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Mass Balance of the Antarctic Ice Sheet 1992–2016

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Mass Balance of the Antarctic Ice Sheet 1992–2016 Journal of Glaciology Mass balance of the Antarctic ice sheet 1992–2016: reconciling results from GRACE gravimetry with ICESat, ERS1/2 and Envisat altimetry Article Cite this article: Zwally HJ, Robbins JW, H. Jay Zwally1,2 , John W. Robbins3, Scott B. Luthcke4, Bryant D. Loomis4 Luthcke SB, Loomis BD, Rémy F (2021). Mass balance of the Antarctic ice sheet 1992–2016: and Frédérique Rémy5 reconciling results from GRACE gravimetry with ICESat, ERS1/2 and Envisat altimetry. 1Cryospheric Sciences Laboratory, NASA Goddard Space Flight Center, Greenbelt, MD, USA; 2Earth System Science Journal of Glaciology 67(263), 533–559. https:// Interdisciplinary Center, University of Maryland, College Park, MD, USA; 3Craig Technologies, NASA Goddard Space doi.org/10.1017/jog.2021.8 Flight Center, Greenbelt, MD, USA; 4Geodesy and Geophysics Laboratory, NASA Goddard Space Flight Center, 5 ’ Received: 31 December 2019 Greenbelt, MD, USA and Laboratoire d Etudes en Geophysique et Oceanographie Spatiale (Legos), Toulouse, France Revised: 8 December 2020 Accepted: 23 December 2020 Abstract First published online: 29 March 2021 GRACE and ICESat Antarctic mass-balance differences are resolved utilizing their dependencies Key words: on corrections for changes in mass and volume of the same underlying mantle material forced by Antarctic glaciology; climate change; ice ice-loading changes. Modeled gravimetry corrections are 5.22 times altimetry corrections over dynamics; ice-sheet mass balance; laser East Antarctica (EA) and 4.51 times over West Antarctica (WA), with inferred mantle densities altimetry −3 4.75 and 4.11 g cm . Derived sensitivities (Sg, Sa) to bedrock motion enable calculation of δ – Author for correspondence: motion ( B0) needed to equalize GRACE and ICESat mass changes during 2003 08. For EA, H. Jay Zwally, E-mail: [email protected] δ − −1 −1 − −1 B0 is 2.2 mm a subsidence with mass matching at 150 Gt a , inland WA is 3.5 mm a − − − at 66 Gt a 1, and coastal WA is only −0.35 mm a 1 at −95 Gt a 1. WA subsidence is attributed to low mantle viscosity with faster responses to post-LGM deglaciation and to ice growth during Holocene grounding-line readvance. EA subsidence is attributed to Holocene dynamic thicken- − − ing. With Antarctic Peninsula loss of −26 Gt a 1, the Antarctic total gain is 95 ± 25 Gt a 1 during − 2003–08, compared to 144 ± 61 Gt a 1 from ERS1/2 during 1992–2001. Beginning in 2009, large increases in coastal WA dynamic losses overcame long-term EA and inland WA gains bringing − Antarctica close to balance at −12 ± 64 Gt a 1 by 2012–16. List of symbols and units Symbol Meaning Usual units ρx Density of material: ρice (ice below the firn), ρearth (Earth dimensionless, material involved in GIA correction), ρa (new firn from relative to water − accumulation variations distributed over range of depths) (1 g cm 3) − M(t), dM/dt Total mass time series, rate of change Gt, Gt a 1 or mm w.e., − mm w.e. a 1 −1 Ma(t), dMa/dt Component of mass change from variations in Gt, Gt a or mm w.e., − accumulation rate: time series, rate of change mm w.e. a 1 − A(t) Accumulation rate mm w.e. a 1 − δA(t) Variations in accumulation rate (A(t) - <A(t)>) mm w.e. a 1 −1 Md(t), dMd/dt Component of mass-change from ice dynamics: Gt, Gt a or mm w.e. − time series, rate of change mm w.e. a 1 − dB/dt Bedrock elevation-change rate mm a 1 − H(t), dH/dt Time-series, rate of change of surface elevation mm, mm a 1 −1 −1 GIAcor Glacial Isostatic Adjustment correction Gt a or mm w.e. a −1 −1 dBcor Correction to dH/dt for bedrock motion (dB/dt) Gt a or mm w.e. a RatioG/dB Ratio of GIAcor to dBcor dimensionless −1 (Sg)md Sensitivity of gravimetry to bedrock motion for Gt mm model md (Iv=Ivins, Pe=Peltier, Wh=Whitehouse) −1 Sa Sensitivity of altimetry to bedrock motion Gt mm −1 δB0-md Rate of bedrock uplift or subsidence needed to provide mm a the GIAcor and dBcor needed to bring gravimetry and altimetry measured dM/dt (with no GIAcor nor dBcor applied) into agreement using (Sg)md and Sa −1 δBadj-md Same as above, but using dM/dt with modeled GIAcor mm a and dBcor already applied − © The Author(s), 2021. Published by δB’ Estimated long-term effect on the rate of bedrock motion mm a 1 Cambridge University Press. This is an Open caused by a long-term dynamic thickening/thinning Access article, distributed under the terms of h(xi,yr,ti) ICESat-based surface elevation at cross-track length units the Creative Commons Attribution licence positions xi and yr (172 m spacings) on the reference (http://creativecommons.org/licenses/by/4.0/), track at time ti derived from