SPECIALTY GRAND CHALLENGE article
Sec. Cryospheric Sciences
Volume 5 - 2017 | https://doi.org/10.3389/feart.2017.00064
Grand Challenges in Cryospheric Sciences: Toward Better Predictability of Glaciers, Snow and Sea Ice
- 1Geophysical Institute, University of Alaska Fairbanks, Fairbanks, AK, United States
- 2Department of Earth Sciences, Uppsala University, Uppsala, Sweden
- 3College of Earth Ocean and Atmospheric Sciences, Oregon State University, Corvallis, OR, United States
- 4Institute for Snow and Avalanche Research, Davos, Switzerland
Cryospheric sciences encompass the study of frozen water in all forms, including glacier ice, seasonal snow, sea, lake, and river ice, and frozen ground. All components of the cryosphere are closely interlinked and coupled to other components of the Earth, in particular the climate system. Due to ongoing rapid changes in response to atmospheric and oceanographic warming, the cryosphere has received increased attention by the scientific community, policymakers, and the public. Widespread glacier retreat and mass loss, decrease in snow cover, decline in sea ice, and thawing permafrost are at the forefront of concern due to the range of possible major socio-economic, ecological, and environmental consequences. For developing efficient mitigation and adaption strategies one of the main challenges in cryospheric sciences is to make accurate predictions of anticipated changes on timescales relevant to policy-makers. This is inherently difficult due to the complex non-linear nature of cryospheric processes and feedback mechanisms. Despite major progress in recent years, currently, accurate predictions are hampered by insufficient observations, process understanding, and modeling capacities. These deficiencies need to be addressed to further the understanding and prediction of the cryosphere.
Here, we focus on glaciers, snow, and sea ice, and discuss some of the “Grand Challenges” related to the need for better understanding and predicting their changes due to anticipated climate change. We are fully aware that our subjective and non-exhaustive focus does not embrace the full range of challenges faced by the broad field of snow and ice research.
Glaciers and Ice Sheets
Glaciers around the world are losing mass at an accelerating pace with profound implications for global sea-level rise, global climate, local river systems, and their physical, biogeochemical, and ecological properties, as well as natural hazards. Observations indicate a consistent and largely homogenous trend of global retreat and shrinkage of the Earth's mountain glaciers, ice-shelf collapses in Antarctica, and an exceptional acceleration in ice flow and associated mass losses of outlet glaciers in Greenland and West Antarctica in response to atmospheric and ocean warming. These changes highlight the need for further capabilities to monitor, understand and predict the behavior of land ice and its interactions with the atmosphere and the oceans.
In the last decade, new remote sensing technologies and missions, such as NASA's Ice, Cloud, and land Elevation Satellite (IceSAT), the Gravity Recovery and Climate Experiment (GRACE), and the Operation IceBridge have revolutionized our ability to monitor the state and changes of land ice masses, in particular of the two huge ice sheets in Greenland and Antarctica, and glaciers in remote polar regions. These observations indicate that mass loss from glaciers and ice sheets has contributed approximately 60% of total global sea-level rise during the period 2003–2009 with roughly equal shares from the two ice sheets in Greenland and Antarctica combined (259 ± 28 Gt year−1 or 0.71 ± 0.08 mm SLE (sea-level equivalent) year−1) and all ~200,000 glaciers outside the ice sheets (289 ± 49 Gt year−1 or 0.79 ± 0.13 mm SLE year−1; Shepherd et al., 2012; Gardner et al., 2013), highlighting their socio-environmental relevance. Extending these estimates to cover the period April 2002–November 2014, Reager et al. (2016) find that the ice sheet contribution has increased considerably (1.26 mm SLE year−1), while the glacier contribution remained similar (0.65 mm SLE year−1). Hence, the share of the ice sheets relative to the mountain glacier contribution has risen. Their results also indicate that the rapidly increasing cryospheric contribution has partially been masked by an increase in water stored on land.
Rapid Dynamic Changes
The discovery that the ice sheets can change much faster than previously considered possible, took the glaciological community by surprise, rendering the ice sheets a “wild card” in any attempts to project future contributions to sea-level rise (Truffer and Fahnestock, 2007; Alley and Joughin, 2012). Some marine-terminating outlet glaciers in Greenland have doubled or even tripled their speed (Joughin et al., 2004) in just a few years, accompanied by thinning and rapid retreat after years of stable front positions (Howat et al., 2007; Stearns and Hamilton, 2007). Flow acceleration has gradually expanded to the north (Rignot and Kanagaratnam, 2006). Some glaciers have then returned to “normal” flow speeds (Murray et al., 2010) indicating that rapid changes in either direction are possible within just a few years. The largely synchronous acceleration in ice flow over large areas is indicative of a common climatic (Joughin et al., 2008) or oceanic driver (Holland et al., 2008; Straneo et al., 2010), although the response to regional and local forcing is complex (Moon et al., 2012, 2014, 2015; Straneo et al., 2013).
Many Greenland outlet glaciers occupy deep troughs extending far inland below sea level setting the stage for inherently unstable glacier behavior. The situation is even more worrisome in West Antarctica, where most of the ice sheet is grounded below sea-level on an inland-sloping bed, providing a delicate setting prone for potential run-away effects once retreat is initiated (Joughin and Alley, 2011), as had been envisioned early on (Mercer, 1978). Rapid changes possibly indicative of such an ice sheet instability have recently been observed at Thwaites and Pine Island Glacier (Mouginot et al., 2014), which combined drain ~5% of the Antarctic Ice Sheet. Ice-sheet simulations by De Conto and Pollard (2016) suggest that rapid mass loss from Antarctica due to marine ice-sheet instabilities may cause a meter of sea-level rise by 2100 and more than 15 m by 2500. Studies investigating the observed dynamic thinning, grounding line retreat and net mass loss suggest that these changes may signal the onset of a collapse of the West Antarctic ice sheet (Favier et al., 2014; Joughin et al., 2014; Rignot et al., 2014; Ritz et al., 2015). Once initiated, a yet not fully understood chain of feedback mechanisms may cascade: reduced buttressing of the upstream ice due to retreat causes ice speed-up, which leads to dynamic thinning and increased calving at the marine-terminating fronts, which in turn leads to further mass loss and retreat. Surface mass-balance processes do not trigger rapid changes directly, but enhanced surface melt has been identified as a precursor to catastrophic ice-shelf collapses (Banwell et al., 2013).
