Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 3 Discussions The Cryosphere , and J. L. Smellie 1 (2001–2009). Tidewater 1 − a 2 , M. J. Hambrey 1 3542 3541 erence is largely a result of orographic temperature ff (1988–2001) to 2.4 km , N. F. Glasser 1 2 − a 2 , J. L. Carrivick . This east-west di 1 1 − a 2 This discussion paper is/has been under review for the journal The Cryosphere (TC). Please refer to the corresponding final paper in TC if available. Centre for Glaciology, Institute for Geography and Earth Sciences, AberystwythDepartment University, of Geography, University of Leeds,Department Leeds of LS2 Geology, 9JT, University UK of Leicester, Leicester LE1 7RH, UK the Eastern Antarctic Peninsula willablation areas attain are more removed. stable frontal positions after low-lying and precipitation gradients acrosswater the glacier Antarctic recession rates Peninsula.slope may and result Strong hypsometry from variability on the glacier inon mass influence tide- the balance. of Western High glacier snowfall Peninsula length,eastern means are that side altitude, not the of currently glaciers Trinity Peninsula rapidly arefjords receding. slowing and as the Recession the glaciers rates floatingof reach ice on tongues tidewater a the retreat glaciers new into dynamic on the elevations equilibrium. James and Ross The flat Island rapid profiles. is glacier likely recession In to contrast, continue the because higher of and their steeper low tidewater glaciers on glaciers on the drier,from cooler 1988–2001, with Eastern limited TrinityJames frontal Peninsula Ross retreat experienced Island after fastest also 2001.glaciers recession retreated on Land-terminating fastest James glaciers in0.04 on Ross the km period Island 1988–2001. are now Large declining tidewater in areal extent at rates of up to length or altitude. This paperfrom firstly 2006 uses to ASTER classify images the from area,hypsometry 2009 length, and of altitude, a 194 slope, SPIRIT aspect, glaciers DEM geomorphology, onSecondly, type this Trinity and Peninsula, paper Vega uses Islanddata LANDSAT-4 and and from James ASTER the Ross Antarctic images Island. Digital from1988–2009. Database 1988 (ADD) From from and 1988–2001, 1997 2001 to 90receded. and % document Glaciers of glacier on change glaciers the receded, westernthe side and eastern of side from Trinity of 2001–2009, Peninsula Trinity retreated Peninsula,has 79 % relatively the slowed little. rate of On from recession of 12.9 km ice-shelf tributary glaciers The Northern Antarctic Peninsula has recentlyrecession exhibited and ice-shelf disintegration, acceleration. glacier However,shelf the tributary dynamic and response tidewater of glaciersability, land-terminating, and has there ice- not are yet sparse been published data quantified for or glacier assessed classification, for morphology, area, vari- Abstract The Cryosphere Discuss., 5, 3541–3594,www.the-cryosphere-discuss.net/5/3541/2011/ 2011 doi:10.5194/tcd-5-3541-2011 © Author(s) 2011. CC Attribution 3.0 License. 1 Llandinam Building, Penglais Campus,2 Aberystwyth SY23 3DB, UK 3 Received: 2 December 2011 – Accepted:Correspondence 8 to: December 2011 B. – J. Published: Davies ([email protected]) 21 DecemberPublished 2011 by Copernicus Publications on behalf of the European Geosciences Union. A new glacier inventory forspatial 2009 and reveals temporal variability inresponse glacier to atmospheric warming inNorthern the Antarctic Peninsula, 1988–2009 B. J. Davies 5 25 15 20 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | , Rau Hock ; ers an ff Vaughan Vaughan Rabassa Cook and ). Antarc- 1995 ; , Pritchard and 2007 ). It is therefore 2005 , , 2009 Morris and Vaughan , ); (iii) to establish rates ), with up to a six-fold to sea level rise ( Skvarca et al. 1 ; − 2009 2003 ). Previous inventories have Cook et al. , , ; ). With continued atmospheric 1982 being lost from Antarctic Penin- ), and the likely future behaviour , 2 ). Other tidewater glaciers on the 2011 16 mm a , 1996 ), but also coordinates, glacier ge- . 2005 , , 0 2011 Abermann et al. 2004 , ± , 2004 Pritchard and Vaughan 22 , . 3544 3543 ). The Antarctic Peninsula region is also one Rabassa et al. Racoviteanu et al. Turner et al. ). Our comprehensive survey includes not only Leclercq et al. ; 1 ; 2010 Rau et al. Glasser et al. , ; ; De Angelis and Skvarca Scambos et al. 1994 2009 , , Vaughan and Doake 1996 1995 , , King Rott et al. ). It is clearly important to establish how the on-going mass balance ). Ice-shelf tributary glaciers accelerated and thinned following the dis- C annual isotherm (the thermal limit of ice shelves ( ◦ Smith and Anderson Skvarca et al. 9 ), and have a total eustatic sea-level equivalent of 0.24 m ( ). What is particularly lacking is data on how glaciers have responded to ; ; ), the viability of glaciers in this region is questionable. With this warming Racoviteanu et al. 2007 2010 − , , 2009 2004 2003 1982 2003 , , , , , )) has moved southwards, resulting in 28 000 km C over the last 50 yr ( ◦ This paper aims to create an inventory of the glaciers of Trinity Peninsula, James Glacier inventory mapping is an essential prerequisite for regional mass balance tributary glaciers, tidewater glaciersdecades. and This land-terminating paper glaciers thereforeextent has over of five the each specific pastrameters individual objectives: for two glacier each (i) glacier to in in mapSpace; 1988, line www.glims.org) the programme with (cf., 1997, length the GLIMS and 2001of (Global recession and Land for Ice 2009; these Measurements glaciers from variability (ii) from in 1988 to recession to rates, identify and 2009; (v) (iv) pa- to to determine analyse controls spatial upon and recession temporal rates. ometry, geomorphology, elevation, aspect, slope,(ELA), hypsometry, equilibrium width line of altitude calvingcontext. Secondly, front, we use terminal this new environment,1988, dataset to snow 1997, analyse change coverage 2001 in and glacier andprehensive extent topographic between and 2009. holistic understanding These of parameters changes provide in the Antarctic basis Peninsula for ice the shelves, first com- et al. of these glaciers. Since PGIS wasern the Antarctic first Peninsula, regional the ice comparatively shelfunusual long to time opportunity disintegrate on elapsed to the since East- analyse thattributary the event glaciers o consequential to response ice of shelf tidewater removal. and ice-shelf Ross Island and Vegaglacier Island length and (Fig. area, as in previous inventories of James Ross Island (cf., climate change across the Northernvaried Peninsula geological, on climatic a and local glaciologicaling scale; settings. questions i.e. regarding For with how example, respect the there tributary toAntarctic are glaciers the outstand- Peninsula on James have Ross changed IslandShelf since and (PGIS) Northeast the (cf., 1995 disintegration of Prince Gustav Ice et al. 2.5 of the most rapidly warming places on Earth, with mean air temperature increasing by The Northern Antarcticclimate Peninsula Ice change Sheet because iset of particularly al. its dynamic relatively and small sensitive size to and northern location ( 1 Introduction integration of Larsen Ice Shelf ( Vaughan changes and associated thinning,how these drawdown changes and will impact ice future front on retreat sea level. willstudies progress, and for and modelling future glacier extents ( increase in centre-line speeds ( Antarctic Peninsula are accelerating, thinningatmospheric and and retreating sea in surface responsetic to temperatures Peninsula increased ( glaciers currentlyet contribute al. 0 warming predicted for theet Antarctic al. Peninsula region overtrend, the the next century ( 2003 sula ice shelves since 1960Vaughan ( tory and numerical modelling purposes ( surprising, given thea glaciological detailed responses and to up-to-date climatePeninsula ( glacier change inventory outlined does above,focussed not on that changes exist up for to the 2001, Northern and contain Antarctic few quantitative data suitable for inven- 5 5 25 15 20 10 15 20 10 25 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ; ; , S, ◦ King King 2008 2005 ), with , , erences van den Stastna ff ). 1982 , ), and waters 2006 , ). Water depths 1 2008 , Turner et al. Smellie et al. s into outlet glaciers, ff Gille van den Broeke and van ). The bedrock structure ), and the smallest on the Rabassa et al. 1 Ferrigno et al. ). On the eastern flank many 1995 s with the floating ice margins ff , 2005 , ). The western coast of the Antarctic ). The greatest warming rates are in 2003 , 2003 , Skvarca et al. 3546 3545 erent sea-ice regimes in the Bellingshausen and ff C warmer than the eastern coast. These di ◦ W). James Ross Island is separated from the Antarctic ) are dominated by large marine-terminating glaciers. ◦ 1 ), but the Western Peninsula in general has the greatest Vaughan et al. Heroy and Anderson ). Since the 1950s, the Antarctic Circumpolar Current has ; Vaughan et al. S, 59 ◦ 2004 2004 , 1978 ) fosters the development of elongate, over-deepened cirques, , ). , ). The island is bounded to the Southwest, South and East by 2008 2009 1992 C, with the warming greatest near the surface ( , , ◦ , ). A strengthening of this circumpolar vortex results in an asymmetric sur- ). The Western Antarctic Peninsula therefore has a polar maritime climate, ). The region of interest for this paper extends from Cape Dubouzet (63 ). 1 s and valley glaciers, and the ice cap drains over the cli 2004 ff ). Trinity Peninsula outlet glaciers flow predominantly east and west, perpendic- 2003 2003 , van Lipzig et al. Martin and Peel 1 ). The Antarctic Oscillation represents the periodic strengthening and weakening , , W) to Larsen Inlet (64 ◦ Currently, 80 % of James Ross Island is ice-covered ( Climate records from the South Orkney Islands suggest that regional warming prob- Fukuda et al. high cli principally via avalanches and ice falls ( (approximately 34 %) is dominatedIsland by and permafrost Eagle processes. Island Snow (Fig. Hill Island, Corry the remainder comprising( rock or Quaternary sediments with perennial permafrost of resistant volcanic rocksHambrey overlying et soft Cretaceous al. sedimentswith ( steep or neartwo vertical plateau back ice walls caps up to that 800 feed m numerous high. small Vega tidewater Island glaciers. is dominated The by ice-free area (Fig. ular to the Peninsula spine ( warmed by 0.2 to the west ofMayewski the et Antarctic al. Peninsula have warmed very rapidly2.2 ( Contemporary glaciology The Antarctic Peninsula Iceits Sheet central is plateau typically glaciers attain 500 m altitudes thick of over over Trinity 1600 m Peninsula, and a.s.l. along its central spine outlet glaciers terminate in floating orPeninsula partly coastline floating mainly tongues. comprises The North-Western groundedof Trinity a ice few cli small ice shelves and numerous small glaciers ( precipitation rates in Antarctica,nent typically ( 3–4 times that of any other part of the conti- Sea enhances warming over thesociated Western with Peninsula decreases and the inBroeke Weddell precipitation and Sea. van over This Lipzig the is South-Western as- Peninsula ( and warming over the Antarctic Peninsula. Decreased sea ice in the Bellingshausen 2.1 Location and climate Trinity Peninsula is the northernmostsula part (Fig. of Graham Land, Northern Antarctic Penin- 2 Regional setting 57 Peninsula by Prince Gustav Channel, which is 8 to 24 km wide (Fig. and James Ross IslandSea have ( a polar continental climate, dominated by the Weddell reach 1200 m andnorth-south shallow orientated southwards Antarctic to Peninsula mountains lesssistent are than Southern an 450 Ocean orographic m westerlies. barrier (Evans tonorthwards, Cold et per- barring continental al., the air warmer in 2005).et maritime the al. Weddell air The Sea masses also of flows thedominated Bellingshausen by Sea the ( warm Bellingshausen Sea, whilst the Eastern Antarctic Peninsula the east (at Marambio and Esperanza stations; cf. Fig. Peninsula is therefore typically 7 are further exacerbatedWeddell by seas, the with di the Weddell Sea being sea-ice bound for much of the year ( ably began in the 1930s ( northwest coast. The most pronouncedto warming changes is in in the atmospheric winter2010 circulation, months, and sea is ice related extentof and the belt ocean of processes troposphericLipzig westerlies ( that surround Antarctica ( et al. face pattern change, with pressurecauses falling over northerly Marie flow Byrd Land. anomalies, This which pressure in pattern turn produce cooling over East Antarctica 5 5 20 25 10 15 10 15 20 25 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ; , ) Cook 2006 2005 British . The , , ; 2 Skvarca 1982 Glasser et al. , ). An average ; cult to map (e.g., Cook et al. between 1988 and ffi 2004 2004 1 Reinartz et al. , ); but this is assumed − , er of 22.5 m width was a ff ), and are given in full 2 ). ). Ground-control points 1 from 1975–1988 ( 2006 , 1 25 m at the 66 % confidence 2009 − ), and rapidly disintegrated in 2009 Rabassa et al. ± a , , Rau et al. Rau et al. 2 ) noticed no dramatic change for ; ). 2006 , 15 m for ASTER images). Mapping ± 1995 2003 2003 , , ), followed by the thinning, acceleration and ). Glacier names and numbers were taken 3548 3547 Ferrigno et al. Racoviteanu et al. 1997 2009 , , Granshaw and Fountain ) Coastal Change dataset (from Vaughan et al. Czech Geological Survey ; Cooper ; and Supplement). The geographical area mapped was lim- 2010 1 , ). Although Skvarca et al. ( Korona et al. Skvarca and De Angelis 1995 ). PGIS was connected to Larsen Ice Shelf until 1957/58 ( ; ; , ). The northernmost ice shelf on the Eastern Antarctic Peninsula, it 1995 2004 , 2006 , 1995 2007 , 2010 , , , ) doubled after the disintegration of PGIS, to 3.8 km Skvarca et al. Rau et al. 1995 ). During the later twentieth century, most glaciers on James Ross Island and , Retreating tidewater termini have been mapped for the entire Trinity Peninsula, with Ferrigno et al. Skvarca et al. Antarctic Survey from previous glacier inventories and published maps ( limited by the pixel resolutionwas of estimated to the be dataset accurate (i.e. therefore to within placed 3 either pixels side (i.e.mum 45 of m). estimate of each A size bu glacier and polygon, aan total error providing error in a margin ASTER equivalent minimum co-registration toto ( and 3 be pixels. maxi- within There the may also mapping be limits. ited by thehttp://www.add.scar.org:8080/add/ availability of satellite imagery). The Antarctic Digital Database (ADD, Sources of uncertaintylargest and errors mitigation in glacier strategiesof drainage are ice-divide basin identification summarised delineation andlimits in are the mapping. derived Table accuracy from of DEM ice interpreterbut divide quality were error mapping. co-registered in ASTER to areas Level the 1B of SPOT-5 images images flat are to pre-processed white reduce ice errors. also Calculation of area is were not necessary since accurate geolocationpixel of in the a SPOT-5 images SPOT-5 image is possible. caninterval, be Each located although on errors the may ground beBerthier to larger in et areas al. of flat glacier ice ( 3.1.2 Error estimation was used to providebecause additional of data high cloud wherefrom cover). the the Topographic ice 2006 elevation SPIRIT margin data Digital was and Elevation contours di Model were (DEM) derived (Table ASTER images (Table outlet glaciers on James Ross( Island showing large reductions in area since the 1940s Snow Hill Island has extensive floating margins. 