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Exceptional Retreat of Novaya Zemlya's Marine The Cryosphere, 11, 2149–2174, 2017 https://doi.org/10.5194/tc-11-2149-2017 © Author(s) 2017. This work is distributed under the Creative Commons Attribution 3.0 License. Exceptional retreat of Novaya Zemlya’s marine-terminating outlet glaciers between 2000 and 2013 J. Rachel Carr1, Heather Bell2, Rebecca Killick3, and Tom Holt4 1School of Geography, Politics and Sociology, Newcastle University, Newcastle-upon-Tyne, NE1 7RU, UK 2Department of Geography, Durham University, Durham, DH13TQ, UK 3Department of Mathematics & Statistics, Lancaster University, Lancaster, LA1 4YF, UK 4Centre for Glaciology, Department of Geography and Earth Sciences, Aberystwyth University, Aberystwyth, SY23 4RQ, UK Correspondence to: J. Rachel Carr ([email protected]) Received: 7 March 2017 – Discussion started: 15 May 2017 Revised: 20 July 2017 – Accepted: 24 July 2017 – Published: 8 September 2017 Abstract. Novaya Zemlya (NVZ) has experienced rapid ice al., 2013). This ice loss is predicted to continue during loss and accelerated marine-terminating glacier retreat dur- the 21st century (Meier et al., 2007; Radic´ et al., 2014), ing the past 2 decades. However, it is unknown whether and changes are expected to be particularly marked in the this retreat is exceptional longer term and/or whether it has Arctic, where warming of up to 8 ◦C is forecast (IPCC, persisted since 2010. Investigating this is vital, as dynamic 2013). Outside of the Greenland Ice Sheet, the Russian high thinning may contribute substantially to ice loss from NVZ, Arctic (RHA) accounts for approximately 20 % of Arctic but is not currently included in sea level rise predictions. glacier ice (Dowdeswell and Williams, 1997; Radic´ et al., Here, we use remotely sensed data to assess controls on NVZ 2014) and is, therefore, a major ice reservoir. It comprises glacier retreat between 1973/76 and 2015. Glaciers that ter- three main archipelagos: Novaya Zemlya (NVZ; glacier minate into lakes or the ocean receded 3.5 times faster than area D 21 200 km2/, Severnaya Zemlya (16 700 km2/, and those that terminate on land. Between 2000 and 2013, re- Franz Josef Land (12 700 km2/ (Moholdt et al., 2012). Be- treat rates were significantly higher on marine-terminating tween 2003 and 2009, these glaciated regions lost ice at outlet glaciers than during the previous 27 years, and we ob- a rate of between 9.1 Gt a−1 (Moholdt et al., 2012) and serve widespread slowdown in retreat, and even advance, be- 11 Gt a−1 (Gardner et al., 2013), with over 80 % of mass tween 2013 and 2015. There were some common patterns loss coming from Novaya Zemlya (NVZ) (Moholdt et al., in the timing of glacier retreat, but the magnitude varied be- 2012). This much larger contribution from NVZ has been tween individual glaciers. Rapid retreat between 2000 and attributed to it experiencing longer melt seasons and high 2013 corresponds to a period of significantly warmer air tem- snowmelt variability between 1995 and 2011 (Zhao et al., peratures and reduced sea ice concentrations, and to changes 2014). More recent estimates suggest that the mass balance in the North Atlantic Oscillation (NAO) and Atlantic Multi- of the RHA was −6.9 ± 7.4 Gt between 2004 and 2012 (Mat- decadal Oscillation (AMO). We need to assess the impact of suo and Heki, 2013) and that thinning rates increased to this accelerated retreat on dynamic ice losses from NVZ to −0.40 ± 0.09 m a−1 between 2012/13 and 2014, compared accurately quantify its future sea level rise contribution. to the long-term average of −0.23 ± 0.04 m a−1 (1952 and 2014) (Melkonian et al., 2016). The RHA is, therefore, fol- lowing the Arctic-wide pattern of negative mass balance (Gardner et al., 2013) and glacier retreat that has been ob- 1 Introduction served in Greenland (Enderlin et al., 2014; McMillan et al., 2016), Svalbard (Moholdt et al., 2010a, b; Nuth et al., 2010), Glaciers and ice caps are the main cryospheric source and the Canadian Arctic (Enderlin et al., 2014; McMillan et of global sea level rise and contributed approximately al., 2016). However, the RHA has been studied far less than −215 ± 26 Gt yr−1 between 2003 and 2009 (Gardner et Published by Copernicus Publications on behalf of the European Geosciences Union. 