1.1. Rationale

The glaciers of the Patagonian Andes and Tierra del Fuego region are currently shrinking rapidly. Regional assessments of glacier shrinkage are, however, only short-term because they are limited by the temporal availability of satellite observations (~40 years), aerial photography (~60 years) and detailed cartography (~60 years) required to produce accurate reconstructions of former glacier extent. Furthermore, inventories and assessments of modern glacier change in Patagonia have generally been restricted to individual glaciers (e.g. Reference Harrison and WinchesterHarrison and Winchester, 2000;Reference Stuefer, Rott and SkvarcaStuefer and others, 2007) or geographically limited to one or two of the large icefields (e.g. Reference Rivera and CasassaRivera and Cassassa, 2004;Reference Bown and RiveraBown and Rivera, 2007;Reference Chen, Wilson, Tapley, Blankenship and IvinsChen and others, 2007;Reference Schneider, Schnirch, Acuna, Casassa and KilianSchneider and others, 2007;Reference Lopez, Chevallier, Favier, Pouyaud, Ordenes and OerlemansLopez and others, 2010;Reference Willis, Melkonian, Pritchard and RamageWillis and others, 2011). Large parts of the southern Andes still lack detailed inventories (Reference Masiokas, Rivera, Espizua, Villalba, Delgado and AravenaMasiokas and others, 2009a). There are no detailed assessments that encompass the entire region, covering both historically documented shrinkage and remotely sensed observations of change in recent decades. This paper therefore aims, firstly, to establish rates of glacier shrinkage from the Little Ice Age (LIA) to the present day across southern South America, and secondly, to determine how rates of shrinkage changed through the late 20th and early 21st centuries.

We here present a long (140 years) and spatially wide (2000km in length) record of glacier change in South America (41–56° S) by calculating changes in glacier length and area between the end of the LIA (~AD1870) and the years 1986, 2001 and 2011, with some limited additional data from 1975. This is the first study to compare length and area changes since the LIA with change in recent decades for the whole study region. We also analyse spatial and temporal variability in glacier change and the controls thereupon. Our data are available from the Global Land Ice Measurements from Space (GLIMS) database (www.glims.org).

1.2. Study area

The Andes is the longest continental mountain range in the world, stretching 7000 km along the coast of South America and reaching almost 7000ma.s.l. In our study area, the mountains reach a maximum of 4000 m a.s.l., decreasing to 1500–2000m in southernmost South America. Between 38° S and 56° S there are four major ice masses (the Northern and Southern Patagonia Icefields, Gran Campo Nevado (GCN) and Cordillera Darwin) and numerous snow- and ice- capped volcanoes and icefields (Fig. 1). Our study area focuses on the Patagonian Andes and Tierra del Fuego, from 41° S to 56° S. This region has been the subject of numerous detailed local studies covering glacier behaviour over various timescales, and there is good historical and geo- morphological evidence for glacier fluctuations since the LIA (summarized by Reference Masiokas, Rivera, Espizua, Villalba, Delgado and AravenaMasiokas and others, 2009a).

Fig. 1. Location of the main icefields and glaciers in southern South America, showing abbreviations used in text and tables. The inset shows the wider location of the study area. Mean annual temperature data for the four temperature transects were obtained from Reference Hijmans, Cameron, Parra, Jones and JarvisHijmans and others (2005) from a 1 km resolution raster dataset. Note decreasing temperatures over the icefields and in areas of high elevation. Local variations reflect the influence of fjords, rivers and mountains. Precipitation data for stations where there were records longer than 10 years were obtained from the Direccion Meteorologica de Chile. Note the strong west-east precipitation gradients that exist across the study area and the low number of stations; precipitation values at each glacier are therefore uncertain. Lakes larger than 15 km² are shown.

The Chilean Lake District (38–42°S) is characterized by shrinking glaciers on active volcanic cones, with frequent ash deposition insulating the ice. These volcano ice caps have been thinning since observations began in 1961, with more rapid thinning from 1981 to 1998. Their negative mass balances were caused by decreased precipitation and upper-tropospheric warming over the last 30 years (Reference Bown and RiveraBown and Rivera, 2007). Equilibrium-line altitudes (ELAs) are at ~1600m at 43° S (Reference Rivera, Bown, Carrion and ZentenoRivera and others, 2012). Glaciers north of 42° S receive higher precipitation during winter months than glaciers between 42° S and 49° S (Reference Sagredo and LowellSagredo and Lowell, 2012).

The Northern Patagonia Icefield (NPI) covers an area of ~4200km² at 47° S (Fig. 2a). Its survival at such a low latitude is attributed to a large volume of precipitation (up to 10000 mm w.e. a^-1) and to the cool temperatures associated with the high elevation of the Andes (Reference Rott, Stuefer, Siegel and Skvarca Pand EckstallerRott and others, 1998; Reference Michel and RignotMichel and Rignot, 1999;see temperature transects in Fig. 1). The NPI is characterized by high ablation rates, steep mass-balance and precipitation gradients and high ice velocities (Reference Lopez, Chevallier, Favier, Pouyaud, Ordenes and OerlemansLopez and others, 2010). The glaciers of the NPI extend below the 0°C isotherm, and the snowline is generally below 2000ma.s.l. (Reference Sagredo and LowellSagredo and Lowell, 2012). The recent fluctuations of NPI outlet glaciers have been extensively studied (Reference AniyaAniya, 1988, 1995, 1996, 1999, 2001, 2007;Reference Harrison and WinchesterHarrison and Winchester, 2000;Reference AranedaAraneda and others, 2007;Reference Chen, Wilson, Tapley, Blankenship and IvinsChen and others, 2007; Reference Lopez, Chevallier, Favier, Pouyaud, Ordenes and OerlemansLopez and others, 2010). Glaciar San Rafael is the only tidewater glacier of the NPI; it is the world’s lowest-latitude tidewater glacier and is among the fastest-flowing glaciers in the world (Reference Warren, Glasser, Harrison, Winchester, Kerr and RiveraWarren and others, 1995;Reference Koppes, Conway, Rasmussen and ChernosKoppes and others, 2011). Peak velocities of 19.7 ± 1.2 m d^-1 were observed in 2007 by Reference Willis, Melkonian, Pritchard and RamageWillis and others (2011). Laguna San Rafael is dammed by large arcuate moraines that were formed during a mid-Holocene readvance of the glacier (Fig. 2b;Reference Harrison, Glasser, Duller and JanssonHarrison and others, 2012).