repeat-track analysis which permits unrestricted re-use, αd Cross-track slope dimensionless distribution, and reproduction in any medium, hr(ti) Surface-elevation time series at reference point length units provided the original work is properly cited. Hj,k(ti) ICESat surface-elevation time series for grid length units cell (j,k) H(t) Time series (ti) of surface elevation from area integration length units cambridge.org/jog of hr(ti) over 50 km grid cells, drainage systems, or regions Downloaded from https://www.cambridge.org/core. 29 Sep 2021 at 05:13:42, subject to the Cambridge Core terms of use. 534 H. Jay Zwally and others Hd(t) Time series of surface elevation driven by ice dynamics length units Ha(t) Surface elevation changes driven directly by length units contemporary accumulation variations CA(t) Surface-elevation change from changes in firn-compaction length units rate driven by variations in accumulation rate CT(t) Surface-elevation change from changes in firn- length units compaction rate driven by variations in near-surface firn temperature CAT(t) Surface-elevation change from changes in firn- length units compaction rate driven by the combined effect of variations in accumulation and firn temperature a a H CA(t) Combination of elevation changes directly by H (t) length units accumulation variations and accumulation-driven a a changes in firn compaction rate (HCA(t) = H (t) + CA(t)) −1 −1 (dM/dt)eq-md Mass change rate after bringing gravimetry and Gt a or mm w.e. a altimetry estimates into agreement using (Sg)md and Sa with either δB0-md or δBadj-md The agreement has been generally better in WA. However, the 1. Introduction behavior in the coastal portion (WA1) is dominated by dynamic The major portion of the East Antarctic (EA) ice sheet (Fig. 1)has losses and is markedly different from the mostly inland portion been dynamically stable for many millennia, as currently shown by (WA2) that has significant dynamic thickening, of which some the 800 000-year-old-basal ice at Dome C (Jouzel and others, 2007) is similar to the thickening in EA (Zwally and others, 2015). and the million-year ice at marginal blue ice areas (Sinisalo and The mass balances of both EA and WA are also significantly Moore, 2010). Surviving through major cycles of climate change affected by decadal variations in accumulation such as those between the 1992–2001 ERS1/2 period and the 2003–08 ICESat with cold-glacial and warm inter-glacial periods, changes in the − period: (a) the regional shift in EA of +21 Gt a 1 in EA1 and marginal extent and the inland thickness of the EA ice sheet − −21 Gt a 1 in EA2, and (b) an increase in WA snowfall that offset have been small compared to changes in the West Antarctic − (WA) and Greenland ice sheets (e.g. Denton and Hughes, 1981; 50% of the increased losses of 66 Gt a 1 from enhanced dynamic Denton, 2011; Mackintosh and others, 2011; Bentley and others, thinning on accelerating outlet glaciers in WA1 and the Antarctic 2014; Pollard and others, 2017). In contrast to EA, much of WA Peninsula (AP) (Zwally and others, 2015). Therefore, determin- is grounded 1000 m below sea level, has a maximum surface eleva- ation of both the short-term accumulation-driven and the long- tion of 2000 m (only half of EA), may be susceptible to dynamic term dynamic-driven components of ice-sheet mass balance is instabilities, and has a more uncertain and complicated long-term critically important for understanding the causes of changes on history, including its major retreat after the Last Glacial Maximum various time scales and the ice sheet’s ongoing- and future- (LGM) and partial re-advance of the grounding lines during the contributions to global sea-level change. Holocene (Kingslake and others, 2018). In their Figure 3, Hanna and others (2020) show the variation In general, variations in the total mass (M(t)) of the Antarctic in the estimates of Antarctic dM/dt from 1990 to 2018 obtained ice sheet (AIS) are the sum of short-term (≲decades) by the three principal methods (altimetry, gravimetry and – accumulation-driven variations (Ma(t)) in the surface mass bal- input output method), which is updated from a similar figure ance and sub-decadal to millennial dynamic variations (Md(t)). in Hanna and others (2013). For EA, those reviews, as well as Dynamic changes in ice velocity occur for various reasons such the multi-investigator results (Shepherd and others, 2018)from as changes in ice-shelf back-pressure, basal sliding or long-term the second Ice Sheet Mass Balance Inter-comparison Exercise (IMBIE), clearly show outliers on both sides of the means, changes in accumulation rate that cause changes in ice thickness − and surface slope that drive long-term changes in velocity.
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