Ice‐marginal debris‐flow deposits in western Allgau, southern West Germany

Jong, M.G.G. de; Rappol, Martin

doi:10.1111/j.1502-3885.1983.tb00360.x

Cited by 15 publications

(3 citation statements)

References 15 publications

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“…10.3). These are classic features for identification of kame terraces occurring in various glaciated regions, as noted by Klimek (1956), John (1972), Huddart andLister (1981), de Jong andRappol (1983), Bitinas et al (2004), Pisarska-Jamrozy et al (2010), and Dauškans (2013). Fig.…”

mentioning

confidence: 87%

STOP 10: Kame terrace in the Upper Daugava depression at Rakuti, near Krāslava

Zelčs¹,

Soms²,

Greiškalns³

2014

Late Quaternary Terrestrial Processes, Sediments and History: From Glacial to Postglacial Environments

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mentioning

confidence: 87%

STOP 10: Kame terrace in the Upper Daugava depression at Rakuti, near Krāslava

Zelčs¹,

Soms²,

Greiškalns³

2014

Late Quaternary Terrestrial Processes, Sediments and History: From Glacial to Postglacial Environments

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“…Past research focused on sedimentological composition of drumlins as well as drumlin distribution and morphology (Bodenburg Hellmund, 1909; Brückner, 1886; de Jong, 1983; Ebers, 1926, 1960; Ellwanger, 1990, 1994; Früh, 1904; German, 1977; Glückert, 1974; Grünvogel, 1953; Habbe, 1988, 1989, 1992; Schreiner, 1976). Alpine drumlins contain a range of unconsolidated sediments (till, gravel, gravel mantled by or interbedded with till, deltaic sediment and ice marginal sediment) and also can be cored by Molasse bedrock (Brauhäuser, 1976; de Jong, 1983; Ellwanger, 1990, 1992; Erb, 1986; Grünvogel, 1953; Habicht et al, 1986; Saxer, 1965; Schmidle, 1914, 1916; Schmidt & Münst, 1979; Schreiner, 1976; Zaugg & Geyer, 2008). Geomorphological maps of single drumlin fields have been published (Früh, 1904; Grünvogel, 1954; Habbe, 1989), and geological map sheets partially delineate drumlins.…”

Section: Introductionmentioning

confidence: 99%

“…Past research focused on sedimentological composition of drumlins as well as drumlin distribution and morphology (Bodenburg Hellmund, 1909;Brückner, 1886;de Jong, 1983;Ebers, 1926Ebers, , 1960Ellwanger, 1990Ellwanger, , 1994Früh, 1904;German, 1977;Glückert, 1974;Grünvogel, 1953;Habbe, 1988Habbe, , 1989Habbe, , 1992Schreiner, 1976). Alpine drumlins contain a range of unconsolidated sediments (till, gravel, gravel mantled by or interbedded with till, deltaic sediment and ice marginal sediment) and also can be cored by Molasse bedrock (Brauhäuser, 1976;de Jong, 1983;Ellwanger, 1990Ellwanger, , 1992Erb, 1986;Grünvogel, 1953;Habicht et al, 1986;Saxer, 1965;Schmidle, 1914Schmidle, , 1916Schmidt & Münst, 1979;Schreiner, 1976;. Geomorphological maps of single drumlin fields have been published (Früh, 1904;Grünvogel, 1954;Habbe, 1989), and geological map sheets partially delineate drumlins.…”

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confidence: 99%

Reconstructing basal ice flow patterns of the Last Glacial Maximum Rhine glacier (northern Alpine foreland) based on streamlined subglacial landforms

Kamleitner,

Ivy‐Ochs,

Salcher

et al. 2023

Earth Surf Processes Landf

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Based on high‐resolution (sub)glacial geomorphological mapping, we present a first digital inventory of streamlined bedforms within the footprint of a Last Glacial Maximum (LGM) Alpine piedmont glacier. A total of 2460 drumlins were mapped across the Rhine glacier foreland. Glacial lineations and one field of subglacial ribs (ribbed/Rogen moraines) — the first record of this type of subglacial landform on the Alpine foreland—were identified. Two flowsets, associated with (i) the Rhine glacier's LGM maximum advance (Schaffhausen stadial) and (ii) a late LGM readvance (Stein am Rhein stadial), are differentiated. The vast majority of streamlined bedforms occur in fields aligned in a 16‐ to 30‐km‐wide swath upstream of the Stein am Rhein frontal moraines. Orientation and elongation of drumlins and glacial lineations set the basis for the reconstruction of paleo‐ice flow. Basal flow paths of the LGM maximum advance are visually interpreted and restricted to the zone proximal to the former ice front. The flow field reconstructed for the late LGM glacier readvance (Stein am Rhein stadial) extends tens of kilometres upstream and is modelled implementing a recently published kriging routine. The derived basal flow patterns paired with information on ice surface levels from lateral and frontal moraines and combined with relative ice velocity differences inferred from spatial changes in bedform elongation reveal detailed insights on ice flow geometries, particularly during the glacier readvance. Reconstructed flowlines highlight basal flow under shallow ice that is strongly controlled by local topography evidenced by diverging around basal bumps and converging in (narrow) valley sections and troughs, where basal flow velocities, steered by topography, are high. Gained paleo‐ice basal flow patterns offer new insights on landscape evolution of the northern Alpine foreland and provide evidence‐based flow data to validate future physical modelling results.

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Pattern of deglaciation of the last (Late Devensian) Scottish ice sheet: Evidence from ice‐marginal deposits in the Dee valley, Northeast Scotland

Brown

1993

J Quaternary Science

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Brown, 1. M. Pattern of deglaciation of the last (Late Devensian) Scottish ice sheet: evidence from ice-marginal deposits in the Dee valley, northeast Scotland lournaf ABSTRACT: The mode of deglaciation of the last Scottish ice sheet is assessed from evidence provided by geomorphological mapping and sedimentology. ice-marginal deposits in the Dee valley have a distinctive morphological expression and a characteristically varied sedimentology that strongly resembles those from subpolar glaciers. The deposits tend to occur in certain topographic situations which can be accounted for by compression of ice near the margin and formation of an ice-cored supraglacial land system. A series of recessional stages of the ice-front can be mapped demonstrating that active retreat occurred. However, additional evidence shows there was probably a thin marginal zone of stagnant ice. Recessional stages are inferred to be stillstands that are considered to be topographically controlled rather than related to climate. Development of the supraglacial land system during deglaciation suggests that the ice sheet had a polythermal basal regime with a cold-based margin. This implies that deglaciation took place in northeast Scotland while the climate remained cold, probably due to a precipitation deficit, which agrees well with chronostratigraphic data. J w r m I of Quaternary Science

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Ice‐marginal debris‐flow deposits in western Allgau, southern West Germany

Cited by 15 publications

References 15 publications

STOP 10: Kame terrace in the Upper Daugava depression at Rakuti, near Krāslava

STOP 10: Kame terrace in the Upper Daugava depression at Rakuti, near Krāslava

Reconstructing basal ice flow patterns of the Last Glacial Maximum Rhine glacier (northern Alpine foreland) based on streamlined subglacial landforms

Pattern of deglaciation of the last (Late Devensian) Scottish ice sheet: Evidence from ice‐marginal deposits in the Dee valley, Northeast Scotland

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