1. Introduction

Arctic sea ice has undergone dramatic changes in the recent past, with end-of-summer area shrinking by an average of 10.7% per decade between 1979 and 2007 (Reference StroeveStroeve and others, 2008), and average thickness decreasing by almost half over this period (Reference Kwok and RothrockKwok and Rothrock, 2009). Within Canada, sea-ice losses between 1968 and 2008 have occurred at a rate of 2.9±1.2% per decade in the Canadian Arctic Archipelago and 8.9±3.1% per decade in Baffin Bay (Reference TivyTivy and others, 2011). In concert with these changes, terrestrial ice masses in the Arctic have been undergoing substantial changes. For example, there has been widespread acceleration and retreat of outlet glaciers around Greenland (Reference Joughin, Smith, Howat, Scambos and MoonJoughin and others, 2010), and decrease in area and mass of ice caps in the Canadian High Arctic (Reference AbdalatiAbdalati and others, 2004; Reference Burgess and SharpBurgess and Sharp, 2004; Reference GardnerGardner and others, 2011). Little is currently known about the detailed interactions between sea ice and tidewater glaciers, however, particularly in the Canadian High Arctic. This information is required to properly assess how glaciers may change under a warming climate, and to better understand the controls on glacier dynamics and iceberg production rates. This is of particular importance given that calving can account for a significant proportion of mass loss from High Arctic ice caps and glaciers. For example, Reference Burgess, Sharp, Mair, Dowdeswell and BenhamBurgess and others (2005) found that glacier calving into the ocean may account for up to 30% of the total volume loss of Devon Ice Cap over the past 40 years, while Reference Williamson, Sharp, Dowdeswell and BenhamWilliamson and others (2008) argue that calving could account for ~40% of the current combined mass loss from glaciers in the Canadian Arctic, Svalbard and Russian Arctic.

Previous studies of the interactions between Arctic sea ice and glacier calving events have largely focused on Greenland. For example, Reference Reeh, Thomsen, Higgins and WeidickReeh and others (2001) found that landfast sea-ice conditions in front of Nioghalvfjerdsfjorden Glacier, northeast Greenland, have an important impact on the stability of its floating margin. Increased sea-ice cover ensures greater stability by protecting the glacier front from wave action and winds. Major calving events did not occur when landfast sea ice was present, but became extensive as the landfast ice broke up. The same series of events was observed on other glaciers in northeast Greenland by Reference HigginsHiggins (1989, Reference Higgins1991). There is also strong evidence that variability in glacier calving and terminus position at Jakobshavn Isbræ, Greenland, is related to the presence of sea ice and ice melange (dense mixture of calved icebergs) in the adjacent fiord (Reference JoughinJoughin and others, 2008; Reference Amundson, Fahnestock, Truffer, Brown, Lüthi and MotykaAmundson and others, 2010), with total summer calving flux more than six times greater than winter calving flux (Reference Sohn, Jezek and Van der VeenSohn and others, 1998). Both seasonal and long-term variations in the surface motion of Jakobshavn Isbræ also appear to be related to the presence of sea ice, ice melange and the associated stability of the terminal ice tongue (Reference Luckman and MurrayLuckman and Murray, 2005; Reference JoughinJoughin and others, 2008). Similarly, Reference Howat, Box, Ahn, Herrington and McFaddenHowat and others (2010) found that seasonal advance and retreat of the terminus of six marine-terminating glaciers in West Greenland correlates with the presence or absence of an adjacent ice melange.

In the Canadian Arctic, previous research on this topic has primarily investigated the interactions between sea ice and ice-shelf calving events. For example, Reference Copland, Mueller and WeirCopland and others (2007) found that the 2005 loss of the Ayles Ice Shelf occurred during a summer with the lowest sea-ice extent on record and a large open water lead along northern Ellesmere Island. In contrast, the Ayles and other adjacent ice shelves remained largely intact for long periods when they were protected by a fringe of semi-permanent landfast sea ice in the past. In one of the few studies that have looked at iceberg calving rates from glaciers in the Canadian High Arctic, Reference Williamson, Sharp, Dowdeswell and BenhamWilliamson and others (2008) argued that summer removal of sea ice could facilitate observed increases in seasonal flow rates, but that it was not an essential condition for order-of-magnitude velocity increases that were observed over short periods on some glaciers.