Fig. 2. Location of the main icefields and glaciers in southern South America, showing abbreviations used in text and tables. The inset shows the wider location of the study area. Mean annual temperature data for the four temperature transects were obtained from Hijmans and others (2005) from a 1 km resolution raster dataset. Note decreasing temperatures over the icefields and in areas of high elevation. Local variations reflect the influence of fjords, rivers and mountains. Precipitation data for stations where there were records longer than 10 years were obtained from the Direccion Meteorologica de Chile. Note the strong west-east precipitation gradients that exist across the study area and the low number of stations; precipitation values at each glacier are therefore uncertain. Lakes larger than 15 km² are shown.

The Southern Patagonia Icefield (SPI) stretches along the southern Andes, reaching altitudes of 3400 m. It is drained by temperate outlet glaciers, terminating on land or in proglacial lakes or tidal fjords (Reference Aniya, Sato, Naruse and Skvarca Pand CasassaAniya and others, 1997). Variations in glacier frontal positions have been studied since the 1940s, with long-term retreat (Reference Aniya, Naruse, Shizukuishi and Skvarca Pand CasassaAniya and others, 1992, 1996, 1997;Reference AniyaAniya, 1996, 1999; Reference Lopez, Chevallier, Favier, Pouyaud, Ordenes and OerlemansLopez and others, 2010) and thinning (Reference AniyaAniya, 1995;Reference Naruse and Skvarca Pand TakeuchiNaruse and others, 1997; Reference Naruse and SkvarcaNaruse and Skvarca, 2000) being evident in the majority of the glaciers. Glaciers are generally larger than in the NPI, and Glaciar Pio XI is the largest in South America (1265 km²) (Reference AniyaAniya and others, 1996).

The NPI and SPI have been shrinking dramatically ever since their LIA maxima, which are securely dated to AD 1870 (Reference Glasser, Harrison, Jansson, Anderson and CowleyGlasser and others, 2011), and are now shrinking at an increasing rate in response to regional climate change. Reference Rignot, Rivera and CasassaRignot and others (2003) estimated that the two icefields jointly contributed 0.042 ± 0.002 mm a^-1 to global mean sea-level rise in the period 1968/1975 to 2000 but that this doubled to 0.105 ± 0.011 mm a^-1 from 1995 to 2000. Reference Chen, Wilson, Tapley, Blankenship and IvinsChen and others (2007) estimated the ice loss rate for the Patagonia icefields from 2002 to 2006 to be 27.9 ± 11 km³ a^-1, equivalent to an average loss of ~1.6ma^-1 ice thickness change if evenly distributed over the entire glacier area and a global contribution to sea-level rise of +0.078±0.031 mma^-1. Reference Ivins, Watkins, Yuan, Dietrich, Casassa and RulkeIvins and others (2011) estimated ice loss rates for the NPI and SPI of 26±6Gta^-1 from 2003 to 2009, using a combination of data from the Gravity Recovery and Climate Experiment (GRACE) satellite and GPS bedrock uplift data. The background to these changes is presumed to be the global surface temperature increase of +0.6 ± 0.2°C in the 20th century (Reference Vaughan, Marshall, Connolley, King and MulvaneyVaughan and others, 2001), resulting in widespread glacier wastage and shrinkage (Reference AniyaAniya, 1988;Reference RamirezRamirez and others, 2001;Reference Arendt, Echelmeyer, Harrison, Lingle and ValentineArendt and others, 2002;Reference Meier, Dyurgerov and McCabeMeier and others, 2003;Reference Cook, Fox, Vaughan and FerrignoCook and others, 2005; WGMS, 2008).

Gran Campo Nevado (53° S) is an ice cap with several steep outlet glaciers (199 km²; Reference Schneider, Schnirch, Acuna, Casassa and KilianSchneider and others, 2007; Fig. 1), which may mean that it responds faster to climatic changes than the NPI or SPI (Reference Moller, Schneider and KilianMoller and others, 2007). It is at much lower altitudes than the NPI or SPI, with mountain summits from 1000 to 1700 m high, and with outlet glaciers reaching sea level. Mean annual temperatures here are +5.7°C, but the ice cap survives because of extremely high precipitation (Reference Moller and SchneiderMoller and Schneider, 2008).

Isla Riesco (52° S) is ~130 km long and 50 km wide, with moderate precipitation on its eastern part (<1000 mm a^-1), which is leeward of the Andes. The western part of the island is within the main belt of the Andes, with high precipitation rates (Fig. 1). The mountains reach 1830ma.s.l., with several small ice caps and mountain glaciers (Reference Casassa, Smith, Rivera, Araos, Schnirch and SchneiderCasassa and others, 2002). All these glaciers terminate on land, with the exception of a few small freshwater lakes.

Tierra del Fuego is an archipelago off southernmost South America (Fig. 1), with many small ice caps and mountain glaciers, as well as the Cordillera Darwin icefield. Cordillera Darwin is the most southerly icefield in the study region, at 54°30’ S, with topography constraining the ice masses (in comparison to the NPI and SPI, where ice-sheds separate the catchments (Reference Warren and AniyaWarren and Aniya, 1999)). The mountains reach 2469ma.s.l., and many of the glaciers calve into the ocean. The area receives more precipitation than does land to the east and north, and glaciers south of the ice divide receive far more precipitation than those north of the ice divide, as a result of the orographic rain shadow (Reference Holmlund Pand FuenzalidaHolmlund and Fuenzalida, 1995). The glaciers of Tierra del Fuego and Cordillera Darwin receive uniform precipitation throughout the year, and have an annual temperature range of ~7.4°C and a mean annual temperature of 1.2°C (Reference Sagredo and LowellSagredo and Lowell, 2012). The mass balance of Glaciar Martial Este, Tierra del Fuego, was negative (-772 mm w.e. a^-1) from 1960 to 2006 (Reference Buttstadt, Moller, Iturraspe and SchneiderButtstadt and others, 2009).

1.3. Regional climate

2.1. Data

Orthorectified (level 1G) Landsat Thematic Mapper (TM) images from 1985–87 and Landsat Enhanced TM Plus (ETM+) images from 2001–02 and 2010–11 were acquired pre-registered to Universal Transverse Mercator (UTM) World Geodetic System 1984 ellipsoidal elevation (WGS84), zone 18S projection (Appendix A). These images have a large swath (185 km) and reasonable spatial resolution (30 m), and a geopositional accuracy of better than ±50 m (Reference Tucker, Grant and DykstraTucker and others, 2004). The 2010–11 images have striping artefacts, caused by failure of the scan-line corrector (SLC) on the Landsat sensor in 2003.