Overall, accelerated ice discharge into the oceans has tripled the mass loss of both ice sheets to 298 ± 58 Gt year−1 (0.83 ± 0.16 mm year−1) during 2000–2011, compared to the period 1992–2000 (Shepherd et al., 2012). Some estimates of multi-year averages of mass loss after 2009 exceed 350 Gt year−1 for Greenland (McMillan et al., 2014) and 150 Gt year−1 for Antarctica (Helm et al., 2014; Khan et al., 2015). Velicogna et al. (2014) found that the significant acceleration of ice sheet mass loss is driven mainly by a few subregions. Sutterley et al. (2014) found that the acceleration of mass loss in the Amundsen Sea area of West Antarctica is nearly 3 times larger during the period 2003–2009 than it was over 1992–2013.
The Fourth Assessment Report (AR4) of the Intergovernmental Panel on Climate Change (IPCC, 2007) pointed out that ice flow may be a key driver of rapid ice sheet change, but recognized that “quantitative projections cannot be made with confidence” mainly due to a lack of process understanding regarding rapid and possibly catastrophic and irreversible changes of ice sheets or parts thereof. The lack of adequate representation of these processes in the previous generation ice sheet models was considered the largest source of uncertainty in projecting twenty first century sea-level rise. In the wake of AR4 a wealth of new observations has been collected, and significant progress has been made in process understanding and the ability of models to account for couplings between ice sheets, ice streams and ice shelves, and their two-way interactions with the atmosphere, their subglacial environment and the ocean. However, models did not mature sufficiently for the Fifth Assessment Report (AR5; IPCC, 2013) to account explicitly for mass losses from rapid dynamic changes. Large uncertainties persist with regard to modeling and projecting ice sheet evolution and possible catastrophic contributions to sea-level change (Vaughan and Arthern, 2007).
Insufficient understanding of the mechanisms of the ice sheets' rapid dynamic changes remains the main culprit in the quest for better projections. Such changes cannot be triggered by the slow flow of ice by internal deformation, which is relatively well understood and represented in models. Hence rapid change can only be caused by interactions of the ice with its boundaries. Better understanding and proper implementation of the relevant processes, in particular at the ice-ocean and ice-bed interface, into predictive models are among the most critical challenges in reducing uncertainties in projections of the ice sheet contribution to sea-level rise.
Evidence is mounting that the ice-ocean interface is crucial to understanding rapid glacier change. Recent results indicate that much of the ablation at marine-terminating glaciers and beneath ice shelves is due to submarine melting rather than iceberg calving (Rignot and Jacobs, 2002; Bartholomaus et al., 2013; Truffer and Motyka, 2016), highlighting the role of the ocean, in particular ocean temperatures, in ice sheet and glacier behavior and adding further complexity to prognostic modeling. For example, Motyka et al. (2011) found specific melt rates exceeding 200 m year−1 beneath the floating tongue of Jakobshavn (Ilulissat) glacier, Greenland, in the mid-1980s. Melt rates increased by ~25% in the following decade. Holland et al. (2008) were among the first to recognize that ocean warming may play a major role in triggering the rapid changes in Greenland. Delivery of warm ocean waters to the glacier fronts increases submarine melt rates, which in turn precipitate a chain of feedbacks that lead to increased flow speeds, calving rates and ice discharge into the ocean. Recent observational studies indicate that near-terminus subglacial freshwater discharge exerts a major control on submarine melt rates (Motyka et al., 2013), confirming earlier theoretical (Jenkins, 2011), and numerical studies (Xu et al., 2012).
In addition to untangling the precise mechanisms at the ice-ocean boundary and their coupling, it is an even greater challenge to implement the complexity of the coupled processes of mechanical calving, submarine melt, and up-glacier feedbacks into prognostic models (O'Leary and Christoffersen, 2013; Straneo et al., 2013; Cook et al., 2014). Despite increased attention to the ice-ocean interface and unprecedented observational detail (Fried et al., 2015) the system is still not well understood; this poses significant challenges to modeling (Slater et al., 2015). Observations of all relevant components and an interdisciplinary approach including glaciologists and oceanographers will be key to success.
The glaciers outside the ice sheets are mainly driven by surface mass balance processes, but 38% of their total area drains through marine-terminating glaciers (Gardner et al., 2013). The role of these glaciers in global mass budgets remains largely elusive, although a few regional estimates exist (see summary in Huss and Hock, 2015). Unstable retreat similar to those observed on the ice sheet outlet glaciers has been observed on non-polar glaciers, such as Columbia Glacier in Alaska (McNabb et al., 2012). Hence, such glaciers provide valuable analogs for ice sheet processes (Post et al., 2011). Research at these far more accessible and logistically less challenging mountain glacier systems can help shed light on the processes that are responsible for rapid changes of the ice sheets' marine-terminating glaciers.