1995 ( 2011 North-Eastern Antarctic Peninsula experiencedstrongest rapid evidence of recession recession and into calving, the prevailing with northernmost climatic the parts. warming Thisretreat ( rate is of generally the attributed James Rosset Island al. glaciers of 1.8 km and Vaughan 2001 ( small land-based glaciers from 1977( to 1988, retreat was observed from 1988 to 2001 set out byin the the GLIMS Supplement. programme Mapping was ( conducted in ArcGIS 9.3 from interpretation of 2009 was the first to show signs of retreat ( rapid recession of the former ice shelf feeding glaciers ( 3.1 2009 glacier inventory 3.1.1 Data sources This inventory island, a Snow snapshot Hill ofable Island the for and glaciers download Vega on from Island the Trinity in Peninsula, GLIMS 2009. James geodatabase. Ross This Is- data Our has methods been conform made to avail- those 3 Data sources and methods 5 5 10 15 20 10 15 25 20 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ; ), Paul ). MAX 2004 ; , Primary -backed ff 2010 2009 , ), and mean , ). On James 2010 ). The nature of Area, Length, Co- 2010 , , ), maximum (H ). Marine-terminating Paul et al. Scambos et al. 2011 ; ; MIN , 2009 2005 , 1992 Paul et al. ), but they do not allow such , , Racoviteanu et al. ; b ), which are impractical for glacial 2010 , , Raup and Khalsa ; 2010 Rau et al. Carrivick et al. , Fricker et al. 2007a ; ; , 2009 (e.g., GAP17 or GIJR65, standing for Glacier , Dahl and Nesje 2005 3549 3550 Bolch et al. 2007 (grounded, floating, land-terminating), , , in addition to notes on geomorphology and ; , Form, Primary Classification, Frontal Character- GLIMS ID, Elevation, Width of calving front, Date ) elevation using the 2006 SPIRIT DEM. Elevation ). Brunt et al. ); this is because ice situated above the cli 2009 Raup et al. 1 , ; Glacier ID 2010 MEDIAN , Oerlemans 2005 Hypsometry , cult to determine whether a glacier is floating or not, or where ffi Racoviteanu et al. Lambrecht et al. and ; are geomorphological descriptors that provide detailed information parameter, glaciers were categorised as floating, partially floating, (if published), 2006 Rau et al. , ) and median (H Svoboda and Paul Raup and Khalsa ; Remarks Tongue MEAN 2010 and , In the Data were automatically derived in the GIS for minimum (H Reinartz et al. grounded or land-terminating. Land-terminating glaciers are relatively few in Antarctica, jor control on(AAR) mass of balance, a as glacier. it strongly It determines is the dependent accumulation on area valley ratio shape, topographic relief and glacier data are unavailable for GAP40,geographical GAP43 limits and of glaciers thecalculated north SPIRIT for of DEM. each GAP34 glacier Values polygon because forAspect using of mean and the the slope 2006 slope and SPIRIT are DEM useful aspectslope (refer data were can to for also Supplement). be modelling used purposes as ( a proxy for ice3.1.5 thickness. Glacier hypsometry Glacier hypsometry is the distribution of glacier surface area with altitude, and is a ma- ing, where either it isthe di glacier may becalving margin. grounded at the lateral margins butmean (H floating in the centre of the inventories. However,have the several floating visual tongues characteristicsgrounding-line, an in of irregular, common: heavily marine-terminating crevassed andfile, glaciers a convex calving an pronounced typically front, irregular a break flat margin,glaciers in long and are pro- slope occasional typically at characterised largeprofile, the by rifts. and a have concave Alternatively, no calving grounded clear front, break tidewater a in slope steadily ( dipping long glaciers that exhibit a combination of these characteristics are defined as partially float- ature and precipitation thandicator marine-terminating of glaciers, climate theythe change can ( marine-terminating be glacier aand tongue sensitive glaciological has applications, in- important butwith the implications detailed grounding geophysical for zone surveys can oceanographic ( only be accurately located et al. istics on the glaciers shape,glaciers) that terminus correspond to and GLIMS classification guidelines (e.g., ( cirque, niche, outlet, valley but as their recession is controlled more directly by changes in atmospheric temper- of scene acquisition, Satellite,classification, Tongue Form, FrontalSlope, characteristics, Aspect, Moraines, Debris ELA glaciology on (cf., tongue, Remarks, 3.1.4 Attribute data for glacier drainageAttribute basins information determined for eachordinates, glacier Name polygon comprises Antarctic Peninsula and Glacier James Rossappropriate Island, to respectively; these previous conform inventories), where Ross Island many glaciers haveincluded well in defined their cirques, polygons butbergschrund the (Fig. contributes plateau snow above them and was icethe glacier. through frequent avalanches and creep flow to Automated methods forquickly large-scale (e.g., inventories can be used to map large regions 3.1.3 Drainage basin delineation out by the GLIMSbody programme of (refer ice to that Supplement).ground includes A all and glacier tributaries nunataks and polygon ( connected is feeders, a and coherent excludes exposed high detail in digitisation.glacier polygons in For our high-resolution this study reason, of a we small used region, following manual guidelines digitisation set to establish 5 5 25 25 20 10 15 15 20 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | , ). ), cult and erent ffi 1 ). The ff ) were 1982 2009 , 2011 2005 , , erent approach ff Furbish and Andrews Rabassa et al. Cook et al. ). In this study, five di 1 HI − 2004 Carrivick and Chase , . James Ross Island was 75 % = ; raw data available for download ; all tidewater outlet glaciers) with 2 2 5 ectively capture the periods before, ff ). However, field programmes are time 100 km erence in area of each glacier polygon for then HI ; Table 2009 ff > 1 , 3552 3551 , 1 ) could then be plotted for the largest glaciers. 2 < (Fig. 2 ective accumulation, mass balance will decline and HI ), which included the largest glaciers on the North- ff 5 < Carrivick and Brewer ). However, there are a wide range of remote methods erence is because of the significantly di ff 262 km 2004 ± (Table , ) as far as possible to facilitate data comparisons, it was not 2 and if 0 1982 Braithwaite and Raper , 154 km min max ± H H − − Skvarca et al. ). 4 median median ) are no longer discernible. While we attempted to follow the nomenclature used H ). Faster rates of accumulation area loss during climatically-driven ELA rise will H = 1982 ( by Rabassa et al. ( from GLIMS; www.glims.org). Trinitycovering Peninsula 5827 was 95 % glacierisedern with Antarctic 62 Peninsula glaciers glacierised, with which is 20 a glaciers reduction ofOur 5 inventory % identified since 104 the glaciers surveysurvey in on identified 1977 James ( 138. Ross Island, This whereas di used the to original map 1977 thepolygons). glaciers (using Many smaller ice glaciers divides or and possibly flow snow unit patches boundaries mapped to by Rabassa delimit et glacier al. 4.1 Glacier size and elevation In 2009, the Northernered Antarctic a Peninsula region total had area 194 of individual 8140 glaciers that cov- number of tidewater glaciers. Theseduring time and slices after e ice-shelfeach collapse. time The slice di allowedof calculation glacier of recession area were lostsurface calculated areas and for that each rates changed period. of less“stationary”. recession. In than “Shrinkage” subsequent the indicates Annual analyses, calculated a rates glacier loss mapping of error surface were area. classified as 4 2009 Glacier inventory results Assuming no migration ofin ice the divides, Supplement, and theand using extent 2001. the and The datasets length ice namedused of front to in each map positions Table glacier ice available extents in was in the also 1997. ADD mapped However, (from these for data 1988 were only available for a limited 3.2 Calculation of glacier change 1988 – 1997 – 2001 – 2009 ative mass balances from onelong-term year ELA to the is next bestover (e.g., several determined years ( by a programme of mass-balance measurements In a glacier inventory, antal, estimation because of it the divides mean a long-term glacierrises into ELA and/or ablation is if and considered there accumulation to areas. isthe be ELA If declining vi- will air e rise. temperature ELAs have considerable inter-annual variability, with positive and neg- where HI 3.1.6 Equilibrium line altitude derivation tent of the impact on the1984 glacier relies on the glacier hypsometry ( depth. When the ELA of a glacier changes, for example due to climate change, theresult ex- in increased glaciermasking recession. 54 glacier Glacier polygons hypsometricthe (i.e. curves those SPIRIT were over DEM, calculated 40 km and by metric the curves area of in cumulativeA area each single (km 100 Hypsometric m Index elevation (HI)glacier (equivalent bin polygon to was using “altitude the calculated. skew”) equation was calculated below, Hypso- originally for each presented by Jiskoot et al. ( consuming and expensive and theto Northern access. Antarctic Peninsula Indeed, regionstudy is only area very ( one di mass-balancefor investigation calculating glacier has ELA been (e.g., published for the long-term ELA derivation methodsin were Table applied (summarised in the Supplement and 5 5 25 20 15 10 15 10 20 25 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | . . , is 2 h; TSL 3 2 TSL (Fig. erent re- ff . However, and ELA ). In general, THAR 3 Skvarca et al. cult to achieve THAR ect the distribu- ffi ff HESS cult. Furthermore, . Snow Hill Island 2 ffi and ELA a), 48 land-terminating 4 culties, large data gaps, and ELA account for most of the 15 km AAR ffi values of 0.4 and 0.3, re- ± 2 p ), and there was again large AAR ; was henceforth excluded from 5 , ELA 2009 ). James Ross Island also had 17 TSL , ELA 6 , MEDIAN (Table , and was 96 % glacierised. MEDIAN 2 3554 3553 MEDIAN 6 km . Jiskoot et al. 3 s; ± ff h). ). There is a weak relationship with log glacier area, 3 3 ). Almost all the glaciers on Trinity Peninsula calve into the 6 for each glacier must necessarily be treated with caution, as was also excluded from further analysis as it is likely to only e,f) and between glacier length and slope (Table b). As the total area of glaciers in the size class 0.1–0.5 km d; Table 3 3 3 MEAN HESS ). However, there is considerable scatter in ELA 5 c), and a rather weaker correlation between log glacier area and ele- is likely to be insignificant and certainly considerably less than 3 km 3 5; Fig. 2 . and is therefore the average of ELA 0 a). A small number of glaciers over 100 km , the underestimate of glacierised area caused by having a minimum glacier 4 = 3 2 , 2 r 3 8; Fig. of glaciers on Trinity Peninsula peaked at 400 m a.s.l., reflecting its high moun- and slope (Fig. . MEAN 0 ), making accurate remote mapping of transient snow lines di = ELA The mean elevation of glaciers was skewed towards glaciers in the 200–300 m a.s.l. 2 MEAN MEAN r There is a very strong regressioncTables between ELA east-west orographic precipitation and wind variations. Standard deviations range from 4.3 Equilibrium line altitudes and they show no correlation with ELA Mapping snowlines on Trinitysults Peninsula to is other likely methods, to assula produce the results strong substantially in east-west di snow precipitation300 lines gradient to on close 400 Trinity to m Penin- seation a.s.l. level of on on snow the at thetotal western the Eastern scene coast, end Peninsula. and coverage of Strong snow the forThese lines winds ablation polar each at season. also glaciers year are a mapped, Inof characterised accumulation addition, and by and it complex there ablation was accumulation separated are di by zones large areas with of gaps patches superimposed in ice ( the data. scatter and low correlation (Fig. the calculated ELA it is entirely derivedhas from the not altitudinal been range checked and hypsometric against curves mass-balance of data, the glaciers, and does not take into account spectively). The large standard error indicates little regional consistency in ELA 2004 mapping of snowlines maysnowfalls occur occur throughout either the just summerskew after season results. or in polar just Because regions, before this oflarge a is these inter-annual likely snowfall inherent scatter to event. methodological and further the di As low analysis. correlation, ELA ELA be applicable to 13 land-terminatingterminating glaciers glaciers, (not glaciers being with generally ice applicableor falls, to glaciers marine- glaciers with terminating complex or in compound steep cirques, cli H vation ( 4.2 Glacier form and classification Outlet or valley glaciers drainsula mountain the chain large (Table plateau iceocean. caps Of that these rest calving onJames glaciers, the Ross 10 Trinity Island had Penin- had floating 16glaciers and and glaciers 20 one with had lacustrine floating partially glacier termini floating (GIJR86; (Fig. termini. Table ( longer glaciers had a lower slope, with large low-angled ablation areas. islands were characterised byfloating small margins. ice caps. Snow Hill Island ice cap has extensive bin (Fig. tain chain. James Ross Island hadabove the 200 m. highest number There of was glaciers a with strong mean elevations correlation of glacier length and maximum elevation out of the 18and small the alpine few glaciers, glacieret and which snowfield were remnant mostly glaciers cirque in the or study small area. valley The glaciers, remaining vided into two separatetogether ice in masses, line or with becausewas the two 66 % structural or glacierised glaciological more withinto and polygons four 11 ice were plateau outlet divide merged ice glaciers. mapping. capshad one with A Vega large nunataks total Island ice dissecting of cap catchments covering 24 326 glaciers covered 168 glacierised area (Fig. only 3 km size of 0.1 km H possible in all cases, either because a glacier was not visible, had retreated and di- 5 5 10 25 15 20 15 20 25 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | , of MEAN g). 