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Paleosea Ice Conditions of the Amundsen Gulf

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Paleosea Ice Conditions of the Amundsen Gulf JOURNAL OF GEOPHYSICAL RESEARCH, VOL. 113, C03S02, doi:10.1029/2007JC004202, 2008 Paleo–sea ice conditions of the Amundsen Gulf, Canadian Arctic Archipelago: Implications from the foraminiferal record of the last 200 years Trecia M. Schell,1 Tamara J. Moss,1 David B. Scott,1 and Andre Rochon2 Received 6 March 2007; revised 11 July 2007; accepted 28 September 2007; published 26 March 2008. [1] Four boxcores were collected as part of the Canadian Arctic Exchange Shelf Study (CASES) in the Amundsen Gulf at water depths of 59 m to 600 m. Data from these cores help to develop a record of changes in the oceanographic history of the area over the last 200 years, with particular reference to the indication of paleo–sea ice formation, a key element of the Arctic ecosystem. The four sites cover a range of water depths and environments to provide a basis for comparison. The benthic foraminifera of sites CA-06 (253 m water depth) and CA-18 (600 m water depth) show an increase in Arctic Surface Water associated agglutinated foraminifera over the last 100 years (uppermost 8 to 16 cm). These are indicating a decrease in sea ice cover and in cold saline Arctic Bottom Water influence; these are similar to Canadian Arctic Archipelago postglacial faunas. This contrasts with abundant planktic foraminifera at the same stations, suggesting strong, oceanic Arctic surface influence (little freshwater) in the central Gulf. The foraminifera of sites 403B (59 m water depth) and 415B (56 m water depth), at the outermost edges of Amundsen Gulf, indicate that the present-day location of the winter flaw lead has been in place for at least the last 100 years, with foraminiferal faunas similar to those of the Beaufort Shelf. Additionally, station 415 is on an earlier Holocene shoreline that is covered with cobbles. Citation: Schell, T. M., T. J. Moss, D. B. Scott, and A. Rochon (2008), Paleo–sea ice conditions of the Amundsen Gulf, Canadian Arctic Archipelago: Implications from the foraminiferal record of the last 200 years, J. Geophys. Res., 113, C03S02, doi:10.1029/ 2007JC004202. 1. Introduction Castleden, 2001]. The extreme climactic conditions present many practical challenges to conduct research of the Arctic [2] The ecological impacts of climate warming are a region. The fundamental question has always been how popular topic of study in today’s scientific community. much of this change is ‘‘natural’’ versus anthropogenic The Previous reports by the Intergovernmental Panel on Climate collection and analysis of historical as well as prehistoric Change [Intergovernmental Panel on Climate Change, changes (as defined by fossil assemblages of microfossils in 2001] predicted that doubling of carbon dioxide in the these cores) in Arctic oceanography and sedimentation data atmosphere would result in global average temperatures to is a valuable means of beginning to shape a more long-term increase by 1.5°Cto4.5°C, and perhaps up to 11°C[Adam, (over 1000 years) scientific understanding of Arctic natural 2006]. The Canadian Arctic is suggested to be particularly history and in this case sea ice cover. sensitive to the warming and is demonstrating dramatic [3] Over the course of a year (September 2003 to August changes to its climate, which are evident in changes to the 2004) the Canadian Arctic Shelf Exchange Study (CASES) permafrost and sea ice cover. These changes can affect the operated the Canadian Coast Guard ship, NGCC Amundsen well-being of species which depend on particular ecological in the Western Canadian Arctic. The research activities of processes and conditions that have been typical of this CASES involved the collection of a multitude of scientific Arctic region. Changes in the Arctic climate can also affect data from the Beaufort Shelf ecosystem. The focus was to the coastal Inuit communities of this region, whose tradi- determine the impacts of climate warming on the biological tional way of life is dependent on what is now a threatened and physical processes of the Beaufort Shelf, and to apply Arctic environment. The Inuvialuit of Banks Island find it these conclusions on a global scale (CASES 2004). The data increasingly dangerous to hunt on the sea ice [Ashford and from our study in Amundsen Gulf, as a part of the Beaufort 1 Shelf ecosystem, will extend this knowledge to the last few Centre for Environmental and Marine Geology, Department of Earth centuries. Sciences, Dalhousie University, Halifax, Nova Scotia, Canada. 