Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ). 1 − , 3 , 1 0.36 m w.e. yr ± C in this region since ◦ 0.64 , A. Julián − 3 0.4 m, ± , C. Azorín-Molina 1 1 ). This loss of glacial ice has continued 1 , J. Chueca-Cía − 2 5022 5021 ) compared to 1981 to 1999 (the ice depth de- 1 − , I. Rico 1 0.1 m w.e. yr ± , S. M. Vicente-Serrano 0.39 5 − , and J. M. García-Ruiz 0.14 m w.e. yr 1 , J. Revuelto ± 1 2.12 m, 0.72 − ± , E. Serrano 4 1.8 m, ± This discussion paper is/has beenPlease under refer review to for the the corresponding journal final The paper Cryosphere in (TC). TC if available. Dept. Geoenvironmental Processes and Global Change, Pyrenean Institute of Ecology, University of the Basque Country, Department of Geography, Prehistory andDept. Archeology, Geography, University of Zaragoza, Zaragoza,Dept. Spain Graphic Design and Engineering,Dep. University Geography, University of of Zaragoza, Valladolid, Huesca, Valladolid, Spain Spain from 2011 to 2014 (the ice depth decreased 2.1 the end of the Littleically Ice during Age years (LIA) with inseason, low the accumulation but mid-1800s. or cannot Thus, high recover thistures air glacier during during temperatures shrinks the years during ablation dramat- with season. theThese The high ablation most data accumulation recent indicated TLS or that data lowsummers support two (2012–13 this air consecutive interpretation. and markedly tempera- 2013–14) anomalous lednificant wet to losses winters near and of zero cool ice massthe balance in dramatic conditions, shrinkage some with that areas. sig- occurred These during the anomalous dry periods and could warm not period of counteract 2011–2012. Local climatic changeswastage during rate the of studycreased this slightly, and glacier, period local air because cannot temperature duringincrease. local the explain The ablation precipitation accelerated period the did degradation and not of acceleration significantly by snow this the in glacier accumulation lack in in- recent ofparticular, years equilibrium the can average between be air explained the temperature glacier increased by and at the least current 0.9 climatic conditions. In Abstract This paper analyzes the evolution ofof the the Monte Pyrenees, Perdido Glacier, from the 1981surface third area largest to glacier by the use present. of Weice aerial assessed volume photographs the by from evolution geodetic 1981, of 1999, methodstopographic the and with maps 2006, glacier’s digital (1981 and elevation and changes models 1999),ning in (DEMs) airborne (TLS, generated LIDAR 2011, from (2010) and 2012,based terrestrial 2013, on laser and climate scan- 2014). dataaccelerated We from degradation interpreted a of nearby the thiswas meteorological glacier changes after almost station. in 2000, The the three-times with resultsdoubling glacier greater a indicate of rate from an the of 2000 rate8.98 ice of to surface ice loss 2006 volume that creased than loss 8.35 for from 1999 earlier to periods, 2010 and (the a ice depth decreased Accelerated wastage of the MonteGlacier Perdido in the Spanish Pyreneesrecent during stationary climatic conditions J. I. López-Moreno The Cryosphere Discuss., 9, 5021–5051,www.the-cryosphere-discuss.net/9/5021/2015/ 2015 doi:10.5194/tcd-9-5021-2015 © Author(s) 2015. CC Attribution 3.0 License. A. Serreta E. Alonso-González 1 CSIC, Campus de Aula2 Dei, P.O. Box 13.034, 50080 Zaragoza, Spain Vitoria, Spain 3 4 5 Received: 10 August 2015 – Accepted: 2Correspondence September to: 2015 J. – I. Published: López-Moreno 29 ([email protected]) SeptemberPublished 2015 by Copernicus Publications on behalf of the European Geosciences Union. 5 25 20 15 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ). 1 − cult, because ffi 0.25 mw.e.yr − from 1997 to 2006. 1 − ) that clearly exceed the 1 − between 1951 and 2010 (Deaux et al., 1 0.65 mw.e.yr − − 5024 5023 C decade ◦ from 1969 to 1997 and 0.9 %yr ) was about twice that for the period of 1933 to 1959. 