2150 J. R. Carr et al.: Exceptional retreat of Novaya Zemlya’s marine-terminating outlet glaciers other Arctic regions, despite its large ice volumes. Further- Price et al., 2011; Sole et al., 2008) but was similar to more, assessment of 21st-century glacier volume loss high- the Canadian Arctic, where the vast majority of recent ice lights the RHA as one of the largest sources of future ice loss loss occurred via increased surface melting (∼ 92 % of total and contribution to sea level rise, with an estimated loss of ice loss), rather than accelerated glacier discharge (∼ 8 %) 20–28 mm of sea level rise equivalent by 2100 (Radic´ et al., (Gardner et al., 2011). This implied that outlet glacier re- 2014). treat was having a limited and/or delayed impact on inland Arctic ice loss occurs via two main mechanisms: a net ice or that available data were not adequately capturing sur- increase in surface melting, relative to surface accumula- face elevation change in outlet glacier basins (Carr et al., tion, and accelerated discharge from marine-terminating out- 2014). More recent results demonstrate that thinning rates let glaciers (e.g. Enderlin et al., 2014; van den Broeke et al., on marine-terminating glaciers on the Barents Sea coast are 2009). These marine-terminating outlets allow ice caps to re- much higher than on their land-terminating neighbours, sug- spond rapidly to climatic change, both immediately through gesting that glacier retreat and calving do promote inland, calving and frontal retreat (e.g. Blaszczyk et al., 2009; Carr dynamic thinning (Melkonian et al., 2016). However, higher et al., 2014; McNabb and Hock, 2014; Moon and Joughin, melt rates also contributed to surface lowering, evidenced 2008) and also through long-term drawdown of inland ice, by the concurrent increase in thinning observed on land- often referred to as “dynamic thinning” (e.g. Price et al., terminating outlets (Melkonian et al., 2016). High rates of 2011; Pritchard et al., 2009). During the 2000s, widespread dynamic thinning have also been identified on Severnaya marine-terminating glacier retreat was observed across the Zemlya, following the collapse of the Matusevich Ice Shelf Arctic (e.g. Blaszczyk et al., 2009; Howat et al., 2008; Mc- in 2012 (Willis et al., 2015). Here, thinning rates increased to Nabb and Hock, 2014; Moon and Joughin, 2008; Nuth et al., 3–4 times above the long-term average (1984–2014), follow- 2007), and substantial retreat occurred on Novaya Zemlya ing the ice-shelf collapse in summer 2012, and outlet glaciers between 2000 and 2010 (Carr et al., 2014): retreat rates in- feeding into the ice shelf accelerated by up to 200 % (Willis creased markedly from around 2000 on the Barents Sea coast et al., 2015). The most recent evidence, therefore, suggests and from 2003 on the Kara Sea (Carr et al., 2014). Between that NVZ and other Russian high Arctic ice masses are vul- 1992 and 2010, retreat rates on NVZ were an order of mag- nerable to dynamic thinning, following glacier retreat and/or nitude higher on marine-terminating glaciers (−52.1 m a−1/ ice-shelf collapse. Consequently, it is important to under- than on those terminating on land (−4.8 m a−1/ (Carr et stand the longer-term retreat history on NVZ in order to eval- al., 2014), which mirrors patterns observed on other Arc- uate its impact on future dynamic thinning. Furthermore, we tic ice masses (e.g. Dowdeswell et al., 2008; Moon and need to assess whether the high glacier retreat rates observed Joughin, 2008; Pritchard et al., 2009; Sole et al., 2008) and on NVZ during the 2000s have continued and/or increased, was linked to changes in sea ice concentrations (Carr et al., as this may lead to much larger losses in the future and may 2014). However, the pattern of frontal-position changes on indicate that a step change in glacier behaviour occurred in NVZ prior to 1992 is uncertain, and previous results indi- ∼ 2000. cate different trends, dependant on the study period: some In this paper, we use remotely sensed data to assess glacier studies suggest glaciers were comparatively stable or retreat- frontal-position change for all major (> 1 km wide) Novaya ing slowly between 1964 and 1993 (Zeeberg and Forman, Zemlya outlet glaciers (Fig. 1). This includes all outlets from 2001), whilst others indicate large reductions in both the vol- the ice cap of the northern island (hereafter referred to as ume (Kotlyakov et al., 2010) and the length of the ice coast the northern island ice cap for brevity) and its subsidiary ice (Sharov, 2005) from ∼ 1950 to 2000, and longer-term retreat fields (Fig. 1). We were unable to find the names of these (Chizov et al., 1968; Koryakin, 2013; Shumsky, 1949). Con- subsidiary ice fields in the literature, so we name them Sub 1 sequently, it is difficult to contextualize the observed period and Sub 2 (Fig. 1). A total of 54 outlet glaciers were inves- of rapid retreat from ∼ 2000 until 2010 (Carr et al., 2014) and tigated, which allowed us to assess the impact of different to determine if it was exceptional or part of an ongoing trend. glaciological, climatic and oceanic settings on retreat (Ta- Furthermore, it is unclear whether glacier retreat has contin- ble S1 in the Supplement). Specifically, we assessed the im- ued to accelerate after 2010, and hence further increased its pact of coast (Barents Sea versus Kara Sea on the north- contribution to sea level rise, or whether it has persisted at a ern ice mass), ice mass (northern island ice cap, Sub 1, or similar rate.
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