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Geometry and Ice Dynamics of the Darwin–Hatherton Glacial System, Transantarctic Mountains

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Geometry and Ice Dynamics of the Darwin–Hatherton Glacial System, Transantarctic Mountains Journal of Glaciology (2017), 63(242) 959–972 doi: 10.1017/jog.2017.60 © The Author(s) 2017. This is an Open Access article, distributed under the terms of the Creative Commons Attribution licence (http://creativecommons. org/licenses/by/4.0/), which permits unrestricted re-use, distribution, and reproduction in any medium, provided the original work is properly cited Geometry and ice dynamics of the Darwin–Hatherton glacial system, Transantarctic Mountains METTE K. GILLESPIE,1 WENDY LAWSON,2 WOLFGANG RACK,3 BRIAN ANDERSON,4 DONALD D. BLANKENSHIP,5 DUNCAN A. YOUNG,5 JOHN W. HOLT5 1Faculty of Engineering and Science, Western Norway University of Applied Sciences, P.O. Box 7030, Bergen, Norway 2Department of Geography, University of Canterbury, Private bag 4800, Christchurch, New Zealand 3Gateway Antarctica, University of Canterbury, Private bag 4800, Christchurch, New Zealand 4Antarctic Research Centre, Victoria University, P.O. Box 600, Wellington, New Zealand 5University of Texas Institute for Geophysics, University of Texas at Austin, Austin, Texas 78758, USA Correspondence: Mette Kusk Gillespie <[email protected]> ABSTRACT. The Darwin–Hatherton Glacial system (DHGS) connects the East Antarctic Ice Sheet (EAIS) with the Ross Ice Shelf and is a key area for understanding past variations in ice thickness of surrounding ice masses. Here we present the first detailed measurements of ice thickness and grounding zone char- acteristics of the DHGS as well as new measurements of ice velocity. The results illustrate the changes that occur in glacier geometry and ice flux as ice flows from the polar plateau and into the Ross Ice Shelf. The ice discharge and the mean basal ice shelf melt for the first 8.5 km downstream of the grounding line − − amount to 0.24 ± 0.05 km3 a 1 and 0.3 ± 0.1 m a 1, respectively. As the ice begins to float, ice thickness decreases rapidly and basal terraces develop. Constructed maps of glacier geometry suggest that ice drainage from the EAIS into the Darwin Glacier occurs primarily through a deep subglacial canyon. By contrast, ice thins to <200 m at the head of the much slower flowing Hatherton Glacier. The glacio- logical field study establishes an improved basis for the interpretation of glacial drift sheets at the link between the EAIS and the Ross Ice Sheet. KEYWORDS: Antarctic glaciology, glacier flow, glacier mass balance, ice/ocean interactions, ice thickness measurements 1. INTRODUCTION The TAM outlet glaciers exhibit large variations in ice flow Recent mass-balance studies have shown that Antarctica is dynamics, with surface velocities ranging between more than − losing mass, primarily as a result of accelerating outlet gla- 1000 m a 1 for the Byrd and David Glaciers (Humbert and − ciers in the northern Antarctic Peninsula and Amundsen others, 2005; Wuite and others, 2009)to<20 m a 1 for the Sea coast of the West Antarctic Ice Sheet (WAIS) (King and Taylor Glacier (Robinson, 1984; Kavanaugh and others, others, 2012; Shepherd and others, 2012; McMillan and 2009). Until now, glaciological studies in the TAM have pri- others, 2014; Wuite and others, 2015). By contrast, the East marily focused on the faster moving outlet glaciers (surface − Antarctic Ice Sheet (EAIS) appears to be gaining mass due velocities generally above 300 m a 1), while comparatively to a recent increase in annual snowfall in some coastal little is known about the slower moving glaciers (surface vel- − regions (Shepherd and others, 2012). Studies of EAIS outlet ocities generally between 5 and 300 m a 1). The Darwin– glaciers draining through the Transantarctic Mountains Hatherton glacial system (DHGS) belongs to the group of (TAM) have documented no major mass imbalance, but slow-moving TAM outlet glaciers and drains ice into the results remain uncertain due to a lack of accurate observa- Ross Ice Shelf. Glacial sediments found in the ice-free tions and direct measurements from many areas (Frezzotti valleys surrounding the DHGS provide evidence of at least and others, 2000; Rignot, 2002; Rignot and others, 2008; five episodes of increased ice extent, the timing of which is Wuite and others, 2009; Todd and others, 2010; Stearns, currently debated (Bockheim and others, 1989; Storey and 2011; King and others, 2012). However, the potential for others, 2010; Joy and others, 2014). Like most TAM outlet change in the TAM outlet glaciers is illustrated well by the glaciers, the dynamic behavior of the DHGS is generally distribution of glacial sediments in surrounding ice-free poorly understood due to insufficient knowledge of key para- areas (Bockheim and others, 1989; Storey and others, meters such as ice thickness, ice velocity, grounding line 2010; Joy and others, 2014). The