1 1 − − 255 m increase in the elevation of the ELA in the glaciers ∼ 0.12 mw.e.yr ± C since the end of the LIA (Dessens and Bücher, 1998; Feulliet and Mercier, ◦ 0.69 erent massifs have had variable reductions in area covered by ice, with a 59% − ff Most studies agree that global warming is responsible for the observed glacier Glaciers are very good indicators of climate change due to their high sensitivity to The southern-most glaciers of Europe are in the Pyrenees, and they have also under- shrinkage and the recent accelerationbeen of this particularly shrinkage. strong The temperature sincemountain increase the has ranges end of ofNogués-Bravo the the et world LIA, al., (Haeberli 2008; andequilibrium and Gardent also line et since Beniston, altitudes al., the (ELAs) 1998; 2014). andof 1970s Beniston glaciers, reduced Global in so et the warming most that accumulation al., has most ablation(Mernild increased 2003; glaciers ratios et al., the are (AARs) 2013). not In in theleast equilibrium case 0.9 of with the current Pyrenees, climatic the2012), conditions air showing temperature an has increase increased of at 0.2 anomalies in precipitation andet al., air 2015). However, temperature establishing a (Carrivickclimate direct and and relationship between the Brewer, annual changes 2004; fluctuationsonly in of Fischer glaciers area of and medium mass of or a small particular size glacier respond is rapidly di to changes in annual snowfall reduction in the Vignemale Massifsif and (Gellatly an et 84% al., reductionPyrenees 1995; in René, from the 2013). Posets-Llardana 1880 A Mas- toThere total has of 2005, been 111 and a glaciers rapid onlyface have glacial imminent disappeared 31 recession extinction. in since actual Chueca the the et glaciersshrinkage 1990s, during al. and (with the (2005, many last ice 2008) of two decades motion) reportedcentury these of glaciers that were remain. the 20th the similar century rates to andof of those the the glacial beginning observed LIA. of from the A 1860 21st similarGlacier to conclusion (French 1900, Pyrenees). has immediately been reached after by the Marti end et al. (2015) for the Ossue 2014). This explains the of the Maladeta Massif, whichThe is decreased currently accumulation close of toablation snow, 2950 season and ma.s.l. are the (Chueca thought increase et tosouthern in al., be (Spanish) air 2005). side the temperature of principal during the causes Pyrenees the of (Chueca recent et glacier al., decline 2005). in the 1 Introduction Most glaciers worldwideIce have Age undergone (LIA) intense inarea retreat the and since mid volume the 19th (VincentZemp end century, et et of as al., al., indicated the 2013; 2014).(Serrano by Little Marshall, et This measurements 2014; al., trend 2011; of Marzeion Mernild has iceLópez-Moreno et et apparently surface et al., al., accelerated 2013; al., 2014, Carturan in 2014). 2015; etloss Thus, the al., Marshall of 2013a; last (2014) global Gardent three and et glacierdecade decades al., Zemp mass 2014; studied. et during Several al. studies the (2015) examinedAlps, early noted this glacier that 21st phenomenon shrinkage has century in accelerated Europe. exceededet since In that al., the the 2014). 1960s, of French mainly In any in theglacier other the Ötzal area 2000s Alps (Gardent was (Austria), 0.4 Abermann %year et al. (2009) calculated the loss of values presented by Huss etIn al. (2010) the for Sierra the Nevada 20thduring of century the (close southern LIA, to disappeared Spain, as the aa white Veleta glacier-derived glacier Glacier, rock during which the glacier was mid(Gómez-Ortiz with 20th reconstructed et century a al., and marked 2014). became degradation during the last twogone significant decades deglaciation. In 2005, theseTrueba et glaciers al., had 2008) an and area in ofthe 2008 495 di ha they (González- had an area of 321 ha (René, 2013). Since 1880, In the Central Italian Alps,1990–2007 Scotti and et reported al. (2014) anof compared approximately glacier the area 10-fold period during greater of theItalian 1860–1990 average more Alps with annual recent and decrease period. found Carturan2010 that et the ( al. average (2013b) rate also of studied ice the mass loss during the period 1980– Over the samerate period of (1980–2010), ice Fischer mass et loss al. for (2015) the calculated Swiss a Alps very ( similar 5 5 15 10 25 20 10 20 25 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 0.36 and − 5026 5025 s, the Cinca River flows directly from the glacier s of 500–800 m in height (García-Ruiz and Martí- ff ff ). 