De Geer moraines on German Bank on the southern Scotia Shelf of Atlantic Canada
B.J. TODD1*
1
Geological Survey of Canada, Natural Resources Canada, P.O. Box 1006, Dartmouth, Nova Scotia, Canada B2Y 4A2
*Corresponding author (e-mail:[email protected])
Numerous, regularly-spaced, parallel, linear to curvilinear ridges of
sediment are recognized as forming at or close to the position of the
grounding lines of water-terminating glaciers (Lindén & Möller 2005).
These De Geer moraines are ice-flow transverse features (De Geer 1889)
with modest heights and widths but with variable lengths. The distribution
and pattern of ubiquitous De Geer moraines on German Bank provides
insight into the direction and timing of regional deglaciation of the
southern Scotian Shelf (Todd et al. 2007).
The distribution and pattern of De Geer moraines provides insight into
the subtleties of deglaciation of German Bank. After the Last Glacial
Maximum, the margin of the Laurentide Ice Sheet retreated to the
northwest, punctuated by many small re-advances that formed De Geer
moraines. The pattern of segmented, southeast-convex moraines suggests
that the ice sheet margin was gently scalloped in nature. De Geer moraines
are absent on exposed bedrock but are numerous on thin deposits of
glacially fluted till; between the flutes the moraines are partly to
completely buried by sediment.
Description
The observations on German Bank are consistent with De Geer moraine
formation at the grounding line of a tidewater glacier as a result of
deposition and (or) pushing during minor readvances and stillstands. The
generally regular horizontal spacing of De Geer moraines suggests that the
rate of ice front retreat was consistent from one cycle of formation to the
next. De Geer’s (1889) description of Swedish moraines invoked an annual
cycle. Ottesen & Dowdeswell (2006), in a study based on the interpretation
of multibeam sonar imagery and historical aerial photographs of a
tidewater glacier in a Svalbard fjord setting, provide compelling evidence
that De Geer moraines formed there when the glacier underwent a minor
readvance each winter during its general retreat. However,
sedimentological studies from Scandinavia suggest that several annual
cycles may contribute to the formation of a single De Geer moraine
(Lindén & Möller 2005).
Across a bathymetric range of over 100 m, southern German Bank is
mantled by swarms of ridges; each ridge displays a simple or curved line
in planform (Fig. 1). In topographic lows, the ridges are subdued in relief
or are absent (Fig. 1a). The strike of the ridge crests is generally westsouthwest–east-northeast. Individual ridges can be traced horizontally
from short segments of a few hundred metres up to almost 10 km. Most
ridge crests are simple lines in planform, but in some areas the crests are
complex with bifurcating crest lines and (or) short, en echelon crest
segments. The longer ridge crests are formed of multiple curved sections 2
to 4 km in length with the crests slightly convex toward the southeast. In
places on German Bank, individual ridges traverse bathymetric ranges of
up to 25 m.
The horizontal distance between ridges, normal to strike, is variable. In
some areas, well-defined parallel ridges have a roughly regular spacing of
approximately 150 to 200 m. In other areas, sub-parallel ridges are as
closely spaced as 30 to 50 m.
The ridges vary in height and width. Ridges displaying a subtle
appearance on the large-scale multibeam bathymetry image (Fig. 1b) are
approximately 1.5 m high and 40 m wide. The more prominent ridges are
approximately 5 to 8 m high and 100 to 130 m wide (Fig. 1 c, d). The
ridges are generally symmetrical in cross section with some of the larger
ridges displaying asymmetry with a gentle slope to the north and a steeper
slope to the south (Fig. 1d).
Cobbles and boulders were observed and recovered from ridges and
gravel was recovered from smooth seafloor in troughs (Fig. 1b).
Interpretation
The ridge swarms on German Bank are interpreted to be subaqueous, iceflow transverse De Geer moraines formed at or close to the grounding line
of the southeastern margin of the water-terminating Laurentide Ice Sheet.
Subaerially exposed De Geer moraines have been interpreted as marking
former ice-margin positions where sediment is deposited or pushed up
during brief stillstands or minor readvances (De Geer 1889; Blake 2000),
while an alternative school of thought postulates that De Geer moraines
formed through the squeezing of substrate into basal crevasses behind the
glacier margin (Zilliacus 1989).
Using the traditional marine geophysical survey tools of seismic
reflection profiling and sidescan sonar, De Geer moraines have been
recognized in the Barents Sea (Solheim et al. 1990) and western Norway
(Larsen et al. 1991). In the marine environment, technological constraints
precluded small-scale (i.e. regional) mapping of glacial landforms like De
Geer moraines until the advent of multibeam sonar in the early 1990s.
Applying this technology, De Geer moraines have been mapped on the
Scotian Shelf (Todd et al. 2007), in the Irish Sea (Van Landeghem et al.
2009) and in the North Sea (Bradwell et al. 2008).
References
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From: DOWDESWELL, J.A., CANALS, M., JAKOBSSON, M., TODD, B.J., DOWDESWELL, E.K. & HOGAN, K.A. (eds) Atlas of Submarine Glacial Landforms:
Modern, Quaternary and Ancient. Geological Society, London, Memoirs, xx, 1-2. © The Geological Society of London, 2014. DOI: xx.xxxx/xxx.x.
B.J. TODD
Fig.1. Multibeam sonar bathymetry and geophysical profiles of De Geer moraines on German Bank, Scotian Shelf. (a) Sun-illuminated multibeam bathymetric image
showing De Geer moraines. Acquisition system Kongsberg EM1000. Frequency 95 kHz. Grid-cell size 5 m. (b) Detail multibeam sonar bathymetric image of De Geer
moraines indicating location of geophysical profiles. Yellow dots denote samples; white line denotes video transect (Todd et al., 2007). (c) Sidescan sonar image of De
Geer moraines. Acquisition system Simrad MS992. Frequency 120 kHz. (d) Seismic reflection profile of De Geer moraines. Acquisition system Huntec Deep-Tow
Seismic. Frequency 0.5–8 kHz. The red box on the location map of the Scotian Shelf shows the location of (a); map from IBCAO Version 3.0.