along-flow varying extent location and surface mass balance (SMB) (Anderson and of moraines and glacial drift sheets show that the behavior others, 2004; Stearns, 2011). These data gaps have led to of the glaciers is affected by changes in both the EAIS and considerable uncertainties in modeling the response of the the Ross Ice Shelf, the latter of which receives two-thirds of DHGS to changes in climate and surrounding ice masses its ice from the WAIS (Mercer, 1968; Bockheim and others, (Anderson and others, 2004), and simple extrapolations of 1989; Denton and others, 1989a, b; Conway and others, glacial drift elevations have been used to infer the Last 1999; Fahnestock and others, 2000; Bromley and others, Glacial Maximum (LGM) ice thicknesses of the WAIS and 2010). As a consequence, the TAM outlet glaciers represent EAIS (Bockheim and others, 1989; Denton and Hughes, key areas for studying the past and present dynamic behavior 2000; Storey and others, 2010; Joy and others, 2014). In of both Antarctic ice sheets. order (a) to reduce the uncertainties in estimates of past ice Downloaded from https://www.cambridge.org/core. 23 Sep 2021 at 16:35:45, subject to the Cambridge Core terms of use. 960 Gillespie and others: Geometry and ice dynamics of the Darwin–Hatherton glacial system, Transantarctic Mountains thicknesses, and (b) to clarify existing discrepancies about the The glacial system is characterized by the presence of ages of the glacial drift sheets, and consequently the LGM several blue ice areas, prominent medial moraines and extent of the glacial system, additional glaciological investi- large adjacent ice-free valleys covered in glacial sediments. gations of the DHGS are required. The SMB of the DHGS is largely unknown. However, − In this paper, we present the findings of an airborne and average daily summer ablation rates of 1 mm d 1 have ground-based radar survey that mapped ice thickness, been measured within the lower Hatherton Glacier blue ice internal features and basal characteristics of the DHGS. In area (Riger-Kusk, 2011). No direct measurements of accumu- addition, GPS measurements of ice velocities were carried lation rates exist from within the DHGS catchment, but values − out at various locations throughout the glacial system. are thought to vary between 100 and 150 mm w.e. a 1 on the − From this dataset we aim to: (i) describe in detail the polar plateau and ∼200 mm w.e. a 1 on the Ross Ice Shelf changes in ice thickness, internal layers, ice base, hydrostatic (Bockheim and others, 1989). Several Antarctic-wide maps equilibrium, ice flux and basal melt rate, as the DHGS flows of SMB cover the region, but due to the lack of direct mea- across the grounding zone, (ii) provide the first ice thickness surements and relatively low resolutions compared with the and bed topography maps of the DHGS, (iii) discuss observed topography within the DHGS, none of these models accur- differences in ice velocity and ice flux between the Hatherton ately accounts for the observed patchwork of ablation and and Darwin Glaciers, and (iv) assess the current mass accumulation areas (Arthern and others, 2006; van de Berg balance of the DHGS. and others, 2006; Lenaerts and others, 2012a, b). The results presented in this paper on grounding zone Ice velocities were previously measured along two cross characteristics, ice flow behavior and balance state provide profiles during the 1978–1979 field season, and show that − new information not only about the DHGS, but also of the Hatherton Glacier flows at ∼40 m a 1 at the confluence slower moving EAIS outlet glaciers in general. The findings with the Darwin Glacier, while the velocity of the Darwin − allow for more accurate modeling of the dynamic behavior Glacier increases from ∼50 m a 1 at this location to ∼120 − of these glaciers to future changes in local and regional ma 1 at The Nozzle (Fig. 1, Hughes and Fastook, 1981). forcing. Such models will improve our understanding of the More recently, Antarctic ice surface velocities have been ice flow dynamics of the slower moving components of the determined remotely by means of satellite radar interferom- Antarctic ice masses, and of the surrounding WAIS and EAIS. etry (InSAR, Rignot and others, 2011b). The resulting map has a spatial resolution of 450 m and shows that the Hatherton Glacier generally moves with velocities of no − 2. THE DHGS more than 10 m a 1 and the Darwin Glacier reaches a − The DHGS (152–161°E, 79.3–80.2°S) consists of two main maximum velocity of ∼110 m a 1 at The Nozzle (Rignot glaciers; the Darwin Glacier which extends from the EAIS and others, 2011c). to the Ross Ice Shelf, and the Hatherton Glacier which Prior to this work, ice thickness has been measured at joins the Darwin Glacier downstream of the Darwin several locations along the Darwin Glacier and at two loca- Mountains ∼40 km upstream of the DHGS outlet (Fig. 1). tions on the Hatherton Glacier during airborne radar surveys Fig.
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