4 Skvarca et al. 432 m a.s.l.) may be of around 100 m a.s.l. c). On James Ross Is- ± 5 (very top heavy) (Ta- 4 . erence between bottom- 1 ff MEAN 909 − < , which is closely related to me- MEAN has been plotted, which generally d,f), but the large Mount Haddington 4 MEAN ) found the equilibrium line of GIV09 92 m a.s.l. It is thus possible that our c,e. There is no correlation with eleva- MEAN illustrate the di ± 4 on Trinity Peninsula are generally around 5 2004 3556 3555 MEAN of 245 culty in obtaining a meaningful parameter from ffi MEAN ). There was considerable inter-catchment variability in 5 (very bottom heavy) to HI . 1 1 m a.s.l. The range of errors for simple basin glaciers with 2009 > , 787 m a.s.l., respectively. The range of values may be less for ± 800 m a.s.l. ELA ± ). The aspect of a glacier controls receipt of solar insolation, as is an underestimate, but it is impossible to verify without further > 5 of 87 d,f). Exceptions are a few glaciers that terminate within narrow bays MEAN MEAN 4 MEAN 500 m, illustrating the di i; Table , example normalised hypsometric curves derived from the 2006 SPIRIT Jiskoot et al. b shows the distribution of ELA over the study region. The subdued topogra- 3 5 > 4 727 and 1265 ± ). GIV09 was, at time of publication, experiencing a negative mass balance, thin- ; see 7 cult to determine, as it had an accumulation area with zones of snow accumulation On James Ross Island, the low-lying topography of Ulu Peninsula resulted in bottom- In Fig. Figure Our topographical ELA predictions can be compared with previous mass balance 5 m to ffi heavy (GAP12, GAP45), equi-dimensionalGAP60) (GAP14, glaciers. GAP53) and Glaciers top-heavy (GAP13, with a small accumulation area could be more sensitive The hypsometric index (HI) of allfive glaciers categories was calculated from and HI glaciersble were divided into dian elevation (which wason used glacier in recession. the The ELA examples in calculation; Fig. see Sect. 3.1.5), is a control land, there is a preferencelargely for southeast northwest-facing and aspects. northwest, Aspects reflecting on the Vega west-east Island axis trend 4.5 of the island. Glacier hypsometry were large with relativelyern small Trinity accumulation Peninsula areas. were TheGAP20. generally remaining bottom-heavy, for glaciers example, on GAP34, East- GAP31 and heavy outlet glaciers draining Dobson Dome (Fig. DEM are presented andfell the at about normalised 60 ELA % of the accumulation area. ELA west-facing preferred glacier aspect on Trinity Peninsula (Fig. glacier shape and elevation distributions.Trinity Peninsula Over were half very (35) bottom-heavy, with ofaltitude large the (Fig. low-lying large areas outlet below glaciers the(e.g., on median GAP13, GAP17). However,more on equi-dimensional the or west top-heavy. coast of Glaciers Trinity that Peninsula, were glaciers formerly are tributaries to PGIS profiles of tidewater outlet glaciersby draining sharp the changes Mount in Haddington slope Icelow-lying angle and Cap in relatively are ice flat falls typified at partly their floating cirque or headwalls, floating followed glacier by large, tongues (Fig. Ice Cap contained largely top-heavy glaciers, such as GIJR115 and GIJR61. The long- climatic factors. For example, GIJR103,has a an grounded ELA valley glacierfloating with a tongues simple (such basin, as,because for of example, their GIJR64, large ELA low-lying ablation areas. 4.4 Glacier aspect Mean glacier aspect is summarised in Fig. However, the glaciers that have accumulationcan areas have on ELA the Mount500 Haddington Ice to Cap 600 m1194 a.s.l., with theland-terminating simple-basin exception glaciers, whose of size may GAP60 be more and closely 61, determined by which have ELA well as influencing the driftingasymmetry of over snow their through surface area, persistent which winds. results, Most for glaciers example, display in a strong northeast to di and ablation, separated by zonesance of was superimposed estimated ice. by Thethan Skvarca altitude our et of remotely zero al. mass mappedpredicted bal- (2004) ELA ELA to be 400spatially-distributed m mass-balance a.s.l. data. This is much higher phy on Ulu Peninsula, James Ross Island, results in low ELA tion (Fig. topographical data alone. studies carried out on2004 GIV09, Vega Islandning (Glaciar and Bahia frontal del Diablo; retreat. Skvarca et al. ( < 5 5 25 15 10 20 15 20 10 25 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | be- 2 erent erent Raper ff ff ; GIV05 ; GIJR72 2 2 km 2 . ), GIJR71 2 over the 8 yr 15 4 km 1 ± . g, it is obvious − 0 4 9 12 km a . . 04 km . 2 0 ± , equivalent to an 0 2 ± 73 ± . 46 . 06 . ). In the study region, they 2003 ). It is noteworthy that di , 2 , and so would be expected to react 2 ) advanced from 1988–2001. Di 03 km . 2 , but the shrinkage of these glaciers is f illustrates that there is a weak negative 0 2 ), although this can vary regionally ( 3 ± 2 km 3558 3557 a). The majority of the 48 land-terminating . 1 km 10 6 2004 . These glaciers then retreated at a rate of . 0 1 , < ± − , the percentage shrinkage varies from 0 to 66 % ); Fig. 2 a 22 2 ). On Trinity Peninsula and Vega Islands, advances . 8 ective precipitation). 2005 1 km ). This equates to an overall retreat rate on James Ross ff with the long profiles presented in Fig. , 9 < Skvarca and De Angelis Paul et al. 5 , and from 1988–2001, lost 727.8 km 2 ). Response times are also determined by slope and mass over the 13 yr from 1988–2001, and 15.1 km 1 9 km − . of surface area between 1988 and 2001, and 121 ). On James Ross Island, GIJR54 (0 ; and GIJR78 by 0 2009 a Oerlemans 2 2 2 2 , ) and GIJR90 (0 153 2 ± in the 8 yr from 2001–2009. The 104 glaciers on James Ross Island 2 km . 01 km 3 15 km . . 1 . value of 0.001). 0 − 0 15 05 km , the extent of glaciers in 1988, 1997, 2001 and 2009 is shown, including the a p . ± ± ± 1 2 0 a,b). However, there has been little shrinkage in these glaciers since 2001. Most ± 02 11 6 . . 10 The seven land-terminating glaciers on Vega Island have all retreated since 1988 The 61 tidewater glaciers and single land-terminating glacier on Trinity Peninsula In the study region, 90 % of glaciers receded in the period 1988–2001, and 79 % . relationship between glacier area andsteeper mean ( slope, and that smaller glaciers are often (Fig. glacier retreat ongenerally Vega Island shrinking occurred by in 2 the to period 7 % 1988–2001, (Fig. with the glaciers glaciers on Jameshighly Ross variable. Island For are glaciers and Braithewaite balance gradient ( The recession of land-terminating glaciersis is of directly particular related interest to because atmosphericon their activity and the climatic Antarctic changes, Peninsula andare ( these generally glaciers small; are scarce fastest most to external are forcings less ( than 1 km Island of 22.3 km from 2001–2009. Two small glaciersappeared (GIJR56 between and 1988 GIJR30) and on 2009. Jamesis The Ross majority accounted Island of for dis- the by arearate the lost of on disintegration James retreat of Ross has PGIS Island and accelerated in James since 1995. Ross 2001, Island For with exhibiting most those particularly glaciers, on rapid recession. the Eastern5.2 annual Antarctic Peninsula Land-terminating glaciers cover 5827 average recession rate16.8 km of 56 km lost 290 tween 2001 and 2009 (Table glaciers. Most of the advancingmay glaciers have were a marine-terminating non-linear outlet response glaciers, to which atmospheric forcing. only occurred fromby 1988–2001 0 in(0 two glaciers (GAP10glaciers had by small 0 advancesby from 1 2001–2009 (GIJR124glaciers by 0 advanced inhas each decreased time since period, 2001; and this that variance highlights the the number individual of dynamics advancing of glaciers these shrank from 2001–2009 (Table data is available; however, thethere values is are no blank newThere in data was the available. only figures and satelliteglaciers. The Supplement Full coverage when total rates of of area all glacier given recession three (with is years errors) therefore are (1988, presented a 2001 in minimum the and value. Supplement. 2009) for 178 5 Glacier change results 5.1 Change in glacierised area On Fig. former PGIS. For purposes of datalar summary, year, where it no is data assumed are that available the for a area particu- is the same as in the previous analysis from which tion zone, especially ifhypsometric the curves ELA in rises Fig. abovethat the the new low-lying floating median tongues altitude.sult of in Comparing the large, Mount the low-lying Haddingtontemperature ablation Ice or areas Cap decreases that outlet in glaciers may e re- be vulnerable climate change (rises in to climate change if the ELA rises and allows a large additional area to be an abla- 5 5 25 20 15 10 20 25 15 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 1 c − 7 a 2 . Indeed, 2 b). Glaciers on 7 ), but emphasise ) occurred prior to 3 2 from 2001 to 2009. 1 − a 6 km from 1988 to 2001 and . ). Our study shows that 2 in the period 2001–2009. 1 ¨ ogren Glacier was a major − 1 − a 395 a 2 2004 . Sj ± 2 1 , 7 − . a ). However, glacier recession has 2 8 in the period 1997–2001. The an- h shows that the largest annual rates 1 6 in the Northern Antarctic Peninsula be- − ¨ ohss Bay, the recession rate is fastest 2 a Rau et al. 2 a), and GAP01 to GAP14 had faster annual 7 6 km ). Our study of GIV09 from 1988–2009 shows . 3559 3560 ). ) was relatively stable in the period 1982–1985, 5 1 c,d shows little correlation between 2009 glacier 395 2003 7 ± , 5 . ¨ ogren Glacier (GAP12) retreated 33 km from 1988 to lost since 2001; this is equivalent to a total recession from 1997 to 2001, and 0.3 km ) receded at 17.7 km 2 1 1 ) since 2001. g; Table also show highly variable patterns of shrinkage, from 0 to − 2 6 a 2 2 1 km since 2001 (error estimated probabilistically). On Vega Island, . 1 3 km − 49 a < ± 19; Fig. 2 . 0 c). erence in GAP15, GAP14 and GAP12. It is apparent that most of the ). In the period 1975–1988, five land-terminating glaciers were found 7 = ff 0 km 2 . r 1 from 2001 to 2009. The glaciers of Western Trinity Peninsula have had e,f). Overall, the largest reaction to climate warming in the Antarctic Penin- 2004 ± 7 Skvarca and De Angelis 1 4 . − a 2 c,d). Glaciers 6 ¨ Analysing the rates of recession for the glaciers that fed PGIS in more detail, Fig. The recession of glaciers (decrease in glacier length) was greatest for ice-shelf trib- From previous inventories, it is evident that most of the margins land-terminating The highest annual rate of recession was reached in the period 1988–1997, when ogren Glacier (GAP12; Fig. of 13.1 m ( after 2001 (Fig. 5.3 Marine-terminating glaciers In total, glaciers receded by 1319 tween 1988 and 2009. Of1997 this with areal the decline, disintegration 70 % ofcontinued, (927 PGIS with in 1995 274 (Table rate of 30 Glaciar Bahia del Diablo (GIV09;but Fig. showed considerable thinning from 1985–1998, with an average surface lowering nual rates of length changeWestern are Trinity in Peninsula former in PGIS general tributary show less glaciers change (Fig. in glacierhighlights length the and di area. shrinkage of these threeshelf disintegration, glaciers with occurred slower and beforesubstantially steadier 1997, larger retreat thereafter. than immediately These the preceding arealwith mapped losses less ice- errors. are areal loss. The OnGIJR92 recession the other rate and hand, decreases GIJR90, for glaciers after which on this, James are Ross situated Island, in in particular R retreating. Of thethe 48 48 mapped land-terminating land-terminating glaciers glaciers2001–2009, had we 15 retreated mapped from glaciers 1988–2001. on hadwere In the stationary retreated. the and island, period none In 36 had advanced. both out time of periods, the remaining glaciers continued shrinkage (0.5 km rates of glacier retreatfor both non-ice-shelf tributary from glaciers 1988–2001 isrates small and by of 2001–2009. comparison, retreat but they The after generallylength, change 2001. had width faster in of Figure calving length tonguethat and rates rates of of glacier length retreat change (cf. were Table faster 1988–2001. Even after 2001, the fastest an- glacier recession has continued sincewere this observed in period. the However, period theof 1988–2001. largest recession Figure areal on changes James Rosssion Island of were land-terminating between glaciers 1988–2001, after withRau this only et period. limited al. reces- This ( supportsto initial be observations retreating; by in the period 1988–2002, 17 out of 21 land-terminating glaciers were There is wide variety inest rates annual of rate glacier of recession; recessionin that GAP05 the did is period not the 1988–2009, feed glacier1.0 km with PGIS. with GAP05 recession the lost high- rates 9.1very of % low of 0.4 km rates its of total recession area or have remained stationary. utary glaciers. For2001 example, and Sj 7.1 km from 2001 to 2009 (Fig. Sj contributor to the icenual rate shelf, of recession and then lost accelerated,GAP15 reaching was 1.2 2.4 km km also afrom 1988 major to contributor 1997, 0.6 to km PGIS and receded at a rate of 13.8 km glaciers in the Northernwhereupon Antarctic shrinkage Peninsula was region widely observed were ( stationary until 2001–2002, sula is in smallthere land-terminating is a mountain weak glaciers regression(1988–2009; between that initial are glacier less size (1988) than and 1 total km glacier area lost (Fig. 35 % (Fig. 5 5 25 25 15 20 15 20 10 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ; in 1 − 1995 a ). C from , 8 2 ◦ a). The 2 . 8 7 − ], and GIJR128 d, Table 1 a). 