In this study we provide an assessment of the links between sea-ice conditions, glacier calving and the production of iceberg plumes from two large tidewater glaciers flowing from the northeast portion of Devon Ice Cap, Nunavut, Canada. A 12 year record from RADARSAT-1 synthetic aperture radar (SAR) imagery provides information on the frequency, magnitude and temporal variability of iceberg plumes which originate from these glaciers over both summer and winter seasons. This RADARSAT-1 imagery, terrestrial time-lapse photography, climate data and tidal predictions are used to assess the causes of these iceberg plumes and their relationship to sea-ice conditions. This research provides a contribution towards the international GLACIODYN project, which examines the response of Arctic glaciers to climate change. It also provides information required for understanding the causes of spatial and temporal variations in ice motion recorded on Devon Ice Cap (e.g. Reference Van Wychen, ice and BelcherVan Wychen, 2010).

2. Study Area

Devon Ice Cap is situated on the east side of Devon Island and has a surface area of ~14 000 km² (Reference Burgess and SharpBurgess and Sharp, 2008; Fig. 1). The eastern margin of the ice cap is fringed by extensive tidewater glaciers that exist due to high accumulation rates driven by moisture sources from nearby Baffin Bay (Reference Burgess, Sharp, Mair, Dowdeswell and BenhamBurgess and others, 2005; Reference Mair, Burgess and SharpMair and others, 2005). This study focuses on two major outlet glacier fronts of the northeast coast of Devon Ice Cap: Belcher and Fitzroy Glaciers (Fig. 1). Belcher Glacier is a large polythermal glacier that is ~5 km wide at its front, and grounded below sea level at its terminus. Ice thicknesses are ~100–250m across the northern half of its terminus and ~300–500m along the southern portion (Reference Dowdeswell, Benham, Gorman, Burgess and SharpDowdeswell and others, 2004). Fitzroy Glacier also appears to be grounded below sea level at its terminus, where it attains a thickness of ~200 m. Belcher Glacier is characterized by motion of >250ma^–1 at its ice front, compared to motion of up to ~200ma^–1 at the terminus of Fitzroy Glacier (Reference Van Wychen, ice and BelcherVan Wychen, 2010). Both glaciers are ~35 km long, although Belcher drains a larger area. Reference Burgess, Sharp, Mair, Dowdeswell and BenhamBurgess and others (2005) calculated that Belcher Glacier is responsible for ~47% of total glacier calving into the ocean from Devon Ice Cap, while the other glaciers along the eastern margin account for ~40%.

Fig. 1.

Study locations on Devon Ice Cap (base image: 2000 Landsat Enhanced Thematic Mapper Plus).

3. Methods

4. Results

Analysis of the 1997–2008 RADARSAT-1 imagery and CIS charts indicates that annual landfast sea-ice retreat from the bays in front of Belcher and Fitzroy Glaciers generally occurs in the second or third week of July (Fig. 3). The start date of sea-ice break-up ranges between 7 and 23 July for Belcher Glacier, and between 15 July and 1 August for Fitzroy Glacier. Sea-ice retreat from Fitzroy Glacier typically occurs later in the summer than for Belcher Glacier, although sea-ice retreat from both glacier fronts occurred simultaneously from 2003 to 2006. The dates of annual sea-ice retreat for the 12 year period indicate no significant longterm trend, similar to the findings of Reference TivyTivy and others (2011) for northwest Baffin Bay. In terms of sea-ice formation, this occurs between mid-October and mid-November, with the embayment in front of Fitzroy Glacier typically freezing up a week or two later than that in front of Belcher Glacier (Fig. 3). It appears that freeze-up occurred later near the end of our study period than at the start, although the spatial and temporal resolutions of our record do not allow determination of whether this is a significant long-term trend.

Fig. 3.

Temporal variability in the presence (grey area) and absence (white area) of landfast sea ice, together with the timing and size of iceberg plumes from (a) Belcher Glacier and (b) Fitzroy Glacier, 1997–2008.