The basal boundary and its effects on ice flow are also poorly known, due to the complexity of the processes involved and the inaccessibility of the glacier bed. The presence of subglacial and englacial water add to the complexity (Chu, 2014); frictional drag at the bed can vary greatly in space and time in response to basal water fluctuations, as has been studied extensively for mountain glaciers (Iken and Bindschadler, 1986). Zwally et al. (2002) linked ice sheet flow acceleration in Greenland to basal lubrication caused by atmospherically induced increased melt reaching the glacier bed. The study triggered a wave of recent observational and theoretical investigations, and provoked much controversy on the role of the subglacial boundary in explaining rapid ice sheet changes (Meierbachtol et al., 2013). While some studies show substantial increase in surface speeds, in particular over land-terminating margins on a seasonal basis (Palmer et al., 2011), others show decreases in ice speed on multi-year time-scales, despite increased melt input (van de Wal et al., 2008; Sundal et al., 2011; Tedstone et al., 2015). These apparently conflicting results are consistent with the notion that subglacial drainage configurations and their efficiency to transmit water vary considerably in space and time (Fountain and Walder, 1998), triggering opposing responses in ice speed to increased water input.
While these results provide support that ice flow is affected by water at its bed, the collective evidence indicates that basal lubrication cannot explain the scope of the observed rapid outlet glacier changes in Greenland and Antarctica. However, the recent discovery of widespread connectivity of subglacial lakes below the Antarctic ice sheet and surprisingly rapid changes in lake storage by drainage into neighboring lakes (Wingham et al., 2006; Fricker et al., 2007) indicates that even in Antarctica, where surface melt is largely negligible, the lower boundary affects the slipperiness at the base of the ice sheet and thus ice speed. Model results indicate that 55% of the grounded part of the Antarctic ice sheet is at pressure melting point (Pattyn, 2010).
Despite recent promising theoretical advances, the inclusion of process-based subglacial hydrology models into ice sheet models is still in an early stage of development. Models generally do not account for water transport from the surface to the bed or lateral water flow along the ice-bed interface. Although some recent progress has been made (Schoof, 2010; Bueler and Pelt, 2015), substantial challenges remain in linking basal stresses to ice motion, and modeling the effect of increased meltwater input on ice discharge. A definitive sliding law, relating basal motion to basal stress and water pressure is still lacking, and may in fact not exist. This is partly due to the heterogeneity of the glacier bed, which can consist of relatively clean bedrock or subglacial till of various granularity.
Processes at the surface-atmosphere boundary (snow accumulation, surface melt) determine the surface mass balance, which constitutes another important boundary condition for glacier and ice sheet behavior. The physical processes are relatively well-understood (Hock, 2005); however, quantifying recent and future surface mass changes still presents a major challenge. For example, ice-sheet wide annual surface mass balances in Greenland derived from regional climate models deviate by up to a factor of two (e.g., Fettweis et al., 2008; Ettema et al., 2009), in particular due to difficulties in modeling snow precipitation (see Section Snow Accumulation). This problem is only exacerbated in the topographically complex mountain ranges that host non-polar glaciers.
Refreezing is a major component of the mass budget, in particular on ice sheets and high-latitude glaciers. Modeling indicates that ~40% of the total surface melt in Greenland may refreeze (Van Angelen et al., 2013). With atmospheric warming, refreezing may initially increase due to increased melt, but eventually it may decrease due to subsurface warming and decreasing pore space. Storage of water in firn may temporarily buffer the contribution of meltwater to sea-level rise (Harper et al., 2012). Modeling needs to account for the subsurface spatio- and temporal variability in temperature, water content and density; however, despite recent observational advances (Forster et al., 2014; Machguth et al., 2016), these processes are often oversimplified, and therefore poorly modeled in ice-sheet or climate models.
To account for feedbacks with the climate system through changes in surface elevation, albedo and freshwater input into the ocean, it is important to fully couple ice-sheet and (possibly also glacier) models to Atmospheric-Ocean General Circulation Models. However, currently most ice-sheet models are stand-alone models without two-way coupling (Vizcaino, 2014; Vizcaino et al., 2015). The necessary large computational resources are an additional barrier to progress in fully coupled modeling. Similarly, downscaling typically coarse-scale climate data to the glacier scale remains a major challenge in modeling and projecting mountain glacier behavior (Ziemen et al., 2016).
Lack of observational data is still a major issue in assessing and predicting change. Glaciological datasets are often short in duration or cover limited areas, although tremendous progress has been made recently. A wide suite of large-scale data sets of the Earth's glaciers at unprecedented spatial and temporal resolution have been collected in the last decade, including surface velocities (Rignot et al., 2011; Moon et al., 2012; Fahnestock et al., 2016), surface elevations (Howat et al., 2014), surface elevation changes (Pritchard et al., 2009), ice sheet bedrock (Bamber et al., 2013), and ice thicknesses (Fretwell et al., 2013). The first complete inventory of all glaciers outside the ice sheets, the so-called Randolph Glacier Inventory (RGI; Pfeffer et al., 2014) combining data from GLIMS (Global Land Ice Measurement from Space) (Raup et al., 2007; Kargel et al., 2014) with new data to achieve complete coverage globally, has removed a major obstacle in modeling these glacier systems. However, lack of accurate bed topography data, and thus initial ice volume, introduces considerable uncertainties in their modeling.
High-resolution data are needed in particular at the ice-ocean interface. In Greenland the fjord arms are largely unmapped, and in Antarctica, the topography under the ice shelves, which strongly affects sub-ice shelf melt rates (Hattermann et al., 2014), is poorly known. Also, too little is known about ocean properties and their short-term variability. Data collection is not trivial given that this domain is often choked with icebergs calling for the development of innovative data collection techniques, such as attaching instruments to deep-diving seals (Sutherland et al., 2013). Data revealing the past, for example, from ice or sediment cores, are essential to put current changes in context, and to validate models. Collecting data on basal drag, thermal conditions and subglacial waterflow at the subglacial boundary will remain difficult, if not impossible. But recent advances in inverting at least some of these properties from surface data are promising (McNabb et al., 2012; Morlighem et al., 2014; Brinkerhoff et al., 2016; Farinotti et al., 2017).
