Reconstructing the extent, flow and decay of the Laurentide Ice Sheet (LIS) on the continental shelves of North America during the last glaciation provides paleoglaciological analogues that are essential for understanding and predicting how modern marine-based ice-sheets will respond to future climate change and sea level fluctuations. The geometry of the LIS during Marine isotope stage 2 (MIS-2; 29–14 ka BP) is one key element for ice-sheet modelling. The maximum extent of the LIS during this stage is well constrained for most sectors of the ice sheet, but major uncertainties remain, especially along the continental shelves of Arctic Canada. Despite a series of recent papers, the extent of the LIS in Western Baffin Bay, an area draining large volumes of glacial ice through multiple ice streams and likely characterized by ice shelves, remains highly speculative. Here we present unequivocal marine geophysical evidence that during the MIS-2 the LIS extended to the edge of the continental shelf, seaward of the previously proposed limits and subsequently retreated episodically westward during deglaciation. These data support interpretations of deep glacial ice grounding in Western Baffin Bay.
The maximum extent of the LIS in Western Baffin Bay during MIS-2 has been a subject of debate for decades and brought different glaciation scenarios oscillating between extensive single dome LIS reaching the edge of the continental shelf 1 and a minimal ice hypothesis where the LIS only reached the fjords head2, 3. The Flint (extensive) scenario1 was supported by modelling4 but, however, lacked field data while the minimalist scenario has been challenged by recent dating of moraines5, 6 and by the identification of terrain preserved under cold-based ice on coastal forelands7, 8. Cosmogenic nuclides exposure dating on terrestrial moraines as well as lacustrine and marine sediment cores data were used to resolve the enigma of the maximum extent of the LIS by proposing a scenario where most of LIS outlet glaciers reached the continental shelf at fjord mouths, with ice margins terminating inland in-between fjords (i.e., the Goldilocks Paradigm)9. This interpretation was largely used in most paleogeographical reconstructions and in ice-sheet modelling studies10,11,12,13,14,15. More recent studies have, however, challenged this model, suggesting a more extensive LIS margin on the northeastern Baffin Island shelf during the Last Glacial Maximum (LGM) based on the observation of (1) an ice-contact seismostratigraphic unit extending on most of the continental shelf (the Baffin Shelf Drift16) and (2) a till wedge at 1300 m water depths at the southeast end of Lancaster Sound deposited at the ice grounding-zone17 (Fig. 1). Therefore, new constraints are needed to enable a more rigorous representation of the LIS extent in the region in order to improve the detail of paleoglaciological models. Swath bathymetry imagery collected over a period of 13 years during scientific expeditions onboard the CCGS Amundsen combined with archived seismic reflection data from the Geological Survey of Canada are used here to map submarine glacial landforms in order to reconstruct the extent, flow and retreat of the LIS margin on the northeast Baffin Island shelf during MIS-2.
Cross-shelf troughs and ice-flow features
Four cross-shelf troughs that were glacially eroded and moulded during Quaternary glaciations16, 18 are observed offshore major fjord systems of northeastern Baffin Island: Pond, Buchan, Scott and Sam Ford troughs (Fig. 1A). These major submarine valley systems alone, however, do not provide unequivocal evidence for ice-flow during last glacial cycle, as they mostly reflect a long-term record of repeated stages of glacial erosion that probably occurred since the Pliocene. Nonetheless, assemblages of smaller-scale ice-flow landforms are observed within Buchan, Scott and Pond troughs on the swath bathymetry imagery. Ice-flow morphologies include mega-scale glacial lineations (MSGLs), ice stream lateral moraines (ISLMs), medial moraines, crag-and-tails, drumlins, meltwater channels and grooves19, 20 (Figs 1 B and 2). MSGLs are indicators of fast ice-flow and are a common and unequivocal signature of ice stream activity21, 22. These elongated landforms (>450 m lengths; <250 m widths; elongation ratios >10:1) are aligned in the trough axis and have low amplitudes (<20 m). Their very good state of preservation and the weak attenuation of their morphology due to a thin cover of postglacial sediments suggest that they relate to the last stage of ice occupation. Crosscut by grounding-zone wedges, MSGLs are interpreted to reflect time-transgressive ice-flows occurring during the landward retreat of an ice stream. In Pond and Scott troughs, MSGLs extend onto the shelf break (Figs 1 B and 2), while in Buchan Trough, the lack of extensive swath bathymetry coverage makes it difficult to determine the seaward extent of the MSGLs (Fig. 2B). A small set of MSGLs lies at ~1100 m present-day water depths some 75 km east of Pond Trough (Fig. 1B). These landforms are oriented (ESE) towards the grounding-zone deposit interpreted by Li et al. (2011) as the limit of the LIS margin during MIS-2.