RADARSAT-1 imagery from 1997–2008 indicates that the production of iceberg plumes is strongly related to the retreat of sea ice from the glacier fronts (Fig. 3). Plumes typically appear in front of both glaciers coincident with sea-ice break-up, although occasionally they occur up to a few days prior to the first day of sea-ice retreat (e.g. 2001, 2002, 2005 and 2007 for Fitzroy Glacier; Fig. 3). Comparison of the iceberg plumes observed in the SAR imagery with the 2007–08 time-lapse photography at Belcher Glacier suggests that these events are likely dominated by the release of an ice melange accumulated at the glacier front during the preceding spring and winter, together with some new glacier calving. It is difficult to quantify the relative importance of these sources to the iceberg plumes observed during sea-ice break-up at Fitzroy Glacier and in other years at Belcher Glacier, but analysis of the SAR imagery suggests that both processes are important. At other times of the year, it appears that new glacier calving provides essentially all of the source for the observed iceberg plumes. The time-lapse photography indicates that both small icebergs and large, full-glacier-thickness icebergs are calved from Belcher Glacier.

Multiple iceberg plumes typically occur annually from both glaciers, although they are more frequent from Fitzroy Glacier than from Belcher Glacier, especially for large (size 3) events (Fig. 3). During the 12 year study period, 24 plumes in total were recorded from Belcher Glacier in the RADARSAT-1 imagery, compared to 38 from Fitzroy Glacier. Some of these events occurred simultaneously on both glaciers, but many did not. Iceberg plumes were typically restricted to an origin from the southern portion of Belcher Glacier (where the ice is thickest), but originated from across the entire terminus of Fitzroy Glacier.

The largest iceberg plumes from Belcher Glacier often occur within a 24 hour period of most of the landfast sea ice breaking up and retreating (Fig. 3). For example, in 2007 a small iceberg plume (size 1) was first detected in the RADARSAT-1 imagery on 15 July (Fig. 4a). The sea ice then began to break up in front of Belcher Glacier on 17 July (Fig. 4c), followed by the release of a large plume of icebergs (size 3) the next day after most of the sea ice had retreated from the glacier front (Fig. 4e). Some of these icebergs originated from the release of the existing iceberg melange, but it appears that there was also new glacier calving shortly after the loss of the landfast sea ice. This sequence of events was confirmed by the time-lapse photography (Fig. 4b, d and f), which indicates that glaciers can calve icebergs even when landfast ice is present, but that large calving events typically only occur once the landfast ice has gone.

Fig. 4.

Sea-ice conditions and iceberg plumes at Belcher Glacier in July 2007 in RADARSAT-1 ScanSAR Wide-B imagery (a, c, e) and near-coincident time-lapse photography (b, d, f). (a, b) A new iceberg plume prior to sea-ice retreat (field of view of time-lapse camera shown by white lines). (c, d) Landfast sea-ice break-up and retreat without any new iceberg plume. (e, f) Major iceberg plume shortly after sea ice retreats from Belcher Bay. Times are in UTC. (RADARSAT imagery © Canadian Space Agency.)

On Fitzroy Glacier the largest iceberg plumes (size 3) typically occur in late July or early August, between a few days and a couple of weeks after landfast sea-ice retreat (Fig. 3 and 5). Small and medium iceberg plumes typically occur simultaneously with the initial loss of sea ice, but large size 3 events are not so common at this time.

Fig. 5.

Progression of sea-ice break-up and production of iceberg plumes from Fitzroy Glacier in RADARSAT-1 ScanSAR Wide-B imagery from summer 2000. (a) Fitzroy Glacier front with landfast sea-ice cover. (b) Beginning of landfast ice break-up with a small iceberg plume. (c) Large (size 3) iceberg plume when no sea ice present. Times are in UTC. (RADARSAT imagery © Canadian Space Agency.)