Snow is a fascinating mixture of ice, water, water vapor, and air. It is the most ephemeral part of the cryosphere, a fact that is intuitively appreciated when considering a dendrite of fresh snow in the palm of one's hand. Snow on Earth has a limited lifetime, because it either melts or consolidates into ice, and it is a highly dynamic material, which can change its density by an order of magnitude within days. Finally, fresh snow reflects almost all incoming short wave radiation, while it acts as an almost perfect black body in the infrared part of the spectrum.
Research on snow microstructure has exploded in recent years, because it is increasingly recognized that important mechanical, thermodynamical, and electromagnetic properties of snow cannot be predicted without a proper consideration of snow microstructure (Aoki et al., 2011; Lowe et al., 2013). Furthermore new observational technologies such as micro-computer-tomography (Schleef and Lowe, 2013), optical spectrometry (DUFISS) (Gallet et al., 2009) or snow micro-penetrometry (Lowe and van Herwijnen, 2012), have made it possible to quantify snow microstructural effects. What is missing is the development of a unifying theory, describing the physical properties and behavior of snow at a larger scale based on laws of snow microstructure development. While it is quite clear that such a theory will include—next to density—the specific surface area of the snow grains and curvature terms characterizing the snow—pore interface, it remains to be shown that a predictive microstructure model based on density, surface area and mean and/or Gaussian curvature is able to replace current more empirical microstructure models (Lehning et al., 2002). This step is currently being addressed in the snow microstructure community (e.g., Krol and Löwe, 2016) and will lead to the development of new snow models, which are able to describe mechanical and electromagnetic properties of snow in a more physical way.
Snow accumulation in mountainous regions, as well as on ice sheets and sea ice continues to be insufficiently understood (see also Section Surface Processes). The mountain snowpack is a major source of freshwater for many arid and semi-arid regions worldwide, but researchers still struggle to reliably estimate the amount of snow stored in the high alpine regions and how much water can be expected downstream. A major source of uncertainty comes from the fact that measuring (snow) precipitation in the high alpine zone is extremely difficult, if not impossible, given the windy conditions and limited infrastructure available in these areas (Sevruk and Mieglitz, 2002; Sevruk et al., 2009). Recent progress in remote sensing of snow depth distribution is helping to put more constraints on mountain snow cover and precipitation. The analysis of spatial snow depth maps has revealed reduced snow amounts at high elevations (Grunewald et al., 2014; Kirchner et al., 2014), but scientists are only starting to investigate the links to precipitation patterns (Mott et al., 2014). It is therefore critically important to intensify efforts to better quantify precipitation and related available snow and water resources in the high alpine zone.
The problems described above are aggravated in polar regions, particularly in Antarctica, due to continuous high winds and low temperatures. Smaller errors in snow accumulation lead to large errors in the total ice sheet mass budget due to the enormous area of the ice sheet (Zwally and Giovinetto, 2011). Errors in accumulation estimation stem from very sparse measurements of precipitation in both polar regions together with an unknown accuracy of precipitation predictions by weather models. Wind-blown snow adds uncertainty; it results either in redistribution or loss of snow (e.g., open water leads in sea ice). Drifting and blowing snow also results in an unknown amount of sublimation, reducing the total mass before final deposition.
Larger-scale models of ice sheets, glaciers, and sea ice typically treat snow processes at the surface of these ice masses in a rudimentary way, and at an inadequate resolution for calculating, for example, a flux divergence of blowing and drifting snow. While the most advanced models such as MAR (Gallee et al., 2013; Amory et al., 2015) or RACMO (Lenaerts et al., 2012) implement parameterizations of the complex snow processes, quantitative validation is challenging. The community agrees that potential calculation errors are large, and critically influence the modeled total mass balance. One of the most critical processes is drifting and blowing snow, but it is largely unknown how much of the snowfall is permanently deposited and ultimately incorporated in the ice mass (Zwaaftink et al., 2013). Only recently have regional climate models, applied to the ice sheets, started to include a more physical description of firn processes (Van Angelen et al., 2013) and snow redistribution by wind (Lenaerts et al., 2012).
Snow melt and energy balance have been investigated over decades and are generally well understood. However, snow melt models often rely on erroneous meteorological input data (Schlögl et al., 2016), either because the measurements are spatially not representative or because input is taken from meteorological models, which insufficiently resolve boundary layer feedbacks. These feedback effects have been studied over glaciers with respect to katabatic wind formation and associated temperature effects (Greuell and Böhm, 1998; Shea and Moore, 2010). Recent results show how local flow features can change the turbulent heat fluxes (Mott et al., 2015), and that terrain sheltering has significant small-scale effects on melt efficiency (Mott et al., 2016). It is generally accepted that regional melt and therefore also catchment runoff (Cullather et al., 2016) can be well described with calibrated models, often using empirical temperature index methods for snow melt. At the same time, physics-based energy balance models, which are preferable for their transferability to other environments and future climates, have shown a high sensitivity to meteorological input (Schlögl et al., 2016). This remains a challenge to be addressed in the future.
Snow Representation in Earth System, Climate and Weather Models
The discussion above already suggests some of the difficulties in dealing with the thin and highly dynamic yet important snow component in larger-scale models. Misrepresenting the massive influence that snow exerts on the atmosphere and the soils will strongly bias model results (Beer, 2016). Snow representation in larger-scale models generally does not correctly reproduce the effect of snow on the atmosphere or ground correctly (Van Angelen et al., 2012). To limit the detrimental effect of an insufficient snow representation, some meteorological models (e.g., COSMO, Baldauf et al., 2011) assimilate snow-covered area, which can be estimated from a combination of ground and satellite observations. This produces acceptable results for short-term forecasting, but it remains a challenge to have an adequate representation of snow dynamics in larger-scale models. Assimilation also does not solve the problem of insufficiently representing the effects of snow on other model components.