2 erent glaciers in the same region (Reinwarth and Escher-Vetter, ff ect on the development of ice bodies, and can cause notable varia- , respectively. ff 1 − Researchers have studied glaciers in the Marboré Cirque since the mid 19th century This paper focuses in the recent evolution of the Monte Perdido Glacier, the third 0.39 mw.e.yr (Schrader, 1874), and manytics next of studies ice examined masses the andde extent the Llarena, and features 1936; other of characteris- Hernández-Pacheco thecent moraines and studies deposited Vidal have during established Box, theextent the LIA 1946; of (Gómez location Boyé, LIA of 1952). glaciersGarcía moraines More (Nicolás, Ruiz to re- 1981, and deduce 1986; Martí theronmental Martínez changes dynamics Bono, during de and 2002; the Pisón Martín Holocene and through Moreno, Arenillas, study 2004) of 1988; and sediments have in Marboré analyzed Lake envi- and the surrounding slopes, andMarboré has Cirque created (5.8 a km longitudinal west–east basin called the a new DEM obtainedLaser in Scanning (TLS) 2010 runs from2013, and that Airborne 2014. were We LIDAR, examined performed these andand data during four air along with the temperature successive data autumns from on Terrestrial during precipitation, the of snow recent closest 2011, depth, years meteorological 2012, in station. thissnowfall Identification region accumulation of is has changes particularly been importantlast higher because decades and in of the the the temperatures 21stlantic 20th, century slightly Oscillation associated cooler index to than (Vicente-Serrano persistentmost the positive et recent conditions response al., of of 2010; the theunknown. remnant Buisan Moreover, North ice the et bodies availability At- of al., to annual this 2015).examination TLS short of data Thus, climatic the in anomaly the recent relationship is years between as permits changes yet detailed in climate and glaciers. 2 Study area and review ofThe the Monte previous Perdido research Glacier on is the(OMPNP) Monte located in Perdido in the glacier the Central Ordesalie Spanish and Pyrenees on Monte (Fig. structural Perdido 1). National flatsand The Park beneath ice are the masses surrounded main are byBono, north-facing, summit vertical 2002). of cli At the the Monte base Perdido Peak of (3355 the m), cli − largest glacier in the Pyrenees.1981 We document to changes 2006 in the andDEMs glacier provide surface derived area updated from from information topographic on maps volumetric of changes 1980 by and comparing 1999 (Julian and Chueca, 2007), and snow/ice melt, whereas large glaciersMoreover, respond very much more small slowly glaciers (Marshall, 2014). term may monthly develop or and seasonal evolvetion climatic for due changes, reasons to such unrelated wind as to (Chueca avalanchesa et long- and considerable al., snow e 2004; accumula- Serrano ettions al., in 2011). the Local ELAs topography of also di has Thus, direct mass-balance estimationsin or ice volume geodetic provide methods betterchanges that information in on determine the climate changes relationship (ChuecaPyrenees, of there changes et are in al., very glaciers few 2007; with estimationsjosé of Cogley, et lost 2009; al., ice 2014; Fischer volumes Marti (Delchanges et Río et of et al., al., al., glaciated 2015), 2015). 2014; surface although San- González-Trueba In abundant areas et research (Chueca the al., has 2008). et examined Annual al., recent estimatesglaciological 2005; of method glacier López-Moreno were mass only et fluctuations performed al.,and based in 2006; on the the Maladeta Ossoue Glacier Glacier (Spanishthickness (French Pyrenees) Pyrenees), was and 14 m these duringOssoue indicated the the Glacier last mean (Arenillas 20 loss etin years of al., in the ice 2008; the Spanish René, Maladeta Pyrenees 2013;pographic Glacier, compared Marti maps and digital et for 22 m elevation 1981 al., models inthe and 2015). (DEMs) the Monte 1999 Other Perdido derived in studies Glacier the from (Julián Maladeta to- and Massif Chueca, (Chueca 2007), and et reported al., losses 2008) and 1999; Carrivick and Brewer, 2004; López-Morenoof et al., recent 2006). changes Moreover, many in studies lengths, glaciers parameters examined that the respond evolutionalso to of explained climate glaciated fluctuations, by surfaces although or geometric this glacier adjustments relationship is (Haeberli, 1995; Carturan et al., 2013a). 