For the NPI, additional data were obtained for 1975 from Reference AniyaAniya (1988). These data originate from 1974/75 vertical aerial photographs, which were used to create a map by the Instituto Geografico Militar, Chile, which was subsequently used in a glacier inventory by Reference AniyaAniya (1988).

Elevation data were derived from the Shuttle Radar Topography Mission (SRTM) digital elevation model (DEM) version 4.1 (hereafter SRTM4), at 3" resolution (90 m) (Reference Jarvis, Reuter, Nelson and GuevaraJarvis and others, 2008), providing elevation data from February 2000 (Appendix B). Vertical and horizontal errors are ~10 m (Reference FarrFarr and others, 2007). SRTM4 is a void-filled DEM, which may introduce inaccuracies in areas of steep topography (Reference Reuter, Nelson and JarvisReuter and others, 2007;Reference Frey and PaulFrey and Paul, 2012), but is suitable for use in glacier inventories (Reference Frey and PaulFrey and Paul, 2012). There is uncertainty in glacier elevation in our 2001 census as a result of differing times of image capture between the SRTM4 and Landsat data.

2.2. Glacier digitization for 1986, 2001 and 2011

Our methods follow GLIMS protocols, with each glacier between 41 ° S and 56° S (Fig. 1; Table 1) being manually digitized as a separate polygon (Reference Rau, Mauz, Vogt, Khalsa and RaupRau and others, 2005;Reference RaupRaup and others, 2007a,b;Reference PaulPaul and others, 2009;Reference Racoviteanu, Paul, Raup, Khalsa and ArmstrongRacoviteanu and others, 2009;Reference Svoboda and PaulSvoboda and Paul, 2009;Reference Raup and KhalsaRaup and Khalsa, 2010). We digitized glacier outlines in a GIS (ESRI ArcMap 9.3) at 1: 10 000 scale using cloud- and snow-free Landsat satellite images available from summer months in 1985/86, 2000/01 and 2010/11 (Appendix A). Using data from Reference AniyaAniya (1988), the extents of 38 outlet glaciers for the NPI were also digitized for 1975. Ice divides on the icefields were determined from previous publications (Reference AniyaAniya, 1996, 1999;Reference AniyaAniya and others, 1996;Reference Rignot, Rivera and CasassaRignot and others, 2003; Reference Bown and RiveraBown and Rivera, 2007;Reference Rivera, Benham, Casassa, Bamber and DowdeswellRivera and others, 2007;Reference Lopez, Chevallier, Favier, Pouyaud, Ordenes and OerlemansLopez and others, 2010), and downloaded from GLIMS where possible (e.g. Reference Schneider, Schnirch, Acuna, Casassa and KilianSchneider and others, 2007) to ensure consistency with other studies, or by using high points, nunataks, glaciological structures or breaks in slope (Reference Glasser and ScambosGlasser and Scambos, 2008;Reference Davies, Carrivick, Glasser, Hambrey and SmellieDavies and others, 2012;Table 1). All icefield outlet glaciers and ice caps and all mountain glaciers that could be clearly discriminated in the satellite images (as distinct from snow) and that were larger than 0.1 km² (because of image resolution and the danger of misclassification of snowpatches) were digitized in this study. Near the NPI, SPI, Cordillera Darwin and GCN, there are numerous small isolated glaciers with a ‘Mountain glacier’ classification, which have been considered separately (Northern Patagonian mountain glaciers (NPMG), Southern Patagonian mountain glaciers (SPMG), Cordillera Darwin mountain glaciers (CDMG) and Gran Campo Nevado mountain glaciers (GCMG)).

Table 1. Identification of glaciological and geomorphological features. After Reference Glasser, Jansson, Harrison and RiveraGlasser and others (2005, Reference Glasser and Scambos2008)

2.3. Geomorphological mapping to determine LIA extent

Glacier extent at the LIA was digitized for glaciers between 38°S and 56° S (Fig. 1) (Reference Glasser, Harrison, Jansson, Anderson and CowleyGlasser and others, 2011) for glaciers with clear trimlines and moraines. The LIA extent was inferred from geomorphological evidence, including trimlines and terminal moraines in front of contemporary glaciers (e.g. Fig. 2), which were identified according to previously defined criteria (Table 1). The inferred LIA glacier extents were checked against known LIA positions from published valley-scale dendrochronological and licheno- metric dating studies, for example for the Chilean Lake District (Reference Bown and RiveraBown and Rivera, 2007), NPI (Reference VillalbaVillalba, 1994; Reference Harrison and WinchesterHarrison and Winchester, 2000;Reference Winchester and HarrisonWinchester and Harrison, 2000;Reference Glasser, Hambrey and AniyaGlasser and others, 2002, 2004;Reference AranedaAraneda and others, 2007;Reference Harrison, Winchester and GlasserHarrison and others, 2007, 2012), SPI (Reference AniyaAniya, 1995, 1996;Reference Masiokas, Rivera, Espizua, Villalba, Delgado and AravenaMasiokas and others, 2009a,b;Reference Rivera, Koppes, Bravo and AravenaRivera and others, 2011), GCN (Reference Koch and KilianKoch and Kilian, 2005) and Cordillera Darwin (Reference Kuylenstierna, Rosqvist and HolmlundKuylenstierna and others, 1996;Reference Masiokas, Rivera, Espizua, Villalba, Delgado and AravenaMasiokas and others, 2009a). In situations where multiple trimlines or moraines exist, we drew the LIA limit at the trimline or moraine closest to the contemporary glacier snout (see Fig. 2 for examples from the NPI). At those glaciers where there is no visible evidence of shrinkage since the LIA or where the LIA limits are ambiguous or difficult to establish (e.g. for some fjord- terminating glaciers of the SPI), the limits are assumed to be the same as in 1975 or 1986 (the earliest possible data available). Our results are therefore minimum estimates of ice shrinkage over the time period ~AD 1870–2011.