8 − 8 ) and a ) dramatically disin- 2 ). The retreat of ice Skvarca et al. 1 and ¨ ohss Bay experienced 7 2007 erence in recession be- ). Our inventory shows , ered rapid areal decline ff from 2001–2009, indicat- 2011 ff erences in inter-catchment , 1 ff − 2004 ¨ a ohss Bay on James Ross Is- , 2 Sone et al. ¨ ohss Bay. ], GIJR115 [0.5 km ], in Holluschickie Bay, for example, de- 1 Rau et al. Glasser et al. 1 − ; − a a 2 2 ¨ ohss Bay, but the margin was stationary from ¨ ogren Inlet, Eyrie Bay and Duse Bay. Almost 3562 3561 d, which shows the di in the period 1988–1993 ( 1995 8 1 , − a 2 ), suggesting that a few particularly warm years may ). The remaining glaciers of R from 2001–2009, when the ice shelf retreated beyond 8 ). Regions of exceptionally rapid glacier recession on 8 1 C from 1999 to 2004 ( − ◦ 2010 a 5 ¨ , ohss Bay on James Ross Island (Fig. 2 ), but after 2001 none have advanced more than the error − from 1988–2001, and 15.1 km 8 Skvarca et al. 1 − ; erence to overall recession rates. Di ff a )). There is strongly asynchronous behaviour (Fig. ). Average retreat rates for James Ross Island were 1.8 km 2 1 1982 ). Our study indicates that glaciers on James Ross Island retreated , 1982 Laska et al. , ] (Fig. 2004 1 , − a 2 Overall, recession rates across the Antarctic Peninsula are slowing, which may be Many large tidewater glaciers on James Ross Island su Some ice-shelf tributary glaciers on James Ross Island also show small signs of ad- Rabassa et al. tegrated after 2001.ture Small and ice mass shelves balance are susceptible of to tributary small glaciers changes ( in tempera- 2006 to 2009 ( have made a large di recession rates may reflect variance inand altitude, non-linear accumulation tidewater area, glacier shifting responses ice to divides, oceanic and atmospheric6.2 forcing. Impact of the disintegration ofThe Prince remnant Gustav of Ice PGIS Shelf in R a continued and steadily increasing glacierRabassa recession et since al. the first inventory 1977 (cf., 6.1 Comparison with previous inventories Our data support( the general recessional trend reported in previous inventories glaciers draining the Mountrates Haddington are Ice likely Cap to on continue James if atmospheric Ross temperatures Island, continue these toas retreat a rise. result of tidewater glaciersfrontal reaching stability. their grounding In lines, addition, andJames reported achieving Ross increased mean Island, were annual air temperatures on Ulu Peninsula, glaciers of Croft Bay andclined comparatively GIJR72 little. [0.1 km Variable ratesCape of areal Broms shrinkage are of alsofaster Southeast noticeable from around James 1988–2001, Ross withland, Island. some Snow exceptions Hill around Island In and R general, the Western most Trinity Peninsula glaciers (Figs. retreated 6 Discussion the period 1975–1988, and 2.1 km and sea surface temperature increases. Given the hypsometry of the large tidewater at a rate of 22.3ing km increased rates ofrates recession in immediately the post longer-term, ice-shelf which disappearance are but presumably slower in response to continued atmospheric from 1988 to 2009[0.4 (e.g., km GIJR108 [0.6 km Rau et al. tween 1988–2001 and 2001–2009.in These a tidewater discernible glaciers ice now shelf, no but longer calve terminate directly into R in area at athe rate narrow of pinning 1.9 point km at1988–2001. the This head is of highlighted R in Fig. from 1988–2001 (Table margin. All advances1988 were to small and 2009. wereshrinkage subsumed There rates by for are the the fewerThis overall period contrasts data recession with 1988–2009 available glaciers from have for on remained North-Eastern Western low Trinity Antarctic Peninsula in (Fig. Peninsula, thatvance but during region the (Fig. period 9). enhanced (Table drawdown and faster rates of annual recession after 2001. GIJR90 declined On Trinity Peninsula, ice-shelf tributary glaciers retreatedrapidly fastest from overall and 1988–2001 particularly (Fig. Trinity Peninsula include Larsen Inlet,all Sj glaciers show signs of glacier recession; four glaciers on Trinity Peninsula advanced 5.4 Spatial and temporal patterns of glacier change 5 5 25 20 15 25 10 20 15 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ). eren- 2005 ff , ). James Pritchard and 2003 ¨ ohss Bay after , ; ). Oerlemans 2004 , 1987 , c) is a response to the initial ¨ ohss Bay. Structural glacio- 8 Vaughan et al. ; Rignot et al. 1987 ering regional response can probably , ). The response of land-terminating ff Meier and Post ). As south-westerly winds blow across 2004 , 2004 3564 3563 , ). These tributary glaciers began to stabilise and Aristarain et al. ect the climate system through the formation of deep Rau et al. ff ¨ 2008 ohss Bay since 2001 (Fig. , ). After 2001, the region therefore entered a period of “nor- ). The removal of the ice shelf would have raised local air van Lipzig et al. 1987 , 2004 , Hulbe et al. ; 2007 ). In addition, up-glacier thinning may result in steepening, increased driving , 8 Hulbe et al. Meier and Post ected the regional climate ( The majority of the glacier ice lost on James Ross Island is accounted for by the dis- Previous workers have hypothesised that the disintegration of the ice shelf may have The recession of marine-terminating glaciers in the Northern Antarctic Peninsula ff be attributed to precipitationtial gradients, exacerbated wind by patterns climatic (cf., warming and di integration of PGIS in 1995.prior For most to remaining 2001, glaciers, recession withparticularly rates ice-shelf were rapid highest tributary recession. glaciersrecession Western or on Trinity have Peninsula Eastern remained glaciers unchanged. Trinity had Peninsula This di very exhibiting low rates of enhanced back-stress and pinning against the fjord sides. the Antarctic Peninsula mountains, risingstarving air precipitates the moisture east as of snow precipitation in ( the west, a Ross Island lies in theperatures precipitation will shadow of have the resultedglaciers Antarctic in are Peninsula. less Higher a able air rise to tem- withstand in precipitation ELA; starvation. smaller accumulation areas mean that temperatures through the availabilitysmall of glaciers more on ice-free Jameslocal water climate Ross because in Island of summer. the may large be In land area, addition, particularly which susceptible has a to low changes albedo. in once the glaciers retreated to within their bays with shrinkage slowed as a result of mal” glacier recession.distinctive The phases: Northern 1988–1995, Antarctic theice-shelf Peninsula stable disintegration region and ice-shelf has rapid period; readjustment thusboundary of 1995–2001, had the conditions; the ice-shelf three and period tributary 2001–2009, of glacierschanges to when in new all atmospheric glaciers and areice-shelf oceanic tributary retreating temperatures. glaciers in in response The R pinning to more of rapid recession the of ice-shelflogical the post-break controls up are in thereforefloating the strongly tongues mouth influencing following of the ice-shelf patterns R disintegration. and rates Ice-margins of retreat stabilised of after 2001 It therefore appears thatthus had the a removal strong of impactbreak the on up the ice would island’s shelf glaciers. immediatelywater changed a It ( has the been local suggested climate that ice-shelf and glaciers is particularly interesting,hibited because their on highest James annual rates Rossterminating of Island, retreat glaciers these in are glaciers thebalances ex- directly ice-shelf disintegration are influenced period. therefore by Land- a climatic sensitive perturbations indicator and of their climate mass variability ( figuration. However, this advance was subsumed(cf. by Fig. the overall large glacierstress, shrinkage faster flow, and short-term advance (cf., and rapid retreat.2001 The was therefore acceleration caused of byspheric recession ice-dynamical warming. factors, of exacerbated the Small byfrom continued ice amounts 1988 atmo- shelf of to growth in 2001, which in R mainland could of some be James ice-shelf because Ross Island, of glaciers and pinning was structural against observed and Persson dynamic Island variations and in the ice-shelf con- reach a new dynamiconce equilibrium they after become 2001 stabilised andously in been rates their observed of narrow to fjords. recession berates a began ( Indeed, major to fjord control reduce on geometry tidewater has glacier previ- advance and recession shelves from pinning points (such as Persson Island) can result in enhanced calving Vaughan highlights some important trends.highest For during glaciers feeding the PGIS,the period rates destabilisation of of recession of ice-shelf were and tributary disintegration. limit glaciers, glacier as Ice-shelf motion ice upstream removal of shelves can the reduce lead ice longitudinal to shelf stresses ( 5 5 10 25 25 20 15 20 15 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | c ), 2C 8 ) in- 5 1987 erential , ff van Lipzig C could be erent rates. ◦ ff C would raise d). The more ◦ 5 ) are most sensi- 5 Aristarain et al. ). These glaciers have ), a rise of 2 2009 plots above the accumulation values (such as GAP12) and , 2007 , 2C MEAN IPCC C per 1000 m ( ◦ ; calculated for these glaciers (Fig. 8 . 5 2C Jiskoot et al. − 2003 3566 3565 , values (such as GAP13; Fig. , and it is immediately obvious that the di ), which combined with high snowfalls ( 5 5 MEAN during the same interval. However, GAP17 has a very and 1 − 4 C rise in temperature, glaciers will still retain accumulation 6, compared with 1.8 for GAP18 (cf. Fig. ◦ . a g) is bedrock-controlled. Vertical joints in the hard Neogene Vaughan et al. 1 2 4 − 6 km . 0 ± 2 . C per 50 yr ( ), render them less susceptible to the changes in ELA brought about by ◦ 2004 , The tidewater glaciers on James Ross Island are likely to be extremely vulnerable to The outlet glaciers draining Mount Haddington Ice Cap typically have a large upland a 345 m rise in ELA.ter GIJR27, for glacier example, has may be a particularly large,area. vulnerable as low-lying Other this glaciers flat tidewa- with tongue, low-lying and tonguesering will ELA only have 20–30 projected % accumulation areas ofglaciers cov- their are area likely (e.g., to GIJR72, continuetion to GIJR115, areas retreat GIJR128, of very GIJR136). glaciers rapidly. on These Furthermore,will Mount result the Haddington in large Ice rapid accumula- loss Cap of are accumulation fairly area flat. here. An increase in ELA areas covering at leasttries 40 remain % similar. of The thevulnerable; steady a glacier steep rise slopes surface, in on assuming ELAtionally, these as does that glaciers these not glacier also glaciers expose render hypsome- a retreatdecrease them significantly towards in less larger the size, area grounding-line resulting to zones, in ablation ablation. a areas more Addi- will stable mass balance. tive to change. In general,have however, the large, tidewater high-elevation glaciers accumulation onto Eastern areas. Trinity the Peninsula Without prevailing climate, athey these further reach large strong their tidewater perturbation grounding-lines. glaciersdicates will that The most even ELA likely with stabilise a 2 when Given a calculated adiabatic lapseand rate assuming of that thecurrent isoline topographic of ELA zero mass valuesELAs balance calculated on over these are the glaciers, representative an Northernon increase of the Antarctic of hypsometric the 2 Peninsula curves by in 345 Fig. m. This is illustrated as ELA reached in the Antarctic Peninsula region between the “present” and the year 2040. hypsometry of the glaciersfuture. may be Bottom-heavy an glacierstop-heavy important with glaciers control with low-lying high on ELA ELA rates of recession in the et al. If atmospheric temperature risesrate over of the 2.5 Antarctic Peninsula continue at the current in the stepped hypsometricglacier curves long profile of (Fig. GIJR123basalts and and GIJR115 hyaloclastites (Fig. encourageglaciers 6). the then erode formation This a of unusual beneath, deep resulting steep in basin cirque partly in headwalls. floatingencourage the to further softer floating grounding-line The glacier Cretaceous retreat. tongues. sandstone Rising and sea mudstone levels would 6.4 Changes in equilibrium line altitude changing atmospheric temperatures (cf., large accumulation areas ifrendering future them less recession sensitive occurs to and an upwards thus shift recession in theaccumulation will ELA. area be on slow, theflat ice and low-lying cap, partly a floating steep or icefall floating over tongue. cirque These headwalls, attributes and can a be very observed retreated at 0 top-heavy HI index of stable glaciers on the Westernhypsometric Peninsula typically curves have (Figs. equi-dimensional or top-heavy accumulation areas situated athypsometric high curves altitudes, of which these contributes grounded to tidewater their glaciers stability. indicate The that they will retain Topography and hypsometry are important factorsand in may influencing explain glacier some massshows balance, of GAP17 the and inter-catchment variability GAP18GAP17 in (both remained recession outlet stationary rates. tidewater during glaciers) Figure the receding period at 2001–2009, di whilst the adjacent GAP18 6.3 Glacier hypsometry 5 5 25 20 10 15 25 10 15 20 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | , ) and Benn C since ◦ 2010 , Hulbe et al. ; 2003 , ). Numerous papers Holland et al. 2010 , ). Rapid recession of tidewater since 2001 (error estimated proba- ), driven by reduced sea-ice forma- Scambos et al. ), thus accelerating terminus retreat. 