Grounding-zones wedges at the ice margin
Grounding-zone wedges (GZWs) are formed by the accumulation of subglacial sediments at the grounding zone of an ice stream during temporary standstills of an ice margin e.g. 23,24,25. GZWs have been associated with the presence of ice shelves24 which restricts vertical accommodation space for sediments in favor of sediment progradation, leading to the formation of low-amplitude and horizontally extensive landforms (i.e., GZWs)23. GZWs are observed in the four studied troughs from swath bathymetry imagery and/or seismic data (Figs 1 B, 2 and 3A). On swath bathymetry imagery, GZWs form asymmetric tabular topographic highs that are perpendicularly aligned to trough orientations and characterized by stoss sides with lower gradients (Fig. 3A). On seismic reflection profiles, most of the GZWs consist of acoustically semi-transparent to chaotic wedge-shaped deposits overlain by thin unit of high-amplitude parallel reflections (Fig. 3A). The transparent to chaotic acoustic unit is interpreted as diamictic debris, mainly from a sub-ice stream deformable till layer26,27,28,29 delivered to the grounding zone during a period of ice margin stabilization24. GZWs are conformably covered by a thin sediment drape (6–8 m) that is coherent with postglacial sedimentation rates observed in Scott Trough16. Also, all the GZWs observed in Scott, Buchan and Pond troughs overprint sets of MSGLs formed during a previous phase of ice-flow (Fig. 2). They are therefore interpreted to reflect episodic phases of ice margin stabilization during deglaciation rather than a maximum position30.
Trough-mouth fans and glacigenic debris flows
At the shelf edge of Scott Trough, MSGLs terminate at the head of a 17 by 42 km-wide fan-shaped bathymetric bulge interpreted as a trough-mouth fan (TMF)17, 31,32,33. TMFs generally consist of stacked acoustically transparent lenses of glacigenic-debris flows (GDFs) separated by acoustically stratified units representing suspension-settling sediments, turbidites and/or contourites34,35,36,37. GDFs are mostly the product of instabilities at the grounding zone during the occupation of the trough by an ice stream, while the stratified units relate to deglacial to interglacial conditions17, 38,39,40,41,42,43. Stacked GDFs interbedded with stratified units observed on seismic reflection profiles in Scott Trough could represent such a succession of glacial debris flows and interglacial sedimentation, but of unknown age (Fig. 3B). At the distal end of the trough, an erosional surface truncates the upper stacked GDFs. This surface is overlain by an acoustically semi-transparent unit interpreted as till, which is itself overlain by a thin unit (~6–8 m) of high amplitude parallel reflections interpreted as glaciomarine and hemipelagic sediments16. The erosional surface and the above sediment sequence indicate a glacial advance followed by deglacial to postglacial sedimentation. This sequence is also observed in the outer sector of Buchan Trough in a similar 18 by 44 km TMF. No similar bathymetric bulge is present at the mouth of Pond Trough, as the latter ends abruptly at its junction with Bylot Trough. Seismic reflection data also show stacked GDFs at the southern end of the Bylot Trough on the Lancaster Fan, just east of Cape Jameson Bank (Fig. 3C). A hummocky terrain and undulating ridges are identified at the shelf edge on Scott TMF (Fig. 2A). These landforms are similar to ‘lift-off moraines’ and could reflect temporary stabilisation of the grounding-zone of a tidally influenced ice margin44. Consequent with the extent of the till unit on the TMF, these ridges probably reflect the maximal extent of the LIS margin in Scott Trough.
Ice stream lateral moraines
Ice stream lateral moraines (ISLMs) indicate fast-flowing ice surrounded by either slower ice-flow or ice-free terrain45, 46. Multiple ISLMs are observed on both sides of Buchan and Scott troughs (Fig. 1B and 2), forming >40 km linear ridges with a relief reaching 120 m. On seismic reflection profiles, the outer-trough moraines show prograding internal reflections dipping away from the trough (Fig. 3D). This dipping architecture within the outer-trough ISLMs reflects horizontal sediment progradation, in a similar way to GZWs formation47. Sediment progradation therefore indicates the absence of horizontal constraints (i.e., grounded ice) on the outer continental shelf. Similarly to GZWs it could also indicate the presence of a constraint for vertical accumulation (i.e., ice shelf)47.