2.4. Glacier attribute data

Attribute data for each glacier polygon include a unique Local ID (the same as that used in previous inventories, where appropriate), GLIMS ID (Reference Raup and KhalsaRaup and Khalsa, 2010), any established glacier name, X and Y coordinates of the centroid, surface area (km²), primary classification (Reference Rau, Mauz, Vogt, Khalsa and RaupRau and others, 2005), form, frontal characteristics, ID and acquisition date of the satellite image, analyst name and analysis time. For LIA polygons, any published evidence of LIA ice extent and associated references are also included. Glacier aspect (azimuth of the accumulation area;Reference EvansEvans, 2006) was estimated using vectors that follow the steepest part of the glacier accumulation area. Glacier length was measured for 520 glaciers according to standard procedures (Reference Lopez, Chevallier, Favier, Pouyaud, Ordenes and OerlemansLopez and others, 2010;Reference Davies, Carrivick, Glasser, Hambrey and SmellieDavies and others, 2012), following the longest flow pathway from the highest point on the ice divide to the glacier tongue (see Fig. 2). Minimum, maximum and median elevations and slopes for 2000 were derived automatically for each glacier in the GIS following analysis of SRTM4 (Reference PaulPaul and others, 2009;Reference Frey and PaulFrey and Paul, 2012).

2.5. Uncertainty

Digitized glacier lengths and outlines are accurate to ±30 m (i.e. ±1 pixel). Accuracy may be less in the centre of icefields, where ground control points are scarce, but as the same ice divides are used for each year inventoried, the uncertainty that this introduces into relative change measurement is limited. There may be inaccuracies where snow cover on nunataks in the centre of the icefields or adjacent to the ice edges has been misclassified as ice. We used qualitative methods to identify errors in glaciers with seasonal snow or large deviations in area between each year mapped, and manually improved these with additional Landsat images. Indeed, seasonal snow cover is not a significant problem in Patagonia because of the strong seasonality, and there is very little lying snow in the summer months near the glacier snouts. Where snow and ice is difficult to discriminate (e.g. on snow-capped mountains and volcanoes), glaciers have not been digitized.

Other potential sources of uncertainty include ice-divide and drainage basin identification, error in co-registration (Reference Granshaw and FountainGranshaw and Fountain, 2006), clouds and shadows, and delineation of debris-coved glaciers (Reference Bolch, Menounos and WheateBolch and others, 2010). However, this uncertainty was limited with manual digitization at resolutions up to 1: 10 000 (Table 1), which is more accurate than automatic classification (cf. Reference Jiskoot, Curran, Tessler and ShentonJiskoot and others, 2009), particularly when dealing with debris-covered glaciers (Reference PaulPaul, 2002). Automatic classification is particularly useful and suitable when analysing larger datasets comprising >1000 glaciers with clean ice. However, we acknowledge that delineating the boundary of debris-covered ice is very difficult with images of this resolution. A further source of error is the striping on Landsat ETM+ images taken after 2003, and it was necessary to interpolate across the stripes. This was mitigated by using numerous overlapping images, so that interpolating across large stripes near the margins of the image was not required.

Statistical quantification of errors is difficult without ground control points, high-resolution satellite images or ground-truthing in the week that the satellite image was taken (Reference Svoboda and PaulSvoboda and Paul, 2009). In order to quantify uncertainty, we conducted error analysis of the digitization of six NPI outlet glaciers in 1986 (i.e. the same glacier was independently digitized five times), both with and without debris cover and with grounded and floating termini (cf. Reference Stokes, Popovin, Aleynikov, Gurney and ShahgedanovaStokes and others, 2007). This yielded an average standard deviation of +0.3 km², or 2.0% of the area. Analysis of the area changes of glaciers is therefore considered to be accurate to within 2.0%. The glaciological uncertainty of ice divides is likely to be far larger than the mapping uncertainty, which has little influence on the final glacial outline, especially when comparing ice margin change from different years.

2.6. Analysis of glacier change

There are four kinds of data resulting from this study: glacier descriptors (area, length, primary classification, aspect, frontal characteristics, etc.), length changes (km a^-1; ma^-1), area changes (km²;%) and annual rates of change (% a^-1) (cf. Reference Bolch, Menounos and WheateBolch and others, 2010). We use ‘recession’ where length changes are discussed and ‘shrinkage’ for area changes. Annual rates of change were calculated by dividing the area change by the time between analyses for each glacier (time is taken from the date the satellite image was acquired). These are the only results that can be directly compared over different time periods and different glaciers, because of the different lengths of time between analyses (i.e. ~116 years from 1870 to 1986, ~15 years from 1986 to 2001, and ~10 years from 2001 to 2011, depending on when the satellite image for each glacier was acquired).

3.1. Characteristics of South American glaciers in 2011

In 2011, 626 glaciers were considered in our assessment, which included 386 major outlet glaciers from the main icefields (44 from the NPI, 161 from the SPI, 35 from GCN and 99 from Cordillera Darwin) (Table 2). These four principal icefields dominate the glacierized area (Fig. 3a). Glacier sizes in 2011 ranged from 0.1 to 1344 km² (SPI-137; Pio XI) (Table 2). Although there are many small glaciers, a few large glaciers made up the majority of the glacierized area (Fig. 3a). The mountain ranges beneath the SPI, NPI, GCN and El Volcan are orientated north-south, resulting in a predominantly west-east aspect for the outlet glaciers (Fig. 3b).

Fig. 3. (a) Glacierized area in 2011 and number of glaciers in each size class. (b) Glacier aspect for the main regions. (c) Number of glaciers in each ‘Primary Classification’ (from GLIMS protocols). (d) Numbers of glaciers in each category of the ‘Form’ attribute (from GLIMS protocols). (e) Mean altitude for glaciers across the study region. (f) Comparison between glacier area in 2001 and glacier maximum altitude, with regression line. Note logarithmic scale. (g) Relationship between glacier latitude and median altitude. (h) Relationship between glacier length and mean slope. Note logarithmic scale.

Table 2. Summary of the glacier inventory, divided into regions. Regions are ordered north to south. Location in decimal degrees

In the study region there were 233 outlet, 95 valley and 229 mountain glaciers, 26 ice caps and 38 icefields, with outlet glaciers dominating the glacierized area. Although mountain glaciers are numerous, they made up only a small proportion of the glacierized area (8.3%; Fig. 3c). Many of the valley or outlet glaciers have a compound basin (numerous cirques or catchment areas) or compound basins, where two compound basin drainage systems merge (Fig. 3d;Reference Rau, Mauz, Vogt, Khalsa and RaupRau and others, 2005). The majority (526) of the glaciers surveyed terminate on land, although 100 have calving termini (35 marine and 65 lacustrine).