1 2002 − , a 2 2005 ), and possibly contributing to short-term , 2007a , 3567 3568 99 km 2002 . ). , Cook and Vaughan ). Furthermore, retreat of the terminus, as a re- 0 ; ± 4 . van der Veen 1991 2007b , 2008 , Benn et al. , ). Meredith and King Powell van der Veen ; ; Benn et al. 2008 1987 , , www.glims.org ). In grounded tidewater glaciers, terminus position may be controlled by 2002 , Glasser and Scambos Gille 2007a ; , The observed asymmetry and variability in recession in tidewater glaciers may be We measured variability in glacier length and area changes on the Northern Antarc- Of the 194 glaciers surveyed, 90 % showed rapid retreat from 1988–2001 and 79 % ¨ ohss Bay on James Ross Island and Snow Hill Island retreated faster from 2001– Meier and Post The Antarctic Peninsulasulted is in experiencing the rapid disintegration atmospheric of warming, many ice which shelves has ( re- glaciers in the regionbetween is advancing likely and to retreatingrecessional trends be glaciers, ( enhanced with by increased the calving asymmetry exacerbating of the the calving7 flux Conclusions et al. the local geometry of the fjord ( 2008 R 2009. Annual rates1988–2001. of Three recession distinct phases inshelf were disintegration land-terminating era); observed: 1997–2001 glaciers (period 1988–1997 of were (theriod immediate also adjustment); ice-shelf of 2001–2009 stabilisation and higher (pe- and ice- from long-termclimate-driven adjustment recession). to new Total dynamic glacierisedhas equilibrium declined area and at general in an thebilistically), average Northern of with 30 Antarctic total losses Peninsula from of 2001–2009. glacierised area of 11.1 % from 1988–2001 and 3.3 % small glacier advances. explained by complex calving processes.trolled by The crevasse calving depth, flux ice velocity, of strain tidewater rates, ice glaciers thickness is and con- water depth ( climate change on the cryosphere. retreated from 2001–2009, although thetially. rates Overall, and annual patterns rates of ofice-shelf recession recession vary tributary were substan- higher glaciers. from 1988–2001 Some in tidewater glaciers and on Western Trinity Peninsula, glaciers in data will be invaluableof to this numerical climatically modellers sensitive seeking region.from to GLIMS The predict ( full the glacier future inventory behaviour is available for download tic Peninsula between 1988, 1997,data 2001 for and monitoring 2009. glacierarea This recession and inventory on provides length the important presentedographical Antarctic in coverage Peninsula. this and tudy Changes amount considerably in of extend glacier detail the available hitherto for available understanding ge- the impacts of ( have documented the disintegrationoughly of and those quantitatively iceregion. investigate shelves, changes We but provide this in the is all firstislands to detailed the glaciers the inventory first southeast, in of to with 194slope, the detailed thor- glaciers estimates aspect, Trinity on of hypsometry, Peninsula Trinity size, morphological Peninsula length, and descriptors, elevation ranges, form ELA, and classification. These tion and atmospheric warming.extent) may influence Changes enhance in bottom melting sea-surface and temperatures thinning (and ( Tensile strength sea of ice glacier iceincreased decreases calving as rates ice ( becomessult more of temperate, increased resulting calving, in leadsand to glacier larger thinning, up-glacier further stretching exacerbating rates, increased greater calving ice rates speeds for tidewater glaciers 1951 ( therefore propensity to calve ( The calving fluxbe and largely recession controlled of byatures tidewater non-linear as glaciers glacier well in responses asperatures to the atmospheric around changes the study temperature Western in and region Antarctic oceanic precipitation Peninsula is temper- have gradients. risen likely by to Ocean more tem- than 1 6.5 Oceanic temperatures and climate forcing 5 5 25 20 25 15 15 20 10 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ) Coastal 3567 http://www.add.scar.org:8080/add/ 3567 ). Stefan Senk and Tristram Irvine-Fynne are 3548 3543 3570 3569 2005 ¨ Otztal Alps (1969–1997–2006), The Cryosphere, 3, ). This work was funded by NERC grant AFI 9-01 (NE/F012942/1). It is 3566 , erence in rates of recession. Raw data and shapefiles are available from ff www.glims.org 3564 of tidewater glaciers, Ann. Glaciol., 46, 123–130, 2007a. glaciers, Earth-Sci. Rev., 82, 143–179, 2007b. estimates of glacierRemote mass Sens. balances Environ., 108, in 327–338, 2007. the Himachal Pradesh (Western Himalaya, India), on the James Ross Island1987. ice cap, Antarctic Peninsula, Antarctica, J. Glaciol., 33, 357–362, glacier area and volume in205–215, the doi:10.5194/tc-3-205-2009, Austrian 2009. Glaciers on Trinity Peninsula that fed PGIS have stabilised since 2001, with slower Despite fears of continued run-away retreat and terminal destabilisation of tidewa- Tidewater glaciers on Western Trinity Peninsula remained stable between 1988 and Benn, D. I., Hulton, N. R. J., and Mottram, R. H.: “Calving laws”, “sliding laws” and the stability Berthier, E., Arnaud, Y., Kumar, R., Ahmad, S., Wagnon, P., and Chevallier, P.: Remote sensing Benn, D. I., Warren, C. R., and Mottram, R. H.: Calving processes and the dynamics of calving Aristarain, A. J., Pinglot, J. F., and Pourchet, M.: Accumulation and temperature measurements Abermann, J., Lambrecht, A., Fischer, A., and Kuhn, M.: Quantifying changes and trends in acknowledged for their help in programming and statistical analysis. References Acknowledgements. a contribution to thegrateful SCAR for ACE helpful (Antarctic andBolch. Climate constructive The Evolution) authors criticism Programme. acknowledge and Etienne(CNES) comments Berthier for The the and from authors SPOT-5 the images Hester are Centreaccess and Jiskoot National to the d’Etudes and SPIRIT ASTER Spatiales Tobias DEM.frontal images Neil positions from Glasser were was NASA determined providedChange as with from shapefiles, a no-cost mapped the by NASA-supported ADD Cook researcher. ( et al. ( The 1997 glacier data acquisition. Supplementary Data. Dataset forand the errors analysis for 1988, of 1997,and glacier 2001 the change, and with di 2009. areas,GLIMS lengths, Also ( given are calculated rates of change Supplementary Methods. Detailed information on methods used in glacier attribute zip dynamic equilibrium, and then retreat slowlyELAs. in response We to therefore warming anticipate climates and thatconcerned rising the with results the of more thisThe southerly project behaviour ice will of be shelves PGIS relevant that tributarymoval to surround can studies glaciers the be and Antarctic used their Peninsula. toice-shelf long-term model disintegration response events. and to predict ice-shelf glacier re- response to contemporarySupplementary and material future related to thishttp://www.the-cryosphere-discuss.net/5/3541/2011/tcd-5-3541-2011-supplement. article is available online at: the observed climatic warming, withexerting a glacier strong size, mitigating length, or slope, enhancing type, role. ELA and altitude ter glaciers, this study showsa that time-limited ice-shelf period tributary of glaciers adjustment. are Ultimately, ice-shelf more tributary likely glaciers to will undergo find a new on the Eastern Trinitywarming, Peninsula are but apparently they more mayzones. vulnerable stabilise to in continued the climate future as they retreatannual towards recession their rates grounding sincehave then. been On from low-lying James tidewater Rossare glaciers. Island, likely Annual the tidewater to largest glaciers arealcontrol recession continue for changes rates in the widespread response glacier retreat to in Northeast continued Antarctic atmospheric Peninsula is warming. apparently The primary 2009, and to dateprevailing show south-westerly only winds, slow and, unless rateswill strong of perturbation probably retreat. to remain this They stable system receiveglacier occurs, in thinning, abundant which snow areal is from extent. observedfrontal in stabilisation This other has occurred parts inference (Rott of et does the al., not Antarctic 2011). Peninsula, take In even contrast, account after large tidewater of glaciers 5 5 25 20 15 10 25 20 10 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | , 3551 3548 , 3579 , 3543 3548 3579 , 3562 3549 , 3547 , 3550 3551 3544 3548 er, M., Pettit, E. C., and Davies, B. 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J., 5 25 20 10 15 1020 1025 1015 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | . ◦ and ◦ er width cients ap- Remarks ff . Panchro- er width of er width of ffi ◦ ff ff er above ff , sun azimuth of ◦ 8 . 22 . Use of multiple im- , sun azimuth of 55 − 60 km. Datum: WGS84 2 ◦ × and sun elevation of 40.5 ◦ 22 − Panchromatic image. 120 km swath Captured at an incidenceof angle Derived fromlarge the footprint aboveSPOT-5 HRS (120 km stereoscopic two pairs swath) (Korona et al., 2009) Data Source Sensor onSatellite. Level the 1B Multispectral images. NASA Validated Terra and radiometric geometric coe Captured atgle an of incidence55.2 an- sun elevation ofmatic 37 image. 120 km swath plied. Coverage for eachis scene 60 Zone 21S LT4215105160XXX11 LT42161051990040XXX01 ages aids thesonal omission snow of sea- divide identificationsual, (DEM, vi- glaciologicaltions, slope, interpreta- aspect,hydrology tools) automatic (as above); checkingeral over images where sev- possible gins is covered incolumn the of thealso Table database. See Error is less thanincluded in 3 the pixels bu so is Visual checks and bu 22.5 m on eitherpolygon side of glacier Visual checks and bu 112.5 m on either sidepolygon of glacier ∗ ). James Ross Island: 23 Jan 2006 Dates as above for the two DEMs tured dates from 2001 to 2009 Antarctic Peninsula: 7 Jan 2006 9 Feb 1990 Panchromatic image. Scene ID: 5) Rau . 2005 5 m) . , 3580 3579 5 % Visual checks and bu . 22 112 10 % Multiple methods used for ice- 0 4 % Snow coverage of glacier mar- 15 m ± ± ± 3 pixels ( ± ± ± (RMS) for VNIR ( et al. 3 pixels ( , 6 m ± ) 15 m Various 40 m. Absolute horizontal precision ofRMS. 30 Vertical m pre- cision 5 m with an absolute horizontal precision of 30 m RMS (Korona et al., 2009) 2010 , Bolch et al. Granshaw and ) 2006 Bolch et al. , ) Sources of error and error mitigation in defining the area of each glacier polygon. Data sources used in Trinity Peninsula glacier inventory. ASTER VNIR (Advanced Spaceborne Thermal Emission and Reflection Radiometer) SPIRIT DEM (SPOT-5 Stereoscopic Survey of Polar Ice: Reference Images andphies) Topogra- Notes Resolution Date Cap- LANDSAT-4 TM 75 mSPOT-5 (Satellite Pour l’Observation de la Terre) HRS (High Resolution Sensor) orthoimages 29 Feb 1988 Panchromatic image. Scene ID: Error in co-registration and glacier size ( 2010 Fountain Identification of glacieraries (digital bound- mappingASTER error) images on Scene quality, clouds, seasonal snow, shadows ( Sources of errorsIce-divide andidentification drainage basin Uncertainty Mitigation Identification of glacieraries (digital bound- mappingLANDSAT error) image on Delineation oftongues ( debris-covered Refer to Supplement for further details of ASTER images. Table 2. ∗ Table 1. Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 2 , Trinity Peninsula. = AAR , ELA ) MEDIAN 2 THAR MEDIAN ratio (AAR) of 50H %. Equivalent to from hypsometric54 curves tidewater glaciers for over 40 km the mum glacier altitude cave contours of the ablation season ELA Island Ice Caps. ) area (km = 2 867 2378 407 75 90 15415262 6160 253 95 9198 66 89 3582 3581 ± ± ± ± ± er to either side of the glacier polygon. TP ff Vega Island. IIC = Glaciers area (km Median ElevationAccumulation Area Ratio Represents an accumulation Assumes an area AAR of 60 %; derived Toe to Headwall RatioHess Ratio method between minimum and maxi- Transient Snow LinesMean Altitude ELA of Transition between the convex and snow con- line at the end Mean of ELA Number of Total glacierised Total land % Glacierised MEDIAN AAR THAR HESS TSL MEAN TPJRIVIIICTotal 62 104 5827 24 1781 194 4 168 8140 365 Summary table of the glaciers of the Northern Antarctic Peninsula. Error is deter- Methods of ELA calculation. Refer to the Supplement for more information. Altitudes ELA ELA ELA ELA ELA ELA Method Description Notes James Ross Island. VI = JRI Table 4. mined by applying a 22.5 m bu Table 3. are derived from theyear 2006 2006. SPIRIT DEM, and these ELAs are therefore approximations for the Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 001 001 001 001 001 001 001 001 001 ...... value 0 0 0 0 0 0 0 0 0 P < < < < < < < < < James Ross Island. error = Standard 2 r TP JRI VI IIC All ” is the number of observations. “ltg” Adjusted n n 68 0.00 295.50 0.384 55 0.95 72.21 152 0.00 263.88 0.290 192 0.62 159.30 192 0.82 102.00 Trinity Peninsula. JRI Floating 10 16 2 0 28 Ice Field 1 0 0 0 1 = all glaciers. 3584 3583 Outlet glacier 27 45 11 0 83 Valley Glacier 21 16 0 0 37 = Partially Floating 20 16 5 0 41 Land terminating 1 48 7 0 56 Mountain Glacier 1 17 0 0 18 -values are calculated at the 95 % confidence level. ECR P TSL HESS AAR THAR Glacieret and snowfield 1 8 0 0 9 Total area lost 186 0.04 200.10 0.003 ELA ELA ELA ELA ) Mean Island Ice Caps. All MEAN = Summary of glacier descriptors. TP Regression table for variables in the inventory. “ MEAN MEDIAN MEDIAN MEDIAN MEDIAN Primary Classification Ice Cap 11 18 13 4 46 Tongue Grounded 31 24 10 4 69 1988 glacier area (ltg)Width of calving tongueELA Total area lost Total area (ltg)Maximum lost Elevation 55 Total area lost 115 0.19 186 0.03 3.24 8.377 0.14 0.041 428.78 ELA ELA Maximum ElevationMaximum ElevationMean Elevation GlacierMean length Slope GlacierMean area SlopeMean AspectMean 174 Aspect Glacier areaELA 192ELA Glacier area Glacier 0.79 length Mean 192 Elevation Maximum 0.48 Elevation 3.10 192 192 192 174 51.22 0.30 59.57 0.00 0.05 0.02 0.08 106.81 69.38 235.84 3.14 0.814 0.160 0.001 Variable AMean Elevation (H Variable B Vega Island. IIC = Table 6. VI Table 5. means “land-terminating glaciers”. Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Island = Vega Island. IIC = Number of Glaciers 49 1 15 3 0 19 19 11 11 4 1 27 . . 1988–2001 2001–2009 49 7 6 2 0 15 1 1 . er). “Stationary” glaciers have shown no 5 6 30 14 2 52 No. % No. % 1 − ff . < 1 5 35 42 1 1 79 < < . − HI 1 HI HI < < > < < 3586 3585 James Ross Island. VI 19 2 2 . . . = 1 1 − − AdvancingStationaryTotal 8 9 4.5Advancing 5.6Stationary 178Total 4 3 100 35 1 7.1 1.6 Advancing 184 19.0 1.8Stationary 56 100 Total 3 0 100 6 8 3.0Advancing 0 13.3 6.0 60Stationary 100Total 1 3 100 100 24 2 5.9 2.9 Advancing 103 23.3 11.8Stationary 17 100 0 0 2 100 0 0.0 0 11.8 17 0 100 0 1 0 25.0 Glacier Hypsometry TP JRI VI IIC All Trinity Peninsula. JRI = all glaciers. All glaciers Retreating 160 89.9 146 79.3 Trinity Peninsula Retreating 51James Ross Island 91.1 Retreating 52 91Vega Island 86.7 91.0 76 Retreating 73.8 Island Ice Caps 14 Retreating 82.4 15 4 100.0 88.2 3 75.0 = Number of glaciers in each hypsometric class. Categories are from Jiskoot ). TP Number of glaciers advancing and retreating in the period 1988 to 2009. Note that 1 Very bottom heavy Class Description35 Equidimensional Value Very top heavy HI 2 Bottom heavy 1 4 Top heavy 2009 missing data meansis not greater all than 194 thechange glaciers greater mapped than were error the error. included. (margin only Glacier bu change is only noted if it Table 8. Ice Caps. All Table 7. et al. (

Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 64°0'0"S

Island Ice

= Island Andersson 395.6 218.1 136.1 19.3 22.2 ± ± ± ± ± Marambio Cape Green Kilometres GAP40 720 m ISLAND Cockburn Island SEYMOUR 41 GAP 5

GAP43 EREBUS AND EREBUS Esperanza TERROR GULF TERROR 57°0'0"W 57°0'0"W GAP38 Gage Cape

GAP42 GAP39

Projection: WGS UTM 1984 Zone 21S Projection:

0 102030 Ula Point ISLAND GAP36 GIJR132

SNOW_HILL

GIJR131 UND GIV22 BAY 930 m

GAP37 VEGA

Point

GIV12

Y SO Y GIJR134 Hamilton MARKHAM GIV15 Rabot Point

Skep Point GAP35 LT GIJR122 SNOW HILLISLAND Vega Island. IIC DUSE BAY DUSE

Humps IslandHumps MIRA

=

AD GIV26 GIV10 GIV09 Snowfield GIJR128 GAP34

GIJR136 m

GIV28 Belen GIJR119 Fjordo GIJR137

GIV05

610 GIJR118

GAP33 GIJR124 The Naze

EAGLE ISLAND JR123

GAP32 GI CORRY ISLAND CORRY 67 GIJR117 Hill GIV29 GIJR 1600 m Terrapin GIJR64 ISLAND Eyrie Bay Eyrie Point LOCKYER