Snow and Climate Change
Global warming naturally has a large impact on snow dynamics impacting the duration of snow cover and timing of runoff production. Anticipated changes include a shift from snow to liquid precipitation and a potential increase in total precipitation (Lenaerts et al., 2013). More snow accumulation may offset increased ablation of ice sheets as long as it remains sufficiently cold, as has been shown to be important locally in certain regions (e.g., Schmucki et al., 2015). However, future snow changes are currently not modeled well on a global scale. Due to the difficulty to correctly represent snow dynamics in climate models, as discussed above, it is challenging to make reliable predictions on future snow and its feedback effects on the atmosphere and soils. Locally, water resources and tourist industries are affected by future snow changes. Globally, sea level rise and positive feedback mechanisms via release of carbon or methane following permafrost thaw are of major concern.
Sea ice covers between 4 and 6% of the Earth's oceans, with a large seasonal cycle that profoundly impacts the climate of the polar regions and planet. Seasonality and interannual variability of pack ice differ between the poles. The Arctic Ocean is confined by land, such that its seasonal cycle in ice cover has smaller amplitude than the Southern Ocean (Eisenman, 2010). The Arctic experiences a continental climate in winter as the sea-ice pack impedes heat and moisture fluxes to the atmosphere. In contrast, the Antarctic sea-ice pack is constrained by the circumpolar current, extends to lower latitudes, and experiences heavier snowfall, which contributes to ice mass and a larger seasonal cycle in ice extent.
Sea ice plays an important role in regulating global climate. Loss of ice amplifies changes in radiative forcing, enhancing ice loss and warming, and thus represents a positive feedback in a warming climate. The loss of sea ice is attributed to be one of the main factors explaining the Arctic Amplification (Screen and Simmonds, 2010), in which surface temperature increases are observed to be twice as large in the Arctic compared to the global average (Polyakov et al., 2003; Bekryaev et al., 2010). Sea-ice loss increases solar absorption in the ocean (Perovich et al., 2011) and momentum transfer from wind into the ocean (Martin et al., 2014), leading to the speculation that sea-ice variability can be linked to multi-decadal variability in ocean circulation (Giles et al., 2012).
Identifying the magnitude and direction of feedbacks involving the ice surface energy balances in the current, past and future climates is central to unraveling the role of sea ice in the Earth's climate system. These feedbacks control seasonal, interannual, and longer-scale variability of the sea-ice pack, and their related climate sensitivities impact the polar oceans, atmosphere, land and ecosystems; and hence global climate.
Recent Sea-Ice Changes
There has been over 50% loss of sea-ice volume from the Arctic since 1979 (Schweiger et al., 2011; updated to 2015), which is primarily manifested as a loss of perennial ice area (Maslanik et al., 2011) through enhanced transpolar ice drift events (Nghiem et al., 2007), export to the Greenland-Iceland-Norwegian Sea (Smedsrud et al., 2017), and increased melting within the Arctic (Kwok and Cunningham, 2010). The Antarctic has experienced a slight increase in sea-ice extent, but with large zonal variability, with increasing ice extent in the Ross Sea and decreasing extent in the Amundsen-Bellinghausen Sea (Turner et al., 2015). Less is known regarding variability in Antarctic ice thickness and volume.
The decrease in Arctic sea ice is happening at a time of increasing economic interest in mineral exploration, transport and tourism across the region (AMAP, 2004). There is increasing need for improved ice forecasting and accurate projection for strategic planning, as expected changes may increase hazards to human activity in the sea-ice pack (Stewart et al., 2007). The time scale needed to assist governmental and industry planning range from 10 to 50 years ahead. This presents one of the largest challenges to the sea-ice observers and modelers: non-linear dynamics in the climate system impede model predictions of the sea-ice change over timescales longer than 2–10 years (Blanchard-Wrigglesworth et al., 2011; Guemas et al., 2014).
Until recently, one of the most significant challenges of the sea-ice community has been global observation of ice thickness. With satellite monitoring of ice thickness now available (Laxon et al., 2003), the challenge has moved to understanding biases in the measurement method. This has led to a need to better characterize the snow cover on sea ice, as a lack of information about snow thickness is the largest cause of uncertainty in sea-ice thickness measurements (Kwok and Cunningham, 2008). The lack of information about ice thickness is no longer the leading cause for uncertainty in appropriate model parameterizations. Uncertainty in projection of sea-ice change over the coming century is mainly attributed to a number of physical processes, outlined in Section Observation and Model Needs, that are inadequately constrained by current observational data.
Sea Ice in Climate Models
The observed recent changes in Arctic sea-ice pack are better represented in the climate models of IPCC's AR5 compared to AR4 due to improvements to sea-ice thermodynamic parameterizations in AR5 (Stroeve et al., 2012). However, these improvements have not decreased the spread in model realizations. Part of the uncertainty lies in natural variability in the Earth system, since predictions of sea ice are most uncertain on decadal timescales (Blanchard-Wrigglesworth et al., 2011).
Attribution of recent sea-ice loss in the Arctic has been called a “Grand Challenge” of climate science (Kattsov et al., 2010). To meet this challenge, we need to be able to accurately simulate the seasonality in the feedbacks controlling sea-ice mass balance. To do so we need better observational data constraining these feedbacks, which are related to coupled processes between the upper ocean, sea ice and atmosphere. In particular we do not know how heterogeneity in the sea-ice cover impacts the radiative, sensible and latent heat fluxes from the surfaces. Uncertainty in cloud properties results in significant uncertainty in downwelling longwave radiation flux at the ice-ocean surface.