Ice-contact sediments on the continental shelf
Swath bathymetry imagery reveals ridges parallel to the shelf break on the banks seaward of Cape Adair (Fig. 1B). These ridges consist of acoustically semi-transparent sediment bodies overlain by a thin (<10 m) unit of high amplitude parallel reflections (Fig. 3E). Based on their architecture and amplitude, these ridges are interpreted as ice-contact fans or moraine ridges typical of tidewater glaciers on high-latitude continental shelves48. The chaotic acoustically semi-transparent unit extends laterally from the ridges and parallel to the shelf break; it is interpreted as ice-contact sediments correlated to the Baffin Shelf Drift16.
Extent of the Laurentide Ice Sheet
Position and timing
Ice-contact landforms and deposits mapped on the northeastern Baffin Island continental shelf allow reconstructing the configuration of the maximum extent of the LIS during MIS-2. In Scott and Buchan troughs, the presence of MSGLs extending to the shelf break, together with a till unit extending on the TMFs, indicate that the LIS reached the shelf break during the last glacial episode (Fig. 4). The GZWs observed in the troughs are located landward from the maximal extent of the LIS at the shelf edge. Therefore, they are interpreted to have been constructed during phases of standstill of the westward episodically retreating LIS margin. MSGLs mapped in Pond Trough reach Bylot Trough, but the absence of a depocenter (TMF) indicates that the LIS extended farther in this area. The LIS grounding-zone at the end of Lancaster Sound9 is located ~100 km eastward from the MSGLs terminus. Ice flowing through Pond Trough likely converged into the Lancaster Ice Stream in Bylot Trough and from there flowed eastward to reach the LGM grounding-zone on the Lancaster TMF17. Subglacial sediments delivered to Bylot Trough by the Pond Trough ice stream would have been taken in charge by Lancaster ice that fed the Lancaster Fan. In Sam Ford Trough, GZWs constructed from the same till/ice-contact seismic unit in both Buchan and Scott troughs extends at least to the middle of Sam Ford Trough to form a distinct transverse-to-flow ridge (Fig. 1B). This northeast GZW is the farthest confirmed position of the LIS in Sam Ford cross-shelf trough. It cannot be ruled out, however, that the LIS margin reached the shelf break at the mouth of Sam Ford Trough as geophysical data are needed farther offshore.
On the inter-trough areas between Sam Ford and Buchan troughs, the Baffin Shelf Drift and the position of the moraines extend near the shelf break. These ice-contact sediment bodies are geometrically linked to the seaward extent of the ISLMs. They provide evidence for a continuous maximum margin between Sam Ford Trough and Buchan Trough. Offshore Cape Jameson, the inter-trough area separating Pond and Buchan troughs was probably covered by ice, but additional data is required to enable the identification of ice-contact sediments. GDFs observed east of the Cape Jameson Bank reflect ice flowing from the Lancaster Ice Stream trough Bylot Trough.
Ice-contact deposits observed at the shelf edge are interpreted as MIS-2 because (1) they occur down-ice (eastward) from series of GZWs deposited during an episodic westward retreat of the LIS margin; and (2) the grounding-zone wedges are overlain by only one sedimentary sequence of deglacial-postglacial deposition corresponding to the last glacial retreat. The thickness of the upper sedimentary sequence along with the sedimentation rates observed in Scott Trough support a deglacial origin for the GZWs. A deglacial age for the GZWs therefore implies a seaward position of the LIS margin during MIS-2. The LIS margin could have reached its maximum extent prior to the LGM49 and remained at this position until well after the LGM. Extrapolation of radiocarbon dates on postglacial sediments in Scott Trough yield a minimum age of 15 ka BP for the beginning of postglacial sedimentation and, therefore, for the end of glaciation on the shelf16. We can only presume that the maximum extent of the LIS represents the LGM conditions during MIS-2, but further investigations including absolute chronology dating should focus on constraining the exact timing of the maximum ice extent. An absolute age for the LGM on the northeast Baffin Island continental shelf is not well constrained because: (1) the ice-contact sediments and the TMFs reported here could be of diachronic origin; (2)14C dates from these deposits are lacking; and (3) the LGM is a diachronic position corresponding to a time-period rather than a precise event in time. This time-period along eastern Baffin Island is yet to be resolved50.