5 5 25 20 10 15 25 15 20 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | C ◦ Insti- ). ◦ 40 ≈ , and they were used in the 2 C every 100 m, the annual 0 ◦ 5028 5027 (IGN) (Sheet 146-IV, Monte Perdido; Topographic National C, although this station is on the south-facing slope of the Monte ◦ erent dates can be used to calculate changes in glacier ice volume. This ff The climate in this region can be defined as high-mountain Mediterranean. Precip- The 1981 DEM was obtained from the cartography published by the Spanish There has not been a direct estimation of the current location of the ELA in the The map of Schrader (1874), numerous old photographs, and the location of the tuto Geográfico Nacional Map Series, scale 1restitution : was 25 000). based on This awas map photogrammetry also was flight derived published in from in Septemberdido; 1981. cartography Topographic 1997 National The published and Map 1999 by its DEM 2006 Series the and cartographic MTN25, its IGN scale cartographic (Sheet restitution 1ber : was 146-IV, 25 1999. based Monte 000). The on Per- It 2010 a photogrammetry DEM wasmade flight was published by in obtained in the Septem- from an IGN airborne inOrthophotography LIDAR (NPAO). late flight summer (MDT05-LIDAR) of 2010 in the context of the National Plan for Aerial itation as snow canis fall from on November the to glaciersearch May, and estimated any most the time ablation mean of is annual(Del year, from precipitation Valle, but 1997), June was with most about to most snow 2000 September. precipitation mm Previous accumulation occurring in re- during Marboré spring Lake and autumn. 3 Data and methods 3.1 Comparison of DEMs DEMs from di technique is well establishedet for al., the 2002), study(Chueca and of et we glaciers al., have inestimate 2004, previously the mountainous changes applied 2007; in areas it ice Julián volume (Favey 1999) and in in were the Chueca, several derived Monte Perdido from studies 2007). Glacier. Two topographicmeasurements. DEMs of Thus, maps All (1981 and the and three we one DEMs Pyrenees used (2010)context have 3 was and of from cell a DEMs airborne size geographic to LIDAR ofgeodetic information datum 4 system m (European (GIS) Datum ED50; and UTM unified projection, working zone under 30). a single 2250 ma.s.l.) is 5.03 upper Cinca valley, but studies atplaced the it end of at the about 20th2000), 2800 and and m beginning at in of about the 2950 the m 21st2005). Gállego in century The the Valley, mean west Maladeta annual Massif, of air east temperature the of at the OMPNP the OMPNP closest (López-Moreno, (Chueca meteorological etPerdido station al., Massif. (Góriz Assuming at a lapse rate of 0.55 to 0.65 the 1970s (Nicolas, 1986; García-Ruizwhich et are al., currently 2014). unconnected, The are twoPerdido Glaciers. currently remaining The glacier referred glacier bodies, as beneath the theinto Cilindro upper and three and Marboré lower small peaks Monte has andthat transformed isolated Hernández-Pacheco ice and patches Vidalthickness (García-Ruiz Box of (1946) 52 et m previously al., forthe estimated the 2014). ice upper a It cover glacier maximum at is and ice thebodies noteworthy 73 m end have for mean of the elevations the of lower LIAthe 3110 glacier. had high In and elevation already 2008, 2885 of m disappeared. 82% the (Julián The upperavalanche of and activity upper glacier, Chueca, snow over and accumulation 2007). the lower is Despite ice ice limited body due and to its the marked minimal steepness ( LIA moraines (García Ruiz andof Martí the Bono, 2002) large indicateand north-facing a Marboré unique wall peaks) glacier of at (Fig.Marboré the the 1). foot Glacier, The Monte map with Perdido of threeMonte Massif Schrader Perdido small (Monte Glacier, (1874) which ice Perdido, distinguishes was divided Cilindro theserac tongues into Cilindro- falls that three until stepped joined ice the masseswas in mid connected fed the by 20th by headwall, century. snow The and from glacier ice the that avalanches from existed the at intermediate the glacier, lowest dissapeared elevation after (Oliva-Urcia et al., 2013)et al., and 2014). by dating of Holocene morainic deposits (García-Ruiz isotherm should be roughly atbecause 2950 the to glacier is 3150 ma.s.l., north-facing. although it might be slightly lower 5 5 20 25 10 15 20 25 15 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | erential ff 1.5 m for the 1981 and 2.12 m, and is less than ± ± , a laser beam divergence of Flight, September 1999, scale ◦ Flight, September 1981, scale of ciently precise for our study. The maximum ffi Pirineos Sur 5029 5030 , considering that the firn zone was nearly absent Gobierno de Aragón 3 erence lower than 40 cm, and there was no apparent − ff 0.2 m for the LIDAR-derived DEM