Uncertainty in the Surface Energy Balance of Sea Ice
Sea-ice has the largest seasonal cycle in mass of all cryosphere components. This seasonality is controlled by the balance of positive and negative feedbacks to ice thickness that change over the year as the surface energy balance goes from net positive in summer to negative in winter. Interannual variability in sea-ice thickness reflects variability in atmosphere and ocean, and indicates high sensitivity of the sea-ice cover to the surface energy balance. The average change in heat budget to explain the loss of ice over the last three decades is only about 1 Wm−2 (Kwok and Untersteiner, 2011). Attribution of this additional heat is a matter of current debate.
Positive feedbacks on sea-ice loss are numerous, and are counteracted by the large negative feedback caused by ice thickening in winter. Representing the variability from these competing processes is important for correctly modeling climate sensitivity (Notz, 2015). Carmack et al. (2015) document the terms that have most uncertainty in the sea-ice surface energy budget. The atmospheric flux components introduce an order of 10 Wm−2 uncertainty, which is more than enough to explain recent ice loss. Inability to constrain these fluxes in models contributes to the wide variability in sea-ice seasonality, interannual variability and trends in climate models. The uncertainty in ocean heat flux to the sea-ice pack is another, smaller, yet significant contributor.
A review of recent advances in parameterizing sea ice-atmosphere processes is presented by Vihma et al. (2014). Carmack et al. (2015) include a review of sea ice-ocean processes. Climate model sensitivity is related to the representation of sea-ice processes, and models present wide variability in their representation of the sensitivity of sea ice to greenhouse gas forcing (Stroeve and Notz, 2015). The processes that contribute to this uncertainty are outlined below.
Observing recent changes of the sea-ice pack give us some indications, though not conclusive, of the feedbacks driving these changes. We know that solar absorption through the increasing open water area in the Arctic during summer (Perovich et al., 2011) may be increasingly delaying freeze-up for areas of the northern hemisphere ice pack (Steele et al., 2010; Jackson et al., 2012; Timmermans, 2015). This is associated with an increase in oceanic heat and moisture flux to the atmosphere, with unknown impacts on atmospheric stability (Overland and Wang, 2010). At the same time, the sea-ice pack is more open, and its areal extent reduced, increasing wind-tress transfer into the ocean (Martin et al., 2014). Increased wind combined with increased geostrophic ocean currents around the Beaufort Gyre since 2007 (Giles et al., 2012; McPhee, 2013) are linked to increased ice drift rates in the Beaufort Sea (Petty et al., 2016), and to pooling of freshwater in the upper water column, increasing stratification, in the Canada Basin (Morison et al., 2012). Decreasing sea-ice mass implicit from the observational evidence has been associated with: changes in ice drift (Rigor and Wallace, 2004; Nghiem et al., 2007) and increased divergence of the pack (Hutchings and Perovich, 2015), both of which precondition the pack for enhanced melt; changes in cloudiness (Kay et al., 2008), which affects both shortwave and longwave radiation balance; and increasing Pacific summer water inflow to the Chukchi Sea (Shimada et al., 2006; Woodgate et al., 2010, 2012). Also, an increasing Atlantic water inflow to the eastern Arctic (Polyakov et al., 2012) is another heat source, that may reach the ice through various mixing mechanisms (Carmack et al., 2015). Variability in Atlantic water in the Arctic may be related to the Atlantic Multidecadal Oscillation and a similar period of oscillation in the sea-ice pack (Miles et al., 2014). Heat released from the Atlantic water has recently been identified as a significant contributor to sea-ice loss (Polyakov et al., 2017).
Perhaps the most fundamental gap in our knowledge of sea-ice feedbacks relates to our poor understanding of polar clouds. Kay and Gettelman (2009) find that changes in cloud cover cannot explain the increasing ice-albedo feedback during summer, but they probably contribute to increasing longwave cloud feedback in fall. This longwave feedback is particularly difficult to model. The distribution of ice and water droplet size distribution is not well known in Arctic clouds; the sensitivity of sea ice in fully coupled models to this uncertainty in cloud parameterization is as large as the observed sea-ice reduction (Karlsson and Svensson, 2013; Pithan et al., 2014). Our inability to constrain one of the leading-order terms in the ice-ocean surface energy budget, can result in model ranges for ice thickness much different from those observed. Limitations in our knowledge of Arctic cloud composition are such that cloud parameterizations are weakly constrained, and cloud longwave emission biases may be offset by biases in the sea-ice model. In summer, the longwave feedback is closely connected to the albedo feedback (Karlsson and Svensson, 2013), as increasing ice loss results in increasing longwave emission from the surface and moisture flux to the atmosphere.
From the leading-order problem of resolving cloud properties and the downwelling longwave radiation, there is an array of cascading uncertainties, with the surface-cloud feedback being dependent on several physical processes that may be inaccurately parameterized in models. This leads us to another fundamental feedback in the system, the ice-albedo feedback. The albedo of sea ice may be biased in models as we do not consider the disparate evolution of melt pond fraction on ice of varying type and surface roughness (Fetterer and Untersteiner, 1998), snow cover (Petrich et al., 2012; Skyllingstad et al., 2015), and time in the melt season (Eicken et al., 2004). The spatial variability of the ice surface morphology is not well-represented at the sub-grid scale in climate models, and the seasonal transitions of this surface and its albedo are only recently being considered in models (Flocco et al., 2010). Observations suggest changes in melt-pond coverage may be an important component of the recently observed Arctic sea-ice loss (Flocco et al., 2012; Rösel and Kaleschke, 2012), since light transmittance through ponds enhances ice melt (Itoh et al., 2011; Nicolaus et al., 2012). Parameterization of melt ponds relies on knowing the ice surface morphology and snow cover, which are controlled by the continuous deformation of the sea-ice pack and snow blowing over the rough surface.