Winter iceberg plumes were occasionally detected in the SAR imagery when landfast sea ice was present, although these events are less frequent and generally smaller than summer events (Fig. 3). Over the 12 year study period, a total of six iceberg plumes from Belcher Glacier and five from Fitzroy Glacier were recorded more than a week before break-up or a week after freeze-up. Winter events occur on both glaciers simultaneously in some years, but appear isolated in other years. For example, an iceberg plume occurred on 27–28 January 2006 from Belcher Glacier, when no plume was observed from Fitzroy Glacier. However, iceberg plumes occurred simultaneously from both glaciers on 28–30 December 2003.

An important issue when assessing events observed in the satellite record is whether the RADARSAT-1 imagery captures all the iceberg production events that occur from Belcher and Fitzroy Glaciers. To test this, all of the Belcher time-lapse photography was compared with the satellite image record for both summers 2007 and 2008. This comparison indicated that small glacier calving events prior to landfast sea-ice retreat are not always reliably identified using RADARSAT-1 scenes with 100m resolution. However, events that occurred when sea ice was no longer present were easier to identify due to their typically greater size and the high backscatter contrast between rough calved ice and open water. Another issue is that small, short-lived events are captured with time-lapse imagery collected at hourly intervals (Fig. 6a), but may be missed with satellite imagery collected at daily or longer intervals (Fig. 6b and c). The long-term record presented here (Fig. 3) should therefore be treated as a minimum estimate of iceberg production events from northeast Devon Ice Cap, especially for small, short-lived events. However, we have high confidence that medium and large events are well recorded by the satellite imagery, which accounts for the bulk of ice lost by calving in this region.

Fig. 6.

(a) Photograph of Belcher Glacier from 4 August 2008, showing a very small glacier calving event (white arrow) which had occurred in the previous hour. (b, c) RADARSAT-1 imagery from the closest available times before (b) and after the calving event (c) does not show an iceberg plume, although careful analysis indicates a change in shape of the glacier front over this period. Times are in UTC. (RADARSAT imagery © Canadian Space Agency.)

5. Discussion and Conclusions

The results of this study demonstrate a direct relationship between sea-ice conditions and the production of iceberg plumes from Belcher and Fitzroy Glaciers. Small to medium iceberg plumes occur almost simultaneously with the loss of landfast sea ice from the embayments in front of the glaciers, which occurs when PDDs have exceeded ~150 a^–1. These events likely represent the release of previously trapped ice melange, together with new glacier calving. The largest iceberg plumes then typically occur within a few days of the loss of the landfast ice, during open-water conditions. These events are likely dominated by new glacier calving. This highlights the importance of sea ice in providing a protective fringe for High Arctic tidewater glaciers, as has previously been found by, for example, Reference Reeh, Thomsen, Higgins and WeidickReeh and others (2001) and Reference Howat, Box, Ahn, Herrington and McFaddenHowat and others (2010). However, the occurrence of winter iceberg plumes (albeit typically smaller than summer events) when landfast sea ice is present indicates that sea-ice conditions do not provide the only factor controlling iceberg production processes. In addition, it is likely that more small glacier calving events occur than have been identified here due to limitations in detecting them in RADARSAT-1 ScanSAR imagery. Analysis of climate and tidal conditions shows little relationship to the timing of iceberg plumes, which suggests that both winter and summer calving probably also occur as a stochastic process in response to the movement of highly crevassed ice toward the glacier terminus.

Over the study period, we observed fewer iceberg plumes originating from Belcher Glacier than from Fitzroy Glacier, although there is no evidence of significant terminus retreat of either glacier over the period 1997–2008. The iceberg plumes discussed here thus reflect the normal loss of mass from the terminus of these glaciers as part of the ablation process. Previous studies have mainly focused on glacier dynamics and water depth at the terminus as the primary factors influencing calving rates on tidewater glaciers (e.g. Reference Van der VeenVan der Veen, 2002), but the results here indicate that adjacent sea-ice conditions should also be considered. This is important for determining the long-term evolution of tidewater glaciers in the Canadian Arctic, as previous studies in West Greenland suggest that sustained glacier retreat may be triggered by declines in sea-ice concentrations (Reference JoughinJoughin and others, 2008; Reference Howat, Box, Ahn, Herrington and McFaddenHowat and others, 2010; Reference Vieli and NickVieli and Nick, 2011).