meene, 1977;Verbraeck, 1984;Klostermann, 1992;Schirmer, 1995;Berendsen & Stouthamer, 2001;Cohen et al., 2002;Busschers et al., 2007;Erkens et al., 2011). In this area, a well-preserved terraced morphology exists, with OSL-datable fluvial sequences with aeolian cover and with palaeochannel fills that allow vegetation AbstractIn the Weichselian, the Lower Rhine in the Dutch-German border region has used three courses, dissecting ice-marginal topography inherited from the Saalian. In the Late Weichselian, the three courses functioned simultaneously, with the central one gaining importance and the outer ones abandoning. This study aims to reconstruct the fluvial development and forcings that culminated in abandonment of the northern branch 'Oude IJssel-Rhine', at the time of the Lateglacial to Holocene transition. The fluvial architecture is studied using a cored transect over the full width of the valley, detailed cross-sections over palaeochannels and geomorphological analysis using digital elevation and borehole data. Biostratigraphy, radiocarbon dating and OSL dating provide a timeframe to reconstruct the temporal fluvial development. In its phase of abandonment, the fluvial evolution of the Oude IJssel-Rhine course is controlled by the ameliorating climate and related vegetation and discharge changes, besides by intrinsic (autogenic) fluvial behaviour such as the competition for discharge with the winning central branch and the vicinity of the Lippe tributary confluence. The rapid climate warming at the start of the Late Glacial resulted in flow contraction as the initial response. Other fluvial geomorphic adjustments followed, with some delay. An aggrading braided or transitional system persisted until the start of the Allerød, when channel patterns finally changed to meandering. Floodplain incision occurred at the Allerød -Younger Dryas transition and a multi-channel system developed fed by Rhine discharge. At the start of the Holocene, this system transformed into a small-scale, local meandering system, which was abandoned shortly after the start of the Holocene.The final abandonment of the Oude IJssel-Rhine and Niers-Rhine courses can be attributed to deep incision of the Central Rhine course in the earliest Holocene and is considered to be controlled by flow contraction induced by climate and related vegetation and discharge changes.

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Fluvial incision and channel downcutting as a response to Late-glacial and Early Holocene climate change: the lower reach of the River Meuse (Maas), The Netherlands

Cited by 71 publications

References 25 publications

Responses of an arctic landscape to Lateglacial and early Holocene climatic changes: the importance of moisture

Responses of an arctic landscape to Lateglacial and early Holocene climatic changes: the importance of moisture

Fluvial deposits as a record for Late Quaternary neotectonic activity in the Rhine-Meuse delta, The Netherlands

Climate-driven fluvial development and valley abandonment at the last glacial-interglacial transition (Oude IJssel-Rhine, Germany)

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