In considering the large positive feedbacks in the sea-ice system the reader is probably wondering why the Arctic has not lost its sea ice entirely. As mentioned earlier, there are strong negative feedbacks in the sea-ice system balancing the strong positive feedbacks (Notz, 2015). Some of these feedbacks increase as we move from a perennial to a seasonal sea-ice pack. Rapid ice growth at the onset of winter recovers the pack to a near equilibrium level ice thickness within several months. Ice is insulating, and snowfall insulates further, such that open water and thin ice regions grow ice faster than regions of thicker snow and ice.
Increasing positive feedbacks to ice melt are offset by increased ice growth. The enhanced seasonal cycle in ice volume results in increased amplitude of the seasonal cycle in freshwater input and uptake from the upper ocean, while increasing brine rejection. This potentially increases stability of the upper ocean, which is a negative feedback to ice loss. In the Antarctic, this mechanism may actually be assisted by the injection of continental ice sheet meltwater into the upper ocean (Bintanja et al., 2013), hindering heat flux to the ice base and increasing ice thickness regionally. It is river inflow into the Arctic, and the formation of a halocline that allows a perennial ice cover to exist (Carmack, 1990), and freshwater pooling in the Canada basin is a negative feedback that helps sustain the sea-ice pack.
Upper-Ocean Heat Budget
While ocean stratification is a large-scale feature, there is considerable spatial heterogeneity in the sea-ice basal melt rate (Maykut, 1982). Variable ocean-ice heat flux (e.g., Krishfield and Perovich, 2005; McPhee et al., 2005) has several causes. Sea ice melt creates a fresh layer at the top of the ocean that is warmed by solar energy, and further melts ice [discussed for example in Vivier et al. (2016)]. This heat also becomes entrained into a near surface layer of warm water (Jackson et al., 2010) which is mixed upwards during storms (Jackson et al., 2012; Zhang et al., 2013), melting ice or delaying ice freeze-up. Other oceanic dynamic processes can bring heat upward from depth transported into the Arctic from the Atlantic and Pacific (Carmack et al., 2015). Processes that provide the majority of heat flux to the ice are micro- and mesoscale. Quantifying the partitioning of solar input to the upper ocean between ice melt and delay in freeze up requires parameterization of these stratification and mixing processes.
Preconditioning the Sea Ice-Ocean Energy Budget
Feedbacks related to sea-ice loss or growth are modulated by the thickness distribution of the sea-ice pack, which influences atmospheric and ocean drag. The ice thickness distribution and roughness is controlled by the history of ice drift and horizontal deformation (divergence and shear), growth and melt. The deformation occurs through plastic failure, whereby pack ice can only sustain stresses below its strength without permanent deformation. This is a dissipative term in the kinetic energy balance. In the momentum balance the divergence of the ice stress field is called the ice interaction, and the relationship between stress and deformation follows a rheological model. This parameterization of deformation of sea ice is poorly constrained, due to the difficulty in defining ice strength on the scale of model grid cells.
Model ice strength is typically related to the ice thickness, which is an indication of ice age and hence the properties that impact strength, including salinity and microstructure of the ice. However these relationships have not been assessed in the context of the model ability to simulate features key to the surface fluxes (leads fraction for example). Surface roughness is typically neglected when calculating oceanic and atmospheric drag on the ice, although a parameterization has been implemented in one sea-ice model (Tsamados et al., 2014). The ice interaction term, and drag parameterizations for wind and ocean surface stresses in the force balance on pack ice are often tuned in models to best reproduce observed ice drift, extent, and thickness. This does not ensure deformation fields are accurately simulated (Kwok et al., 2008), or that wind stress is appropriately partitioned between driving ice deformation and ocean currents, which has implications for the surface energy balance. For example, increased opening may result in enhancement of the albedo feedback (Hutchings and Perovich, 2015).
Misrepresentation of ice kinematics profoundly impacts the redistribution of ice thickness to thin (lead) and thick (ridged/rafted) ice. Dynamic thinning or thickening of pack ice is either a positive or negative feedback to the end of summer ice volume, but the nature of these feedbacks is currently not well known.
Observation and Model Needs
In order to simulate observed variability in the sea-ice pack volume, the ice and ocean surface energy balance needs to be accurate. This requires accurate simulation of all the competing feedbacks in the system, which range from strongly negative to strongly positive. Parameterizing these processes will require improved observations. In particular there is need for: improved knowledge of the composition of Arctic clouds throughout the year; identification of melt pond fraction and the processes driving melt pond evolution on ice of varying topography and snow cover; improved representation of sea-ice deformation in models; and improved understanding of how heterogeneity in sea ice impacts atmospheric and oceanic stability and related fluxes across the ice surface.
At the heart of improving the representation of the sensitivity of sea ice to the surface energy balance is improving our ability to realistically simulate interannual variability in sea-ice mass. Climate models extending into the next century project ice loss events that occur on similar timescales as the reduction in Arctic ice volume observed in the last decade (Holland et al., 2006). Diagnosis of feedbacks controlling such events shows a variety of mechanisms that enhance ice loss (Holland et al., 2006; Vavrus et al., 2011). Climate models on average demonstrate lower sea-ice sensitivity to climate forcing than observations suggest. So while the IPCC model ensembles represent a large spread in future projection of sea-ice state, one can question whether this spread of realizations is realistic given that positive and negative feedbacks to ice mass in the system are likely to be larger than simulated.
Identifying the magnitudes of the leading order feedbacks in the climate system is crucial to improve climate model capabilities in projecting climate changes. The nature of sea-ice loss events, the rate of ice change and interannual variability is controlled by feedbacks that are poorly constrained in climate models. Rapid ice loss events are highly likely, and we are currently experiencing one. The time scale and mechanisms for these events are poorly resolved in current climate models.