Mean glacier elevation ranged from 496 m a.s.l. (IH-14) to 2182ma.s.l. (MSL-5) (Table 2). NPI-1 had the highest maximum elevation (3968 m a.s.l.). Overall, 41% of the glaciers had a median altitude of 1000–1500 m a.s.l., with only one glacier having a median altitude of 0–500 m or >2000 m (Fig. 3e). There was a weak relationship (r² = 0.2) between maximum altitude and glacier area in 2001 (Fig. 3f), and there was a trend towards decreasing glacier median altitudes southwards (Fig. 3g;Table 2). There was a large scatter in glacier altitude, with large outlet glaciers from the icefields having a wide range of median altitudes. Glacier slope varied with glacier length (r² = 0.3;Fig. 3h), which is important, as shorter, steeper glaciers typically have the fastest response times (Reference Raper and BraithwaiteRaper and Braithwaite, 2009). Regionally, the steepest glaciers were found in Parque Nacional Vicente Perez Rosales, and the lowest mean slopes were found in the NPI and SPI (Table 2).

The NPI (4365 km²) was 120km long, 70km at its widest, and extended from 46°30′ S to 47°30′ S (Fig. 2). It had a mean altitude of 1340 m a.s.l. We analysed 44 outlet glaciers of the NPI covering 3976km², and 59 isolated nearby glaciers (in NPMG, Cordon La Parvas and Cordillera Lago General Carrera), covering 389km². These mountainous regions generally had glaciers with high mean slopes and altitudes (Table 2). Nineteen of the outlet glaciers had calving termini, of which only one (Glaciar San Rafael) was marine-terminating. Glaciers west of the ice divide made up the majority of the glacierized area of the NPI (Table 3; Fig. 4a). The more southerly glaciers of El Volcan (Fig. 1;Table 2) were primarily small ice caps and mountain glaciers with a mean altitude of 1521 m a.s.l., and all were land-terminating, though some had small lakes in their forefields.

Fig. 4. (a) Glacierized area and rates of area loss for the NPI and SPI, with calving and land-terminating glaciers shown separately. (b) Rate of change 2001–11 against latitude, with glaciers divided into size classes. (c) Rate of glacier shrinkage 2001–11 against glacier mean altitude, with glaciers divided into size classes. (d) Rate of glacier shrinkage 2001–11 against glacier mean slope, with glaciers divided into size classes. (e) Rate of change for each region over three time periods. For Lago del Desierto (LDP) and Southern Patagonian mountain glaciers (starred), the anomalously high shrinkage rates are given in the figure. See Table 2 for abbreviations.

Table 3. Glacier change for the NPI and SPI

The SPI was the largest icefield (13 219 km²), and stretched north-south for 400 km, from 48° S to 52° S along the southern Andes, with widths of 30–70 km and a mean altitude of 1191 m a.s.l. In our assessment, it was drained by 154 outlet and simple basin glaciers with 45 nearby isolated glaciers (in SPMG, Lago del Desierto, Cerro Paine Grande and Torres del Paine) covering 278 km². Its area was again dominated by glaciers west of the ice divide (Table 3), but with several large outlet glaciers draining eastwards. Of the outlet glaciers, 54 had calving termini, and they accounted for 10 945 km², or 83% of the total area (Fig. 4a).

GCN (52°40’-52°55’S) was the smallest ice cap (262 km²), with 35 glaciers (of which 4 calved into lakes), and was 24 km long and 16 km wide. It was surrounded by 17 small mountain glaciers and ice caps. Cordillera Darwin (1931km²) was the southernmost icefield (54°30⁰ S) and was 90 km long and 30 km wide. There were 99 glaciers, of which 66 were outlet glaciers (covering 408 km²). Ten of these had calving termini. There were 18 small isolated glaciers nearby, including 7 valley glaciers, and there were 6 small icefields and ice caps nearby.

3.2. Changes in glacier length and area from 1870 to 2011

3.2.1. General trends

A total of 640 glaciers were digitized from 1870 from 40° S to 56° S (Figs 4–6;Table 4). Of these, 626 remained in 1986. Overall, 90.2% of the glaciers shrank between 1870 and 2011, 0.3% advanced and 9.5% showed no change. Despite some small advances, which are generally short-term and limited to tidewater glaciers, all regions have suffered extensive glacier surface area loss. For the SPI and eastern NPI, the greatest rates of shrinkage were observed in land- terminating glaciers (Fig. 4a). Glacier shrinkage from 2001 to 2011 was greatest in glaciers less than 5 km² in size, while those greater than 100 km² had particularly slow rates of shrinkage (Fig. 4b). Rates of shrinkage were highest in the most northerly glaciers, with most glaciers shrinking. Latitudinal gradients are also emphasized, with nearly all glaciers from 41°S to 44°S shrinking, small glaciers from 44° S to 53° S also shrinking, and with little shrinkage in glaciers from 54° S to 56° S (Fig. 4b). Mean glacier altitude and slope (Fig. 4c and d) had little control on glacier shrinkage in Patagonia.

Fig. 5. Rate of annual change (%a¹) for 2001–11 against 2011 glacier size for each region. SPMG refers to isolated glaciers surrounding the SPI. ‘National parks’ includes Parque Nacional Vicente Perez Rosales, Parque Nacional Corcovado and Parque Nacional Queulat. Grey circles denote calving glaciers; black squares denote land-terminating glaciers. Solid horizontal line is nil change; shrinkage is below this line, and advance is above. Latitude of regional centre is shown.

Fig. 6. Graphs showing cumulative length changes for selected glaciers for key icefields. The black line indicates a glacier that terminates on land. The grey line with short dashes indicates lacustrine-terminating glaciers. The thick black dashed line indicates marine-terminating (tidewater) glaciers. (a) Cerro Erasmo; (b) the NPI; (c) El Volca´n; (d) the SPI; (e) GCN; and (f) Cordillera Darwin.

Table 4. Area change, percentage change and annual rates of change in each region and time period. N refers to the number of glaciers shrinking fastest in this period. For region codes see Table 2

Annualized rates of shrinkage across South America increased for each time period measured (Table 4; Fig. 4e), with overall rates of shrinkage twice as rapid for 2001 11 as for 1870–1986 (0.10% a^-1 for 1870–1986, 0.14% a^-1 for 1986–2001 and 0.22%a^-1 for 2001–11). Across the study area, percentage change per annum was greatest for 18701986 for 212 glaciers, for 1986–2001 for 172 glaciers and for 2001–11 for 155 glaciers. Across the study region, 14 glaciers extant during the LIA had disappeared entirely by 1986, mostly around the SPI.