2 Institut des Sciences de la Mer de Rimouski, Universite´ du Que´bec a` 1.1. Environmental Setting Rimouski, Rimouski, Quebec, Canada. [4] Amundsen Gulf is a 400-km-long, 200-km-wide Copyright 2008 by the American Geophysical Union. embayment or marine trough between Banks Island and 0148-0227/08/2007JC004202 C03S02 1of14 C03S02 SCHELL ET AL.: SEA ICE IN AMUNDSEN GULF LAST 200 YEARS C03S02 Figure 1. Location map of the 4 core sites in relation to the three sea ice regimes (a) offshore pack ice, (b) landfast ice, and (c) polynya location in the Amundsen Gulf region (modified from Barber and Hanesiak [2004]). Victoria Island on the eastern side, and the Arctic mainland 2005; Stokes et al., 2006] show the subglacial bed form coast at the western shore. Amundsen Gulf is the one part evidence for several major paleo-ice streams, and their of the westernmost end of the Northwest Passage, and retreat. They suggest that by 11,000 calibrated years before connects the Dolphin and Union Straits, and also the present (cal BP) the glacial retreat was occurring, and by Prince of Wales Strait with the Beaufort Sea, and the 10,000 calBP Amundsen Gulf was ice free (indicated by the Arctic Ocean. presence and dating of the Colville Moraine, and other [5] The history of sea ice and glacial ice in the Amundsen deposits). Thin ice stagnated, and melted in situ [Sharpe, Gulf area are both important factors in determining the 1988], possibly the cause of the deep ‘600 m hole’ in long-term (millennial-decadal) exchange of surface waters Amundsen Gulf. These glacial outwash, or ice stream between the Arctic Ocean, the Beaufort Sea and the North- events, are similar in timing to the micropaleontological west Passage during the late Quaternary period. During the evidence from a longitudinal transect of piston cores from Last Glacial Maximum (LGM) this area was under the the Mackenzie Trough (T. M. Schell et al., submitted influence of the Laurentide and Innutian Ice Sheets, and manuscript, 2008). with deglaciation several major ice streams or conduits [6] Other interest in the paleoceanographic history of formed including the Mackenzie River to the west (Lauren- the Canadian Arctic Archipelago (CAA) is focused on tide IS), the Amundsen Gulf Ice Stream in the middle the recent decrease in sea ice and the possibility that the (Laurentide IS, and possibly bounded by the Innutian IS), Northwest Passage from Lancaster Sound to the Amundsen and the easternmost M’Clure Strait–Viscount-Melville Gulf and Beaufort Sea may become ice-free in summer [i.e., Sound (Innutian IS) [Stokes et al., 2006]. In Amundsen Lange et al., 1999]. Historical oceanographic measurements Gulf, seafloor imagery and LandSat imagery [Blasco et al., over the past 50 years show that the annual temperature in Table 1. Location of Boxcore From CASES 2003–2004 (Amundsen) Station Number CASES Sample Number Latitude Longitude Water Depth Sampling Device Sample Type Length (cm) CA-06 2003-CA06A 70°35.4890N 127°13.5680W 253 m boxcore Push core 35.5 CA-18 2003-CA18A 70°39.0030N 123°04.8240W 600 m boxcore Push core 34.5 403B 2004-804-403B 71°06.7770N 128°18.3030W 59 m boxcore Push core 29.0 415B 2004-804-415B 71°54.4550N 125°52.0920W 56 m boxcore Push core 22.0 2of14 C03S02 SCHELL ET AL.: SEA ICE IN AMUNDSEN GULF LAST 200 YEARS C03S02 Figure 2. Seafloor images, seafloor surface backscatter images and seismic sub bottom profiles from site (a) 403B and (b) 415B. the western Canadian Arctic has increased by 0.6°À1.2°C offshore pack ice is mobile annually and multiyear in [Overpeck et al., 1997] and there has been an 8% reduction regions beyond the extent of the maximum landfast ice in sea ice extent since 1978 [Couture and Bancroft, 2003]. (Figure 1a). Landfast sea ice forms annually within the These historical values are presently used to initialize and coastal margins over the continental shelves (Figure 1b). A constrain global circulation models (GCMs) to predict flaw lead polynya system is usually located on the shelf future climate change in the Canadian Arctic. The results break between the Amundsen Gulf and Beaufort Sea. The suggest that by 2070, there will be a 2° to 4°C increase in Cape Bathurst Polynya complex consists of series of leads SST between Baffin Bay and the Central Arctic Ocean and a latent heat polynya within the Amundsen Gulf [MacKenzie, 2003]. The historical records, however, are too (Figure 1c). Summer ice in the Beaufort Sea varies from short to allow realistic evaluation of the GCM estimates. season to season. Normally in April, a polynya develops at The palynological records from North Water Polynya the entrance of Amundsen Gulf and expands toward the (NOW) and Coburg Polynya show quasi-cyclical changes west. In August, the open water in a normal year may of 2° to 4°C at intervals of 1000–1500 years for the past extend 180 to 300 km off the Canadian coast. However, it 8000 years [Levac et al., 2001; Mudie et al., 2006], and did not extend that far in the 2004 season. The average time archaeological evidence shows major century-scale changes of freezeups in the Beaufort Sea is the second week of in hunting modes of paleo-Inuit peoples that may reflect October [Barber and Hanesiak, 2004].
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