Synthesis: Facing the Challenges
All components of the cryosphere are currently undergoing rapid changes in response to atmospheric warming, and the challenges here are multi-faceted. Major challenges in the quest for better predictability of the cryosphere remain in three main areas that are intrinsically connected: observations, process understanding and modeling capabilities. Tremendous progress in observational capabilities, in particular due to recently launched satellites, such as GRACE, CryoSat-2 and Sentinel-2, has enabled us to measure and monitor cryospheric changes at unprecedented spatial and temporal scales. Despite these advances there is a pressing need for more high-resolution and high-quality data. Field campaigns need to be focused in critical areas to address the major deficits in our understanding of processes and feedbacks within the climate-cryosphere system that are critical for modeling future change. Rather than studying individual components in isolation, this is best accomplished in a “system approach” at carefully chosen study sites that include all relevant system boundaries and interactions (e.g., climate-ocean-cryosphere).
Specific aspects, such as characterizing polar clouds and the impact of changing morphology on sea-ice albedo, are disciplinary problems. Yet there is an increasing need to coordinate across disciplines to quantify relevant processes and feedbacks in the system. For example, sea-ice dynamics can be both a negative and positive feedback to summer ice loss that varies spatially, seasonally, and with ice morphology. A pack of increased mobility may open more growing areas of thin ice that melt out early in the melt season, enhancing summer ice melt; but the pack may also open and close more to create larger areas of thicker, ridged, and eventually hummocked ice that is more resilient to complete melt. To characterize the magnitude of these feedbacks requires coordinated instrumental deployments by those studying sea-ice dynamics, sea-ice thermodynamics, atmospheric boundary layer processes, and the upper ocean. Similarly, advancing process understanding of the driving mechanisms of rapid glacier changes requires targeted field campaigns at the critical ice-ocean interface involving both glaciologists and oceanographers. This requires a paradigm shift in the design of field campaigns (Carmack et al., 2015; Shupe et al., 2016).
We also need to communicate and acknowledge the need for increased diversity and inter-disciplinary focus in the cryospheric research community, where cryospheric, ocean, atmospheric, and other geoscientists, including both observers and modelers, collaborate closely. Models can guide our data collection efforts, providing insight into where best to focus limited resources. By more fully integrating modeling teams into observational programs we can develop the unified monitoring and modeling needed to address the most pressing challenges. Data need to be well-documented and made freely and rapidly available. However, managing the increasing amounts of data, which cover larger scales and come at ever higher resolution, will require technical innovations and international coordination to meet the demands of the scientific community.
Among the many outstanding issues outlined above, perhaps the most important “Grand Challenges” in glacier, snow and sea-ice research pertain to incomplete process understanding, in particular inadequate understanding of ice-ocean interactions and glacier basal boundary conditions; drifting and blowing snow as well as snow microstructure and their effect on the physical behavior at larger scales; and the complex feedback mechanisms controlling sea-ice variations, in particular the polar-cloud feedback. In light of recent rapidly accelerated mass losses and indications of a possibly ongoing irreversible collapse of the marine-based West Antarctic ice sheet, perhaps the most urgent challenge relates to a better understanding of ice sheet dynamics in this region and resulting consequences for sea-level rise.
Some challenges are common to glacier, snow and sea-ice research. Often relevant processes occur at a wide range of spatial and temporal scales, but control the behavior of the system on broader scales. For example, recent research has shown that ice-ocean interactions on large scales are influenced by processes at spatial scales of a few meters and temporal scales of minutes, for example, when buoyant plumes rise due to sudden release of fresh water from the bottom of a grounded tidewater glaciers (Xu et al., 2013). Similarly, a short storm can form sastrugis and change snow mass and surface roughness on sea ice (Trujillo et al., 2016) with potentially long-lasting consequences on sea-ice movement over large scales. Hence, incorporating small-scale processes into large-scale predictive models to an extent necessary to predict the system as a whole is a major task for future generation models. Another example for a challenge common to all three subdisciplines is the coupling of stand-alone models for individual components of the climate-cryosphere-ocean system in innovative ways such that feedbacks can be accounted for.
The challenges discussed here will require a concerted effort across disciplines and national boundaries. Many recent scientific findings have taken the cryospheric community by surprise defying previous common wisdom. Keeping an open mind for more surprises to come will be crucial to advance cryospheric sciences. Our field is well-equipped to address these challenges in unprecedented multi-disciplinary and collaborative manners.
RH led the study. JH and ML wrote the sea-ice and snow chapter, respectively, and RH wrote the remaining chapters. All authors provided comments and edits on the entire manuscript.
RH was supported by NSF grants #1604058 and #1543432. JH was supported by ONR award number N000141210470. ML was supported by the Swiss National Science Foundation.
Conflict of Interest Statement
The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.
Comments by M. Truffer, A. Aschwanden, and C. Kienholz and a thorough review by Jack Kohler helped to improve the manuscript.
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Keywords: cryosphere, glaciers, ice sheets, snow, sea ice, modeling, climate
Citation: Hock R, Hutchings JK and Lehning M (2017) Grand Challenges in Cryospheric Sciences: Toward Better Predictability of Glaciers, Snow and Sea Ice. Front. Earth Sci. 5:64. doi: 10.3389/feart.2017.00064
Received: 07 November 2016; Accepted: 20 July 2017;
Published: 14 August 2017.
Edited by:Valerio Acocella, Roma Tre University, Italy
Reviewed by:Steven L. Forman, Baylor University, United States
Nick Van De Giesen, Delft University of Technology, Netherlands
Tómas Jóhannesson, Icelandic Meteorological Office, Iceland
Copyright © 2017 Hock, Hutchings and Lehning. This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) or licensor are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.
*Correspondence: Regine Hock, firstname.lastname@example.org