3.2.3. Northern Patagonia Icefield (NPI)

Almost all glaciers (98.1%) in the NPI shrank between 1870 and 2011. Length fluctuations were measured for 38 NPI glaciers, and showed a general trend of increasing recession (Fig. 6b). Several glaciers were stable from 1986 to 2001, but receded from 2001 to 2011 (e.g. NPI-21 (Pared Norte; 112 m a^-1), NPI-20 (Pared Sur;189ma^-1) and NPI-2 (112 ma^-1)). Still others receded at steadily increasing rates (e.g. NPI-10 (Strindberg) and NPI-14). NPI-7 (San Rafael; lagoonal) receded by 9.6 km (83 m a^-1) between 1870 and 1986, and by a further 1.2 km by 1990, whereupon the margin stabilized.

The highest rates of shrinkage east of the NPI ice divide were for land-terminating glaciers. West of the ice divide, the highest rates of shrinkage were observed in calving glaciers, which also occupy a larger area (Fig. 4a). The large areal losses of the NPI from 1870 to 2011 were dominated by a small number of large glaciers. These include NPI-7 (San Rafael;11.5%), NPI-8 (San Quintin;14.6%) and NPI-25 (Colonia;12.9%) (Fig. 2). Glaciers east of the ice divide shrank by 2.2% from 2001 to 2011 (Table 3), compared with 2.4% for glaciers to the west. Four glaciers had small, shortterm advances (NPI-14 from 1975 to 1986;NPI-32 from 1986 to 2001; NPI-18 and NPI-86 from 2001 to 2011).

Overall, annual rates of area loss for 2001–11 (0.23% a^-1) were twice as high as those for 1870–1986 (0.09% a^-1) (Fig. 4e), with similar rates both west and east of the ice divide (Table 3). However, more glaciers shrank fastest from 1975 to 1986 than from 2001 to 2011 (Table 4). The rapid 2001–11 areal shrinkage of NPI-1 (Grosse;1.69%a^-1), NPI-6 (Gualas;0.97%a^-1), NPI-16 (HPN-4;0.26%a^-1) and NPI-25 (Colonia;0.15%a^-1) dominates the trend observed in Figure 4e, but in general, the small glaciers fringing the icefield shrank fastest (Figs 4, 5 and 6a). The period of most rapid shrinkage of the other glaciers varies, from 1870–1986 (e.g. NPI-7 (San Rafael;0.09%a^-1)) to 1975–86 (e.g. NPI-8 (San Quintin;0.23%a^-1)) to 1986–2001 (e.g. NPI-14 (0.23%a^-1), NPI-12 (Benito;0.33%a^-1) and NPI-5 (Reicher; 0.77% a^-1)) (Figs 2b and c and 7a). It is also clear from the scatter plots in Figure 5 that calving glaciers are currently shrinking less rapidly (as a percentage of their area per annum) than land-terminating glaciers. Indeed, Figure 4a shows that land-terminating glaciers have relative rates of area loss much higher than calving glaciers, both east and west of the ice divide, with land-terminating glaciers east of the ice divide shrinking at 0.27%a^-1 from 2001 to 2011, compared with 0.11%a^-1 for calving glaciers. However, it should be noted that these large calving glaciers have lost the most area in absolute terms and are still shrinking rapidly.

Fig. 7. Map of key icefields showing overall glacier shrinkage, 1870–2011. Glacier extent in 1870 is shown in white. Lakes larger than 15km² are also shown.

3.2.4. Southern Patagonia Icefield (SPI)

For the SPI, 96.5% of the glaciers shrank between 1870 and 2011, with the majority (59 of 154) shrinking fastest from 2001 to 2011. The length fluctuations of 157 glaciers show large but variable linear recession from their LIA maxima (e.g. SPI-14 (O’Higgins;16.0km by 2011;lacustrine) and SPI-1 (Jorge Montt;10.0km by 2001 followed by a small 2001 11 advance of 0.5 km)). Several large glaciers shrank particularly fast between 2001 and 2011 (e.g. SPI-142 (Occidental;216ma^-1), SPI-179 (76 m a^-1) and SPI-22 (157 m a^-1)) (Fig. 6d).

The largest relative area changes (1870–2011) were generally from the smaller outlet glaciers, such as SPI-26 (82.4%), SPI-177 (85.8%) and SPI-169 (93.2%). The larger outlet glaciers have also lost surface area from 1870 to 2011 (e.g. from SPI-1 (Jorge Montt; 12.6%), SPI-14 (O’Higgins; 10.9%), SPI-31 (Upsala;19.7%) and SPI-142 (Occidental; 11.5%)). Three glaciers advanced from 1986 to 2001 (SPI- 137 (2.1 km²), SPI-198 (2.4 km²) and SPI-77 (0.3 km²)) and three from 2001 to 2011 (SPI-113 (4.9 km²), SPI-109 (0.6 km²) and SPI-45 (4.9 km²));in the case of SPI-113, the advance from 2001 to 2011 was beyond 1870 limits. However, it is difficult to determine the 1870 limit for fjordtype glaciers without moraines (e.g. SPI-113).

Overall, annual rates of shrinkage for the SPI were more than twice as rapid for 2001–11 (0.15% a^-1) as for 18701986 (0.07% a^-1; Fig. 4e), but this result is again dominated by a small number of outlet glaciers (Figs 5 and 6b), particularly those south of the main icefield, such as SPI-70 (1.22% a^-1), SPI-149 (6.37%a^-1) and SPI-199 (1.95%a^-1) (Figs 6 and 7b). Although some calving outlet glaciers are shrinking rapidly (e.g. SPI-141 (0.22%a^-1), SPI-145 (1.02%a^-1) and SPI-31 (Upsala;19.7%a^-1)), in general, small, land-terminating glaciers are experiencing the highest annual rates of shrinkage (Figs 5 and 6). Across the SPI, glaciers on the east of the ice divide had slightly higher annual rates of shrinkage (Table 3), with land-terminating glaciers shrinking at rates of 0.29% a^-1 from 2001 to 2011, compared with 0.08% a^-1 for calving glaciers west of the ice divide (Fig. 4a). Figure 7b illustrates the highly variable but rapid area loss in small glaciers around the fringes of the SPI, with particular large glaciers also losing surface area. Rates of area loss are increasing around the SPI, with most glaciers experiencing their highest rates of area loss from 2001 to 2011 (Fig. 8b;Table 4). For most of the remaining glaciers, the period of fastest area loss was 1986–2001.