of 2010. The combined verti- ± s) were used to assess measurement accuracy. Ninety percent of the ff , and a maximum working distance of 6000 m. ◦ erent dates (September of 2011 to 2014) could be compared. Indirect registration The most recent estimates of the evolution of the glacier were from annual TLS When TLS is used for long distances, various sources of error must be considered, The root mean squared error (RMSE) for vertical accuracy calculated by the IGN for ff 1.8 m for comparison of the 1999 and 2010 DEMs. Vertical RMSE values were used namely the instability of the(Reshetyuk, device 2006). and We errors used fromin a georeferencing the frontal the glacier view point and of of atration, the clouds scanning also glacier distance called of with target-based 1500 registration minimaldi to (Revuelto shadow et 2500 m. zones al., We 2014), also souses used that fixed indirect scans regis- reference from pointsflective (targets) targets that of are knowna located shape distance in and the from dimension study theods, are area. we scan placed Thus, obtained station at 11 accurate the of re- global reference 10 points coordinates to at for 500 m. the Using targets standard by topographic use meth- of a di global positioning system (DGPS)acquired with in post-processing. the The UTM globalfor 30 coordinates the coordinate were system global in targetvariant the elements coordinate ETRS89 of datum. was the The 0.05rocks landscape m final and surrounding precision in the cli planimetry ice bodies and (identifiable 0.1 m sections of in altimetry. In- reference points had elevation di relationship between scanning distance andwas observed considered to error. Such add error 40conversion cm bars of of to mean deviations the ice calculatedplying ice elevation depth change mean and to density mass annual of loss mass rates. 900 kgm The budget rates was done ap- (Chueca et al., 2007; Marti et al., 2015). airborne LIDAR have been useding in changes diverse in geomorphology the studies,The volume including device of monitor- used glaciers in (Schwalbe the ettime-of-flight present al., technology study 2008; is to Carturan a measure long-range et the TLS al., time (RIEGL 2013b). LPM-321) between that the uses emission and detection of surveys. LIDAR technology has developed rapidly in recent years, and terrestrial and of 1 : 20 000,tographs color). were There used were (PNOA no1999 2006 high and Flight, quality 2006 August flightsgeometry photographs 2006, for and were scale 2010, georeference already of so themodule 2006 1 orthorectified, : of aerial aerial 5000, but ArcGIS. pho- survey color). The we of referenceDEM The had data for 1981 from to the 1999. by The control correct horizontal use pointsfrom RMSE the was 2.1 accuracy of of to from the the 4.7 the set m, georeferencing of orthophotoshorizontal and control-points error and was ranged value considered was su used totheir calculate temporal error bars changes. to A estimatedgenerate resampling glaciated areas the procedure and final using rectified cubic images. convolution was used to 1 : 30 000, black and white; 1999: a light pulse to produceused a three-dimensional in point this cloud from studyacquiring real employed topography. data The light TLS from pulses snowet at and al., 905 nm ice 2011), (near-infrared), cover a0.0468 which (Prokop, minimum 2008; is angular Grünewald ideal step et for width al., of 2010; 0.0188 Egli ± to estimate error bars toThese provided combined values vertical of RMSEs glacierbecause changes were changes in in considered both ice precise depth analyzedvalues. enough in periods. The our for analyses estimation our were of generally purposes, by ice much the greater volume use than changes of these the was1999 tool performed and “cut-and-fill” in for 1999–2010). comparing ArcGIS Theretrieved pairs (ESRI, from glacial of Inc.) aerial glacier perimeters photographs surface (1981: associated DEMs with (1981– each DEM date were 1999 DEMs, and cal RMSE for comparison of the 1981 and 1999 DEMs is their digital cartographic products at the 1 : 25 000 scale is 5 5 25 15 20 10 15 10 20 25 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | s. ff 0.13 in ± s. Both ice ff . From 1999 to 1 − C) than for the ablation ◦ 5 0.01 hayr ∼ ± 0.06 ha in the upper glacier and 3.0 5032 5031 600 to 1500 mm (Fig. 2e). The trend line had ± ∼ ce (AEMET) provided climatic data from the Góriz ffi 0.19 ha (1.5 ± 0.05) during the accumulation period (Fig. 2c and d). The air p < cient of Mann–Kendall’s tau-b (Kendall and Gibbons, 1990). ffi C). Precipitation during the accumulation period also exhibited strong in- ◦ 2.5 C during the accumulation and ablation periods, respectively. The minimum ◦ ∼ Table 1 shows the surface area of the ice in 1981, 1999, and 2006. From 1981 to Figure 2 also shows that the last three years, for which we have TLS measure- 1999 the glacier lost 4.5 ablation months. 