The revised ice-margin and the distribution of highly elongated bedforms (MSGLs) indicate that ice streams were operating along Buchan, Scott and Pond troughs during MIS-2. The presence of ISLMs suggests that the LIS was experiencing spatial variations in ice-flow velocities, suggesting that inter-trough areas, were submitted to slow ice-flow or cold-based ice45, 46, 51,52,53. The presence of cold-based ice in the inter-ice stream areas is in accordance with the preservation of older deposits than MIS-2 on coastal forelands in between the fjords7. The basal thermal regime of the LIS in the region seems therefore complex and spatially variable with low-gradient outlet fast-flowing ice being constrained to the fjords axis as proposed by Miller et al. (2002). In Sam Ford Trough, the absence of ice-flow morphologies and the presence of perpendicular-to-trough ridges suggest that ice-flow was slow in the trough. This slow ice-flow was probably due to the transport of ice discharge from Sam Ford Fjord into the Scott Inlet Ice Stream. The ice-flow route from Sam Ford Fjord to Scott Inlet can be inferred from the northward orientation of MSGLs and drumlins at the junction of Sam Ford Fjord and Hecla & Griper Trough. The location of the GZWs suggests that the retreat of the LIS margin from the shelf edge to the fjords head has been marked by several phases of stabilization.
The swath bathymetry and geophysical data presented in this paper provide firm evidence that the LIS extended across the northeast Baffin Island continental shelf during MIS-2, reaching the continental shelf break between Scott Trough and Pond Trough. These data also confirm the presence of grounded glacial ice on the Lancaster Fan east of Pond Trough during MIS-2. The proposed maximum extent of the LIS during MIS-2 is located at least 36 km seaward of the previously proposed limits9, 50 and is in accordance with inferred LGM extents recently raised16,17,18.
Fast-flowing ice streams occupied Pond, Buchan and Scott troughs while slow ice-flow or cold-based ice occupied the shelf and Sam Ford Trough. The presence of GZWs in the four major cross-shelf troughs indicates an episodic retreat style punctuated by ice-margin stabilization rather than a rapid/catastrophic retreat16. Finally, these results indicate that the LIS deglaciation was driven by a complex spatially varying thermal regime with low-gradient ice-streams in the troughs and cold-based/slow-flowing ice on the inter-trough areas. An LIS deglaciation from an outer seaward position implies differences in the LIS geometry, dynamics, flow-mechanisms and feedbacks to post-LGM relative sea-level rise in Western Baffin Bay. This revised ice margin and its retreat dynamics should therefore be taken into account to increase the accuracy of LIS reconstructions or modelling, which have implications on how we can understand the long-term evolution of a marine-based ice-sheet during deglaciation.
Multibeam data were collected using Kongsberg Simrad EM-300 (12 kHz) and EM-302 (30 kHz) echosounders onboard the CCGS Amundsen by the Ocean Mapping Group (University of New Brunswick) and the Laboratoire de Géosciences Marines (Université Laval) for the ArcticNet program. The multibeam data were processed using the Caris HIPS&SIPS (www.caris.com/products/hips-sips/) and MB-System (https://www.ldeo.columbia.edu/res/pi/MB-System/) softwares. Data visualization and mapping was realized using ESRI ArcGIS 10.4 software (http://www.esri.com). Seismic reflection data were analyzed and extracted using the LizardTech GeoViewer software (https://www.lizardtech.com/geoviewer-pro/overview). Maps and seismic reflection data were transferred to the Adobe Photoshop CS5 software (www.adobe.com/photoshop) for figure production and editing. Seismic reflection data were enhanced using the Brightness/Contrast tool in Adobe Photoshop CS5 for a clearer visualization.
The multibeam bathymetry dataset can be visualized on the Université Laval Géoindex + website (http://geoindex-plus.bibl.ulaval.ca). The seismic reflection data along with the acquisition specifics are available on the Geological Survey of Canada website (http://ftp.maps.canada.ca/pub/nrcan_rncan/raster/marine_geoscience/Seismic_Reflection_Scanned/).
Publisher's note: Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
We sincerely thank the captains, crew and scientific participants (particularly Gabriel Joyal, Annie-Pier Trottier and Pierre-Olivier Couette) of ArcticNet cruises 2014–2016 on board the CCGS Amundsen. We also thank John Hughes Clarke and his team at the Ocean Mapping Group (University of New Brunswick) who collected swath bathymetry data on board the CCGS Amundsen in the region between 2003 and 2013. We thank D.C. Campbell and J.F. Ghienne for comments on the early version of the paper. This project was funded by ArcticNet Network Centres of Excellence and NSERC Discovery grants to P.L.