Fig. 8. Map of key icefields, illustrating period of fastest shrinkage. Glaciers in dark purple shrank fastest between 2001 and 2011, light purple between 1986 and 2001, bright green between 1975 and 1986, and light green between 1870 and 1986. Glaciers in red advanced and glaciers in orange did not change. Glacier outlines are from 2011. Lakes larger than 15 km² are also shown.

4.1. Comparison with previous inventories

Our calculated area for the NPI of 3976km² in 2011 and 4070km² in 2001 is similar to the previous estimate of a total ice area of 3953 km² in 2001 made by Reference Rivera, Benham, Casassa, Bamber and DowdeswellRivera and others (2007). Our calculated area for the contemporary SPI of 13 219 km² in 2011 also fits with the previous estimate for this icefield of 13 000 km² (Reference AniyaAniya, 1999). For GCN, our calculated area of 243 km² in 2001 fits well with the calculated area of Reference Schneider, Schnirch, Acuna, Casassa and KilianSchneider and others (2007) of 252.6 km² in 2002. Differences may be because we included more of the surrounding glaciers in our study.

Our data lend independent support to the assertion of Reference Rignot, Rivera and CasassaRignot and others (2003) and Reference Glasser, Harrison, Jansson, Anderson and CowleyGlasser and others (2011) that the Patagonian icefields are shrinking at an increasing rate. Our calculated rates of area loss from the NPI suggest that there was an increase in annual area loss rates from 0.09%a^-1 in the 116 years between AD 1870 and 1986, to 0.12%a^-1 in the 15 years between 1986 and 2001, to 0.23% a^-1 from 2001 to 2011 (Table 4).

4.2. Calving dynamics and asynchronous glacier change

The acceleration in relative rates of area loss for the NPI from 2001 to 2011 was dominated by the smaller land-terminating glaciers (Figs 4e and 5). The shrinkage of marine- and lacustrine-terminating glaciers is highly variable, and reflects a dynamic and nonlinear response to multiple factors. For example, NPI-1, NPI-6, NPI-16 and NPI-25 terminate in freshwater lakes, and had particularly rapid rates of area loss. NPI-1, however, ablates not by calving but by rapid thinning and surface melting, with large supragla- cial ponds (personal communication from M. Aniya, 2012). The fragmented snout of NPI-16 is difficult to define, which may induce an error in assessing the shrinkage. Supraglacial debris cover insulates the glacier from solar radiation and so affects ablation rates (Reference Scherler, Bookhagen and StreckerScherler and others, 2011). For example, slow shrinkage of NPI-1 (Glaciar Grosse) prior to was attributed to insulation by thick debris cover (Reference AniyaAniya, 2001). The floating terminus of NPI-6 (Glaciar Gualas) advanced from 1996 to 1999, possibly as a result of stretching (Reference AniyaAniya, 2001). This stretching was followed by more rapid shrinkage from 2001 to 2011, driven by rapid calving induced by large, deep, water-filled crevasses.

NPI-7 (Glaciar San Rafael), NPI-8 (Glaciar San Quintin) and NPI-5 (Glaciar Reicher) (Figs 2, 7 and 8) shrank most rapidly from 1870 to 1986, 1986 to 2001 and 1986 to 2001 respectively. These lacustrine-terminating glaciers are the largest of the NPI and have widely different accumulation area ratios. They have shown repeated stillstands, advances and retreats since the 1920s (Reference Winchester and HarrisonWinchester and Harrison, 1996;Reference AniyaAniya, 2007, Reference AranedaAraneda and others, 2007;Reference Lopez, Chevallier, Favier, Pouyaud, Ordenes and OerlemansLopez and others, 2010). Glaciar San Rafael currently has a high velocity and is thinning extensively (Reference Willis, Melkonian, Pritchard and RamageWillis and others, 2011). Steady thinning of the glacier surface could induce periodic flotation and rapid retreat, followed by grounding and stabilization (Reference AniyaAniya, 2007). An advance reported from 1992 to 1999 for Glaciar San Rafael (Reference AniyaAniya, 2001) explains the reduced area loss rates observed from 1986 to 2001. Glaciar San Quintin terminated on land until 1991, when shrinkage led to the formation of a lake in the former glacier basin, into which it now calves (Reference Rivera, Benham, Casassa, Bamber and DowdeswellRivera and others 2007; Reference Willis, Melkonian, Pritchard and RamageWillis and others, 2011). Large-scale shrinkage was observed in Glaciar Reicher from 1996 to 1999 (Reference AniyaAniya, 2001), before the glacier appeared to reach a new equilibrium. NPI-12 (Glaciar Benito) and NPI-13 (HPN-1) are both thinning rapidly and accelerated in speed between 2007 and 2011 (Reference Willis, Melkonian, Pritchard and RamageWillis and others, 2011). Neither glacier has shown significant shrinkage in this period.

For the SPI, the acceleration of shrinkage post-2001 is dominated by smaller fringing glaciers (Figs 4e, 5, 7b and 8b). However, the majority of the large outlet glaciers draining the SPI calve into freshwater lakes or fjords, with highly variable behaviour in each catchment basin (Reference AniyaAniya, 1995; Fig. 8d). Dynamical changes in the calving glaciers of the SPI are discussed below.

SPI-31 (Glaciar Upsala) calves into a lake on the eastern SPI and shrank at 0.2% a^-1 from 2001 to 2011. Previous studies observed thinning (33 m between 1990 and 1993; Reference Naruse and SkvarcaNaruse and Skvarca, 2000) and rapid area loss, and argued that this was caused by variations in bed topography, with bedrock rises in the lake controlling frontal fluctuations (Reference Naruse and Skvarca Pand TakeuchiNaruse and others, 1997;Reference Naruse and SkvarcaNaruse and Skvarca, 2000). SPI- 137 (Pio XI) is currently shrinking at a rate of 0.04% a^-1. From 1986 to 2001, Pio XI advanced at a rate of 0.01% a^-1, with a documented advance of up to 10 km from 1945 to 1986 (Reference Rivera and CasassaRivera and Casassa, 1999), with thickening by an average of 44.1 m from 1975 to 1995.