4.2 Glacier evolution from 1981 toFigure 2010 3 shows two photographs ofA the simple glacier visual taken in assessment lateyear shows period. summer of In the 1980 1981, fast and thedisconnected 2011. upper degradation and of from lower the glaciers 1973 were glacier tonificant no during ice longer 1978), united this depth and (they with 30 became theybodies noticeable were exhibited seracs heavily crevassed, a hanging with from concave evidencephotograph of the surface of ice edge and motion 2011 of over a shows the theshowing whole sig- that a cli glacier. dramatic The the reduction two indisappearance ice ice of thickness, bodies almost manifested are all by the furtherCrevasses seracs, are concave and separated, surface, only the the as evident retreat well inmotion of of the as ice the eastern from glacier part the hasthere of edges slowed are or the of stopped rocky lower the in outcrops glacier, cli most incovered indicating of by the that these debris middle the two deposits of ice from bodies. the several Moreover, lower crevasses glacier or rock and falls areas in that the are upper partially areas. the lower glacier), corresponding to an overall rate of 0.25 ments of annualSeptember 2011 glacier to mid-September evolution, 2012pecially was had during one the of extremely ablation the25 warmest period) variable %). recorded and The conditions. years one period (es- of Thus, ofthan the 2012 average driest mid- and to recorded the 2013 years coolestto had (close recorded an 2014 to summer, accumulation was and the period very the that accumulation wet period was and of more mild, 2013 humid with air temperatures well below average during the a slight increase, but thiscumulation was during not April statistically significant. varied Similarly,trend from maximum during less snow the than ac- study 50 period to (Fig. 250 2f). cm, and there was no evident Figure 2 illustrates the1983. The high maximum interannual air temperatures variabilitysons during of the had climate snow no accumulation in significant andThe ablation the trends, range sea- between with study the highest Mann–Kendall area and values3 lowest since anomalies close and during to the 4 study 0 periodair (Fig. exceeded temperatures 2a had and very b). tistically weak significant increases ( in both seasons, but these were only sta- 4 Results 4.1 Climatic evolution and variability from 1983 to 2014 3.2 Climatic data The Spanish Meteorologicalweather O station, located atMassif. Given 2250 ma.s.l. no changes on in instrumentationlogical the and station southern observation since practices slope 1983, in and of the(2.7 the meteoro- km) the proximity suggests of Monte that the Perdido it meteorologicalclimatic accurately station record records to consists the the of climate glacier daily variabilityFrom data over these of the air data, glacier. temperature, The we precipitation,tures and for derived the snow annual main depth. periods seriesSeptember), of of precipitation snow accumulation during maximum (November–May) the and and accumulation ablationin minimum (June– season, April and air (generally maximum the tempera- snowstatistical time depth significance of of maximum the snowpack linear atcorrelation climate coe this trends was meteorological assessed station). by The the non-parametric temperature range was larger for the accumulation period ( period ( terannual variability, with a range of 5 5 15 20 25 10 15 20 10 25 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ), 1 − 0.4 m 0.4 m 0.11 m ± 0.15 ha ± ± ± , more than 1 ected almost − ff ), respectively. 1 − 0.14 mw.e.yr ± 0.4 m (1.92 ± 0.23 hayr ± ), with some regions expe- 1.8 m in the upper glacier 1 0.4 m in the lower glaciers). 