BERT SOUND Jefford GAP26 CROFT BAY CROFT GIJR115

HER Cove St Martha Swift GIJR109 Glacier

GIJR61 ICE CAP R113 GIJ GAP30

HADDINGTON

GAP45 ROSS ISLAND JAMES GAP25 GAP31 970 m

GIJR97 GAP24 Cape Foster Cape Lachman Cape Broad Valley Mendel Tait Bay GIJR108 58°0'0"W GAP46 GIJR93

GIJR23 GIJR27 DOME Glacier Brandy DOBSON 28.4 5980.3 6689 15.2 1992.6 2192 1.2 169.8 178 4.8 389.5 400

GIJR95

GIJR112 GIJR72 58°0'0"W GIJR92

49.1 8532.1 9460 GAP47

GIJR96 GAP49 GIJR99 ± ± ± ±

Bay Bay GIJR106 Ulu Peninsula Ulu ± Carlsson Whisky GIJR84 . Long Island

GAP48

2 GIJR90 BAY

GAP50 GAP23 3588 3587 RÖHSS RÖHSS

Bay

Nygren Point Nygren

GAP21 NEL 660 m Island AN Persson Holluschickie GIJR87

22

Cliffs Cape Broms

2 Glacier

615 m GAP51

GAP5 down down

GAP le Russell East Russell Tumb Plateau

Cove Rum

GAP19 GAP20 Louis-Philipe James Ross Island. VI CH GUSTAV

= Victory PRINCE Glacier as as 1280 m TRINITY

Longitudinal Foliation Longitudinal Pressure Ridges Rifts Crev sse (1988) 6

PENINSULA P1 Glacier GAP53 GA Aitkenhead GAP01 ns GAP18 io 86.2 1902.4 6.8 380.6 GAP55 Glacier Diplock Glacier 261.7 8414 153.9 5961.6 14.8 169.8

GAP54 GAP02 Russell West Sjögren Inlet

GAP03 ± ± GAP08 tu 59°0'0"W ± ± ± GAP17

Research Stat Alti de 200 m contours Rivers Lakes Moraine 4

Glacier Boydell

P0

in IsJames Ross Peninsula and nd Glacial Map GAP09

59°0'0"W GA Tr ity la GAP56 Pettus

Glacier GAP10 GAP15 4 2 P1 3 GA GAP05 GAP1 GAP1 GAP57

GAP58

GAP06 GAP11 Glacier Sjögren Glacier Eliason GAP60 GAP59 SEA 9 GAP07 INLET LARSEN LARSEN

-200 ICE SHELF WEDDELL WEDDELL Pyke GAP61 Polaris Glacier Glacier Trinity Peninsula. JRI Albone Glacier = Glacier extent and ice divides, 2009 extent Glacier 2001 Glacier extent 1997 Glacier extent 1988 Glacier extent outside Ice study area all glaciers. All area is given in km Glacier Extents 1988 Extents Glacier

=

Glacier change, 1988 to 2009. Note there is particularly limited data for 1997. Error AreaAll Area 2009 8140.4 Area 2001 Area 1997 Area 1988 TP 5827.3 JRI 1780.5 VI 167.8 IIC 364.7 Area LostAll 2001–2009TPJRIVI 1988–2001IIIC 1997–2001Area 274.1 Gain 1988–2009 134.3All 121.9 2001–2009TPJRI 1.9 16.0VI 1988–2001 1045.5IIC 727.8 1988–2009 290.0 0.09 117.7 0.00 0.06 19.6 8.1 18.7 90.2 0.00 1319.5 0.00 0.08 0.03 0.00 862.0 0.00 0.05 411.9 0.00 0.00 0.13 0.03 35.6 10.0 0.10 0.00 0.00 60°0'0"W 64°0'0"S Index map of James Ross Island, Vega Island, Snow Hill Island and Trinity Penin- er on either side of the ice front only, and is therefore a minimum error of ice front change ff Fig. 1. sula, Northern AntarcticID Peninsula, codes. showing ice Glacier divides,ages extents (refer glacier in to drainage Supplement) 2009, basins usedin 2001, in and the 1997 making glacier Universal this and TransverseZone map Mercator 1988 21S. and (UTM) are all projection shown. subsequent World maps Remotely-sensed were Geodetic projected im- System (WGS) 1984 Caps. All Table 9. margin for 2009 includes errors inherentin in 2001 polygon and determination. 1988 As assumes analysis nobu of migration of frontal ice change divides, error is calculated by using a 3-pixel wide only. Where data is missing,year it and is the assumed that lastestimate. the year glacier TP for did which not change data in was size available; between that therefore, these figures are a minimum Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Cor- follows in 2009 (H) 30 350 1000.00 = 0.79 2 r Length Length 20 25 ) 2 10.00 100.00 Lake Cirque headwall Crevasse Moraine Ice-free land Glacier flowline 2009 200 m contours River 8) between glacier .

0

64°20’0"S 64°10’0"S Relationship between 1.00 10 15 = Glacier length (km) Glacier area (kmGlacier area Mean aspect (degrees) (I) 2 r GIJR122 GIJR121 GIJR138 GIJR120 I C F 05 SNOW_HILL 0 50 100 150 200 250 300 0.01 0.1 GIJR128

0 5 0

20 25 15 10

500 0

2500 2000 1000 1500 GIJR139

Glacier maximum elevation (m a.s.l.) (m elevation maximum Glacier 100 800 600 400 200

1600 1400 1200 Mean elevation (m a.s.l.) (m elevation Mean GIJR123A (degrees) slope mean Glacier GIJR137 GIJR119

GIJR136

) GIJR130 (km covered Area 2 GIJR71 GIJR118A GIJR124 0 6000 5000 4000 3000 2000 1000 1000.00 E TSL AAR AAR HESS THAR THAR GIJR123

GIJR118 2 ELA ELA ELA ELA ELA GIJR67 ELA = 0.62

2

r > 100 km 100 > LOCKYER

GIJR66 2 values.

GIJR117 50.0-99.99 km 50.0-99.99

= 0.95 p 2 2 ) r 2 GIJR64 10.00 100.00

) 10.0-49.99 km 10.0-49.99 2

GIJR116

2 for

5.0-9.99 km 5.0-9.99 1.00

5 2 3590 3589 Glacier area (kmGlacier area Elevation (m a.s.l.) Elevation Size class (kmSize

GIJR62

Relationship between maximum elevation and area GIJR115 km 1.0-4.99

400 1600 1800 2

GIJR61 0.5-0.99 km 0.5-0.99

GIJR109 erent mean elevations, separated according to region. (D) 2 ff H Area covered Area Count of glaciers Count

0 200 600 800 1000 1200 1400 B 0.01 0.1

0.1-0.49 km 0.1-0.49 0

0

200 800 400 600

1200 1000 1400 1600

800 600 200 GIJR56 400 Glacier mean elevation (m a.s.l.) (m elevation mean Glacier 1200 MEDIAN 1800 1600 1400

1000 ELA 0 60 50 40 30 20 10 Number of glaciers (n) glaciers of Number erent methods of ELA calculation. GIJR58 GIJR114 ff GIJR113 GIJR97 erent glacier area classes, compared with total area covered GIJR55

GIJR94 GIJR111 ff

30 GIJR95 1100 > = 0.53 GIJR108 58°0’0"W GIJR112 2 GIJR54 r GIJR93 and di

58°0’0"W

Trinity Peninsula Trinity 1000-1099.99 Islands All glaciers James Ross Island Island Vega 900-999.99 Scatter plot showing a strong relationship (

20 25 800-899.99

)

GIJR110 GIJR92 2

GIJR106 700-799.99 GIJR96 MEDIAN

(C)

600-699.99

GIJR72 GIJR99 500-599.99

was measured from the highest to the lowest point on the glacier polygon. 10 15

Kilometres 400-499.99 Glacier length (km) Glacier area (kmGlacier area GIJR84

GIJR105 3 300-399.99 Scatter plot showing a weak relationship between mean elevation and glacier GIJR103 Classes of mean altitude (m a.s.l.)

GIJR104

GIJR100 200-299.99

GIJR76 GIJR107

GIJR90 100-199.99 Number of glaciers with di Trinity Peninsula Trinity James Ross Island Island Vega GIJR77 (E) A 0612

D

G 05

0.-99.99 0.-99.99 0.01 0.1 1.00 10.00 100.00 1000.00 GIJR86

0

50 30 10 60 40 20

0 Scatter plot showing a weak relationship between mean slope and log glacier area. 50 0

Number of glaciers (n) glaciers of Number 450 400 350 250 100 200 300 150

Length

500

-500 64°10’0"S 64°20’0"S 1500 2500 2000 1000 ) (km area Glacier Glacier maximum elevation (m a.s.l.) (m elevation maximum Glacier 2 5). Subset of the glaciological map for James Ross Island, showing mapped . (F) 0 Frequency distribution of di Scatter plot showing a strong relationship between glacier area and glacier length. = 2 r relation between ELA maximum elevation and glacier length. mean aspect and mean elevation. See Table (G) Fig. 3. (A) ( area. the steepest downhill gradient; inpossible. the accumulation area, it follows the centre line as closely as (B) by each size class. Fig. 2. along the centre line of each glacier drainage basin. In the accumulation area, Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | , ) MEAN MEAN for each C/1000 m) in MEAN ◦ 8 . 5 − = 158 =535 = 741 =559 =362 =880 = 1086 = 904 MEAN 2C MEAN 2C MEAN 2C MEAN 2C MEAN ELA HI = 1.6 ELA ELA HI = 1.8 ELA ELA HI = 1.1 ELA ELA HI = 1.2 ELA MEAN ELA MEAN B D MEAN ELA ELA GIJR123 GIJR115 GIJR128 ELA GIJR27 GIJR128 GAP18 GIJR136 GAP53 GIJR123 Mean aspect of the glacier 2C 2C 2C 2C erent hypsometric indices in ELA

ELA ELA Equi-dimensional ELA

0 0.2 0.4 0.6 0.8 1 ff GIJR115 Ice Fall Floating tongue CentralFlowlinedistance(m) Glacier Long Profiles Percentages of glaciers in each (C) = 721 =742 =812 = 1066 =876 =1087 = 1238 No data MEAN 2C = 1221 MEAN 2C MEAN 2C (E) MEAN 2C Accumulation area ELA HI = 1.8 ELA MEAN ELA HI = 1.5 ELA ELA HI = 1.0 ELA 0 2000 4000 6000 8000 10000 12000 14000 16000 18000 20000 MEAN ELA HI = -1.1 ELA 0 MEAN ELA 800 600 400 200 2000 1800 1600 1400 1200 1000 ELA MEAN ELA No Data ELA GIJR128 GAP07 GIJR123 GAP14 Trinity Peninsula James Ross Island Vega Island Other Islands Very top heavy (HI < -1.5) 600 - 699.99 700 - 799.99 800 - 899.99 900 - 999.999 1000 - 1099.99 1100 - 1199.99 1200 - 1299.99 2C 2C 2C 2C Equi-dimensional ELA ELA ELA ELA 00.20.40.60.81 Top heavy (-1.2 1.5) (1.2 < HI <1.49)

5 0

45 40 35 30 25 20 15 10 MEAN GIJR72

GAP60 r f e N s c aie Gl o b m u r GAP45 GIJR97 ELA MEAN 2C ELA 2C 2C 2C E ELA ELA ELA 0 0.2 0.4 0.6 0.8 1 Trinity Peninsula James Ross Island Vega Island NE SE Kilometres 12.5 =1067 = 312 =661 =893 02550 =1412 =657 = 1006 = 1238 MEAN 2C MEAN 2C MEAN 2C MEAN 2C ELA HI = -1.7 ELA ELA HI = 2.0 ELA ELA HI = 2.1 ELA MEAN ELA HI = -1.5 ELA S MEAN N 40 MEAN 0 20 MEAN ELA ELA ELA ELA No data ground GAP12 Glacier mean aspect GAP13 GIJR108 GIJR115 indicates the possible change in equilibrium line with future climate 2C Floating Partially floating Grounded Land terminating No data SW NtoNE NE to E EtoSE SE to S StoSW SW to W WtoNW NW to N NW 2C Frequency distribution of glaciers with di 2C ELA 2C 2C EFG ELA ELA ELA Tongue Glacier Inventory 2009

0 0.2 0.4 0.6 0.8 1 Glacier mean aspect W Long profiles of three tidewater glaciers on James Ross Island.