SPI-16 (Glaciar Chico) is shrinking slower than many of the other large tidewater glaciers of the SPI (at 0.18% a^-1), which has been attributed to limited calving activity (Reference Rivera, Casassa, Bamber and KaabRivera and others, 2005). However, this glacier is thinning at rates comparable to other glaciers of the SPI, and the rate of area loss has accelerated in each successive period. SPI-14 (Glaciar O’Higgins) shrank most rapidly from 1870 to 1986 (0.09%a^-1), followed by slower shrinkage from 1986 to 2001 (0.02% a^-1) and from 2001 to 2011 (0.01% a^-1). This is largely due to a rapid retreat of 4.7 km from 1973 to 1976 (Reference Lopez, Chevallier, Favier, Pouyaud, Ordenes and OerlemansLopez and others, 2010).

SPI-48 (Glaciar Perito Moreno), on the eastern side of the ice divide, calves into Lago Argentino (cf. Fig. 8b), with only limited area loss (0.1%) after 2001. This glacier is well known for periodic advances and retreats, related to the geometry of its calving front. The glacier periodically advances to Peninsula Magallanes, whereupon it dams the lake. Rising lake levels lead to increased pressure and eventual ice-dam and lake-drainage events through the ice front (Reference Stuefer, Rott and SkvarcaStuefer and others, 2007).

Therefore, across the NPI and SPI, atmospheric temperature changes have led to thinning, resulting in calving glaciers reaching flotation point and becoming unstable (cf. Reference Rivera and CasassaRivera and Casassa, 2004). Stretching may cause short-lived advances, but encourages thinning and enhanced calving, resulting eventually in retreat. Accelerated retreat may occur after shrinkage from a pinning point (Reference Holmlund Pand FuenzalidaHolmlund and Fuenza-lida, 1995;Reference Warren and AniyaWarren and Aniya, 1999). Alternatively, a marine shoal may reduce water depths and encourage advance. The formation of a proglacial lake may accelerate glacier shrinkage, but if the glacier retreats beyond the lake margin, shrinkage may slow down. Therefore glacier shrinkage in calving glaciers is regulated by individual dynamics (calving status, ELA, channel geometry (Reference Aniya, Sato, Naruse and Skvarca Pand CasassaAniya and others, 1997)), with retreating, advancing and stable termini observed.

4.3. Temporal and regional variations

From Figures 4 and 5, it is clear that latitude, size and terminal environment exert the greatest controls on glacier shrinkage, with the more northerly, smaller, land-terminating glaciers shrinking fastest. Calving glaciers are changing in area (relative rates of area loss) more slowly than small land- terminating glaciers, with internal calving dynamics controlling tidewater termini (Fig. 4a). The spikes in SPMG and Lago del Desierto are caused by a small number of very rapidly shrinking glaciers, such as EC-1, SPMG-15 and SPMG-5. Worldwide, small glaciers and ice caps have reacted particularly dynamically to increased global temperatures (Reference Oerlemans and FortuinOerlemans and Fortuin, 1992;Reference Hock, De Woul and RadicHock and others, 2009), and it has been proposed that the volume loss from mountain glaciers and ice caps like these is the main contributor to recent global sea-level rise (Reference Church and HoughtonChurch and others, 2001; Reference Braithwaite and RaperBraithwaite and Raper, 2002;Reference MeierMeier and others, 2007;Reference Hock, De Woul and RadicHock and others, 2009). On a regional scale, both the large icefields and small ice caps and glaciers north of 52° S have suffered accelerated shrinkage from 2001 to 2011 (Fig. 4e), presumably driven by the observed increases in upper- tropospheric air temperatures since 1976, particularly at Puerto Montt (Reference Giese, Urizar and FuckarGiese and others, 2002; Reference VillalbaVillalba and others, 2003;Reference Bown and RiveraBown and Rivera, 2007;Reference Carrasco, Osorio and CasassaCarrasco and others, 2008; Reference Aravena and LuckmanAravena and Luckman, 2009;Reference Rivera, Bown, Carrion and ZentenoRivera and others, 2012). Glacierized summits in the Chilean Lake District lie within this altitudinal zone, so this warming is likely to be a significant control on the mass balance of ice caps and glaciers between 41°S and 46° S in the far north of the study region, resulting in rapid shrinkage (i.e. Parque Nacional Vicente Rosales, Hornopiren, Parque Nacional Corcovado and Parque Nacional Queulat).

There is a very slight east-west gradient in annual rates of area loss for the NPI and SPI (Table 3), in particular for the period 1870–1986, with the eastern glaciers shrinking fastest. This is illustrated further in Figure 6, where smaller glaciers on the east of the NPI and the nearby glaciers exhibit the highest rates of relative shrinkage. We do not find strong evidence for shrinkage gradients in the outlet glaciers after 1986; this contrasts with other studies, where it has been argued that changes in precipitation are driving the accelerated shrinkage east of the ice divide (Reference Aravena and LuckmanAravena and Luckman, 2009). However, it should be noted that absolute rates of area loss (km² a^-1) are higher on the west of the ice divide, due to the larger glacierized area here. Reference Harrison and WinchesterHarrison and Winchester (2000) also found little evidence of clear east- west gradients or patterns of behaviour for the NPI. It is possible that declining precipitation drove increased relative shrinkage rates east of the ice divide for the period 18701986, but after this period more uniform shrinkage would suggest that they are more likely shrinking in response to thinning (cf. Reference Rignot, Rivera and CasassaRignot and others, 2003). Reference Barcaza, Aniya, Matsumoto and AokiBarcaza and others (2009) attribute faster absolute shrinkage (km² a^-1) on western glaciers to high transient snowlines and increased ablation areas; however, this does not take into account glacier size, so results are not comparable.

Mountain glaciers and ice caps between 52° S and 54° S, including GCN and Isla Riesco, had relatively similar rates of area loss from 1986 to 2011 (Figs 4e and 6). The observed shrinkage is in keeping with thinning observed on outlet glaciers (Reference Moller, Schneider and KilianMoller and others, 2007). Mountain glaciers south of 54° S and the Cordillera Darwin, Isla Hoste, Tierra del Fuego and Monte Sarmiento ice caps have had respectively less change since the LIA, which agrees with the findings of other studies (e.g. Reference Kuylenstierna, Rosqvist and HolmlundKuylenstierna and others, 1996). These glaciers shrank fastest from 1986 to 2001 (Fig. 4e), during a period of rapid warming south of 46° S (Reference VillalbaVillalba and others, 2003).