2.12 m in the lower glacier − 0.1 mw.e.yr ± ± ± ± overall, or 0.72 1 − 1.8 m overall); corresponding to rates of 0.36 mw.e.yr ± ± 0.16 myr 0.09 ha in the upper glacier and 3.4 overall, or 0.39 5033 5034 ± 1 ± − (0.8 1 − 0.4 m (0.64 0.4 m in the lower glacier). Ice thinning a ± 0.11 myr ± erent from 2012 to 2013, with a rather wet accumulation ± 0.24 ha (2.0 ff erences in ice depth between consecutive annual scans ± ff 0.16 myr (0.46 ± 1 0.4 m in the upper glacier and 0.38 − ± 2.12 m in the upper glacier and 8.79 ± 1.8 m in the lower glacier (8.98 0.11 myr ± ± 0.4 m in the upper glacier and 0.01 m in the lower glacier). 2.12 m overall); thus, the mean rate of ice thickness decay was 0.34 0.4 m (0.32 0.16 m and 0.81 ± ± measurements ± ± The overall result of a very negative year (2011–2012) for glacier development fol- Comparison of the elevation of the glacier’s surfaces derived from the DEMs (1981 The period of mid-September 2011 to mid-September 2012 was very dry during the Conditions were very di (0.08 riencing losses greater than 6 m.that Only were the at areas high of thethis elevations eastern (around period, part the and of rimaye) this the exhibitedand lower was some glacier lowest typically elevation ice less gain losses during than 2 during m. 1981–2010 Interestingly, the were areas similar with to greatest those with the greatest and lowed by two years (2012–2013to and a 2013–2014) net of average ice anomalous loss positive of conditions 2.1 led in the upper glacier andthe 1.97 entire glacier, and waslower particularly glaciers, intense where in the losesdepth western were increases sectors in more of the than the middle upperexisting 4 of m. crevasses. and the lower The glacier few are scattered likely to points be indicating from the motion of the Very similar conditions occurred in 2013–2014,below with average very wet air accumulation temperature months during and eas the with ablation moderate period. increaseswere Again, in still there thickness areas (sometimes were with exceeding large significant ice 3 ar- m), loss, with although an there average depth decrease of 0.07 period and very cool ablationsharply period. with those These of conditions the ledice previous to thickness. year, in changes Most that that of large contrasted highest these areas of increases elevation the did areas glacier not hadeas of exceed increased remained both 1–1.5 stable m, and ice and some1.5–2 most bodies. m areas were Nonetheless, in even in exhibited the during the noticeabledevelopment upper ice this from and losses year, 2012 (more lower large than to glaciers).0.34 ar- 2013, Despite the the excellent average conditions increase for of glacier glacier thickness was only total change from 2011 tochange 2014. measured Figure over 6 the shows glacier the for frequency these distribution periods. of ice depth to 1999 vs.time 1999 (Fig. to 4). 2010)erage During also the of 1981–1999 indicates 6.20 period, an the acceleration ice of thickness glacier decreased wastage by an over av- (September 2011–2012, September 2012–2013, and September 2013–2014) and the accumulation period and very warmdramatic during declines the of ablation period. ice These depth, conditions with led an to average decrease of 1.94 three-times the rate of the previous 18 years. and 0.48 respectively. The spatial pattern ofwith ice the losses resembled smallest theglacier decreases pattern and from in the 1981–1999, the proximaldistal area eastern and of central-eastern and the parts higher upper of both glacier, elevation ice and parts bodies. the4.3 of greatest decreases the in lower Evolution the of Monte Perdido Glacier from 2011 to 2014 fromFigure TLS 5 shows the di (8.35 in the lower glacier), corresponding to an overall rate of 0.77 Moreover, the changes ineither glacier glacier had thickness increased had thicknesses,mained but spatial rather some heterogeneity. small stationary, No with areas ofof declines sectors the in ice of lower thickness glacier thickness less re- werelower than in glaciers, 5 m. the with The lower1999–2010 largest decreases elevations losses period, that and exceeded the western 25 loss regions and of of 35 the ice m0.72 upper respectively. thickness and During was the 7.95 2006, the glacier lost 5.4 and 9.13 5 5 25 25 20 20 10 15 10 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 0.1 and ± for the 1991–2013). The 1 − erent periods (0.39 ff ect of the cold and wet period ff for the 1983–2014). The smaller 1 − 5036 5035 1.45 mw.e.yr − ), is 50% greater compared to the period 1983–2014 1 − for 1980–1999 and 1999–2010 periods respectively) are similar 1 − 1.45 mw.e.yr − for the 1981–1999 period; and 0.7 mw.e.yr 1 ) (Marti et