Trinity Peninsula Top heavy Top Bottom heavy heavy Top Bottom heavy James Ross Island 1 0 1 0 1 0 0 1 0.9 0.8 0.7 0.6 0.5 0.4 0.3 0.2 0.1 0.9 0.8 0.7 0.6 0.5 0.4 0.3 0.2 0.1 0.9 0.8 0.7 0.6 0.5 0.4 0.3 0.2 0.1 0.9 0.8 0.7 0.6 0.5 0.4 0.3 0.2 0.1

d u t i t l A d e s i l a m r o N (F) e (G) Distribution of glacier hypsometric classes. C warming could result (presuming an adiabatic lapse rate of Mean ELA for each glacier polygon. Glaciers in red have the highest ELA ◦ Distribution of floating, partially floating and grounded glacier tongues at glacier (D) (B) Normalised hypsometric curves of representative tidewater glaciers on Trinity Peninsula erent regions. ff a rise in ELA of 345 m by 2040. and James Ross Island. Hypsometric Index (HI) and mean equilibrium line altitude (ELA Fig. 5. change. A 2 glacier is plotted. ELA are given in the top right hand corner for each glacier graph. The normalised ELA Fig. 4. (A) termini. while glaciers in dark blue have ELA polygons. cardinal direction. di

Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper |

u 0 1 0 s r c a l g y r a t b i r ) m 0 2 - 0 2 , e i t k ( 9

I r o c h e i a l S G P f e g n a h t g n e l r c G GIJR01 GIJR02 GIJR03 GIJR05 GIJR08 GIJR10 GIJR130 GIJR135 GIJR120A GIJR121A

8 7 6 5 4 3 2 1 0

4 0 R J I G

2 2 1 R J I G J I G A 8 1 1 R

5 2 1 R J I G

3 3 1 R J I G

0 4 R J I G

9 4 R J I G

2 5 R J I G

4 5 R J I G

5 5 R J I G

6 5 R J G I on James Ross

8 6 1 R J G I

7 7 R J G I

25

6 8 R J I

G ) on James Ross

25 9 I 1 R J G 2

2 4 0 R J I G

2 2 R J I G 1 A 8 1 1 R J G I

East-coast glaciers glaciers West-coast PGIS tributary glaciers

5 2 1 R J I G

3 3 1 R J I G

0 4 R J I G

9 4 R J I G

2 5 R J I G

5 R J I G

4 89 0

5 5 R J I G

6 5 R J G

I 3 km

8 6 1 R J I G

7 7 R J I G

6 8 R J I G

1 9 R J I G > Scatter plot showing poor Months to 2009 February Months to 2009 February 200 0 252 (D) GIJR55 GIJR04 GIJR91 GIJR86 GIJR68 GIJR54 GIJR52 GIJR49 GIJR40 GIJR133 GIJR125 GIJR122 GIJR118A GIJR77 GIJR56 F Width of calving front (km)Width of calving front 250 150 100 50 C 0% 30% 40% 20% 10%

0

1.0 0.8 0.4 0.2

0.6

d n a l s I s s o R s e m a J n o m k 1 < s r e i c a l g

a J 3 s e d n l s I s s o R s e m a n o m k > r i c a l g

2 Glacier Length 2009 (km)

2

m ( r r i G n i m t - d a l n )

k a e a e c a l g t a n i r e n i t r t n r e a % g n i a n i m e - d n a l i a e a n i g n h c 2

530

0 V I I G 1 530

GIJR91 GIJR77 GIJR118A GIJR133 GIJR56 GIJR122 GIJR125 GIJR55 GIJR40 GIJR86

0 V I I G 1

R I 91 J G 3 1 V I I G

6 GI R8 J

2 V I I G 1 0 J 0 R G 8 I

J 9 R GI 7

2 2 V I I G

JR 7 GI 7

Non-tributary glaciers PGIS tributary glaciers

D

GIJR76

2 V I I G

8 B

J 5 G R7 I

Recession over time of land-terminating

JR70 GI 0101520 0 3 V I I G

0101520

6 IJR G 8

0 GIJ 6 R5

0.8 1.6 1.4 1.2 0.4

9 0 2 c a l r e t w

t ) m k ( 0 0 2 - 1 0 , s r e i g i a e d

JR G 5 I

5 0

--1

-0.2 -0.4 -1.2 -0.6 -0.8 JR G 4 I 5

1 0 V I I G

GIJR 2001-2009 GIJR 1988-2001 J R53 G I

m ( a n k e g n a h c h t g n e l f o e t a r l u n A ) a e t G l s i n e P t i n i r T r o f g n a h c h g n e l r i c a l a u n y e

JR52 I G 1 - 2

GI R51 J

J R49 GI

(B) IJR G 48

47 IJ R G JR42 GI

89 0

J R45 I G 4 1 J R GI 2 2 V I I G

GI 4 0 JR GIJR39

Variance in rates of change for land-terminating JR38 G I

0 3 V I I G J R37 GI

I JR34 G

JR24 G

I GAP12 GAP13 GAP14 GAP15 GIJR84 GIJR90 GIJR92 GIJR93 GIJR95

0 GIJR1 4

3594 3593

139 J G R Months to 2009 February I

38 J G R1 I

5 GI R13 J

3 3

GIJR1 (H)

JR130 G I

7A 12 J G R I

R1 J 25 GI

252 Months to 2009 February 1 22 J R GI

21 J G A R I 1

G IJR120A glaciers Land-terminating

JR120 G I

8A GIJR11

GIV10 GIV01 GIV13 GIV22 GIV21 GIV28 GIV30 200

JR110 GI

Rates of glacier length change in tidewater glaciers on 1 0 JR G

B I

08 J G R

I 1988-2001 2001-2009

JR05 G

0 I )

8% 6% 4% 2%

GIJR04

a I g V n e i c l d n l s a e o s r a g

IJR03

G -1

2 J R0 GI

t r t e g n i a n i m e - d n a l n i a e r a n i g n a h c %

01 GIJ R H 250 150 100 50 E

7 3 9 5 (A)

- Glacier change for small land-terminating glaciers on James 15 13 11

m 3 > s r e i c l g d n a l s I s s o R s e m a J o k a

n 0%

2 -0.1 % -0.2%

s s o R a d n a l s I s e m J n o

m k ( e r r e i a G g n i t a n i m r e t - d n a l n i )

a a c l

2

m ( a a e c l n g n h o e t k e r r i a g i e a c f a R )

GIV10 GIV13 GIV21 GIV22 GIV28 GIV30 a

1 - 2

0 R J I G 1 0

(D)

2 0 R J I G

3 0 R J I G

Percentage change for small land-terminating glaciers (less than

5 0 R J I G

0 1 R J I G

Prince Gustav Ice Shelf Tributary Glaciers

J 0 1 R I A 2 G

A 1 1 J I G 2 R

0 J 3 1 R I G

5 3 1 R J I G

(C)

8 1 J I G R 3 11; see Table 5).

.

2 0 R J I G 1 0 R J I G

3 R I J G 0 0

Scatter plot showing poor correlation between 2009 glacier length and 0 J I G 5 R

Chart illustrating change in glacier area for tributary glaciers to Prince 0 1 R I J G

G A 0 2 R 1 J I

=

89 0

), 1988-2009 1 2 1 R J G I A 2009 Months to February

2

0 3 1 R J I G

1 J 3 R I G 5 2 EasternTrinity Peninsula

WesternTrinityPeninsula

Percentage change for land-terminating glaciers 3 1 R J I G 8 r (B) 200 0 (C) Months to 2009 February Months to 2009 February -2.5 Rate of change in glacier length (km a Area lost (km 200 0 (E) 252 2 2 2 A C 250 150 100 50 Percentage change in surface area for land-terminating glaciers on Vega Island. GIJR01 GIJR02 GIJR03 GIJR05 GIJR10 GIJR120A GIJR130 GIJR135 GIJR138 < 1 km 1 - 3 km > 3 km Glacier change for and-terminating glaciers (greater than 3 km Scatter plot demonstrating a weak correlation between change in glacier area and 250 150 100 50 -0.50 0.00 0.50 1.00 1.50 2.00 2.50 3.00 D -3.5 -3 -2 -1.5 -1 -0.4 G A 4 8 0 16 12

8 0 4

8 6 4 2 0

0% 16 12

16 14 10 12 40% 60% 80% 20%

-60% -20% -40%

a g e V a d n l s I a n o s r e i c l g d n a l s s s e m a o m k 1 s e i c I s o R J n < r a l g

e r r i a G m k ( a e c s r e i c a l g y r a t u b i r t S I G P r o f ) a l

1 ) k a r e c 8 8 9 , m ( a e r i a l G

2

2 2

t i i r e t - d n a l n i ) g n i m k ( a e r r e c a G a n m a l t r t e n a h c % g n i a n i m e - d n a l n i a e r a n i g 2 (F) Tidewater glacier length. (G) ) on James Ross Island. 2 length changes. Fig. 7. Trinity Peninsula. Gustav Ice Shelf. Note that most change occurred prior to 2001. Island. Island. initial glacier size ( correlation between the width of the calving front and the change in glacier length. glaciers on Vega Island. Ross Island. 1 km glaciers on James Ross Island. Many glaciers receded after 1997 and 2001. Fig. 6. (A) Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | (C) Overall (A) -1 Faster 1988-2001Faster 2001-2009Faster No recession rate of recessionSame data Insuficient 0.000001 - 0.053000 0.000001 - Insufficient data -12.929000 --12.929000 -9.963000 --9.962999 -3.701000 --3.700999 -2.061000 --2.060999 -1.097000 --1.096999 -0.646000 --0.645999 -0.401000 --0.400999 -0.223000 --0.222999 -0.131000 --0.130999 -0.089000 --0.088999 -0.054000 --0.053999 -0.028000 --0.027999 -0.009000 --0.008999 0.000000 a 2 Difference in glacier recession glacier in Difference Glacier change 1988-2001 change Glacier km Difference in in recession Difference Recession 1988-2001 Recession 3595 erent time periods. Glaciers in red retreated fastest, ff Glacier extent 2001 extent Glacier 1988 extent Glacier Kilometres -1 -1 -9.195000 --9.195000 -6.560000 --4.345000 -2.353000 --1.818000 -1.312000 --0.956000 -0.627000 --0.573000 -0.402000 --0.218000 -0.115000 --0.108000 -0.067000 --0.065000 -0.037000 --0.036000 -0.014000 --0.012000 0.002000 data Insufficient -2.671000 --2.671000 -2.355000 --2.354999 -1.447000 --1.446999 -0.811000 --0.810999 -0.396000 --0.395999 -0.212000 - -0.114000 -0.211999 - -0.070000 -0.113999 --0.069999 -0.042000 --0.041999 -0.023000 --0.022999 -0.007000 --0.006999 0.000000 0.136000 0.000001 - data Insufficient 12.5 a a 2 2 Glacier change Glacier km Glacier change 2001-2009 change Glacier km Former glacier extents glacier Former 02550 CD AB ¨ ohss Bay advanced during this period (coloured purple).

GAP40

GAP39

SNOW_HILL

GIJR136 GAP34

GAP32 GIJR64

GIJR61 GIJR115

GAP45

GAP31

GAP23 GAP51

GAP53 GAP55 GAP18 GAP15

GAP02

GAP08 GAP56 GAP17

GAP14

GAP05

GAP58 GAP60

GAP61 Recession 2001-2009 Recession Recession 1988-2009 Recession GAP07 erence in recession rates. Glaciers in blue retreated fastest between 1988 and 2001; Annualised rates of recession for di ff Di Glacier rates of recession, 1988–2001. PGIS tributary glaciers retreated fastest. Note that glaciers in red retreatedafter fastest 2001. after 2001. Note that PGIS tributary glaciers retreated slower Glacier rates of recession, 2001–2009.(D) Note a few small advancing glaciers (coloured purple). two PGIS-tributary glaciers in R glacier recession, 1988–2009. Note(B) the slow rates of recession on Western Trinity Peninsula. Fig. 8. and glaciers in darkRecession blue category had the values slowest are annual determined recession rates. by Natural Glaciers Breaks in pink (Jenks) advanced. method.