al., 2015). The accelerated degradation of the Monte Per- − 1 − 0.14 mw.e.yr C for the periods 1983–1999 and 1999–2010 respectively), and precipitation and ◦ ± 1 mw.e.yr The mass loss rates presented in this study for the di − to the reported by Chueca(0.36 mw.e.yr et al. (2007) and Marti et al. (2015) for the Maladeta massif of the 1960s toincreased 1970s occurrence is of removed. very Thus, wetstrong winters Vicente-Serrano negative after et the NAO al. 2000s winters. (2010) was Inperiod associated found agreement, of with that Buisan 1980 frequent the et to 2013 al.tionary the (2015) and overall indicated even number slightly that of increased snow for inthe days the some in view locations. the Macias that Pyrenees et southern remained al.clear sta- (2014) Europe moderations also of and support the some warming othertury. trends Nonetheless, that regions were it of reported is the atdendroclimatological necessary the world reconstructions end to have for of bear undergone the the in Pyrenees 20thered still cen- mind in point that this out the study thea longest (1980–2014) period dry climatic consid- as period records a compared or very to2008; strong the Deaux period positive et spanning anomaly al., since of 2014; the Marti temperature end et and of al., the 2015), LIA0.72 (Büngten et al., most recent mass balancesimilar to values those obtained reported for for theglaciers Swiss in the Alps some Monte (Fischer areas et of Perdido al.,most the Glacier 2015), Italian retreating or Alps are glaciers the (Caturan in best more et preserved theOssoue al., Alps Glacier 2013a); but (Carturan (French much Pyrenees, et lower al., to 2013b) the or the one reported in the 2000 in the Pyrenees (López-Moreno,and 2005). milder These trends air of temperatures decreasingin precipitation during the North winter Atlantic and2008). Oscillation early Most (NAO) spring recent index were studies duringcentury) related this that confirmed to period used a (López-Moreno changes updatedfected shift et databases to al., in the (including most NAO data recent evolutionThus, evolution of of toward no temperature the more and temporal 21st precipitation negative trends overwhen the evolution of the Pyrenees. that both study af- variables period are starts found in near the the 1980s Monte and Perdido the Peak, e lowest ice losses duringshrinkage 2011–2014, over indicating time. a consistent spatial pattern of glacier 5 Discussion and conclusions The results of this studywas indicate that similar the to recent that evolution2013), of of especially the those Monte many in Perdido other Glacier Europeet glaciers (Gardent al., et worldwide 2014; al., (Marshall, Marti 2014;and 2014; Abermann et has Vincent et al., clearly al., et 2015) 2009; accelerated al., the where Scotti Monte after glacier Perdido 2000. Glacier shrinkage was More three-times began1981–1999 specifically, greater period; at from the and the 2000 the annual loss to end of lossobserved 2006 of ice compared from of thickness to 1981 the from area the to 1999 LIA 1999. of toin Acceleration 2010 the in was Ossoue double glacier the Glacier shrinkage rate (French hasriod Pyrenees), been 2001–2013 where also ( mass reported balance decline during the pe- ( dido Glacier cannot simply bethe explained sharp by an decline intensification ofteorological of snow station climate accumulation. clearly warming or Climate refute by stationary this data during hypothesis, (1983–2014) the because of ablation air period a13.6 temperatures (i.e. nearby average remained maximum me- temperature wassnow 13.4 depth and accumulation during accumulation periodcreased were also (average stationary precipitation or was slightly 1013 in- andsnow 1028 depth mm; and in average April maximumrespectively). annual was Previous studies 104 of and the 131temperature Pyrenees cm has and for significantly surrounding the warmed areas showed throughout periodsrelatively that the 1983–1999 cold air 20th period and century, from especially 1999–2010 after theKenawy et the 1960s al., to 2012; Deaux the et mid-1970scant al., decline (López-Moreno 2014). of et At snow the al., accumulation same from 2008; time, mid-March El there to was late-April/early-May a from regional 1950 signifi- to 5 5 10 15 20 25 10 15 20 25 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | of the ff 0.4 m, roughly one-fourth of the ± 5038 5037 This study was funded by two research grants: “CGL2014-52599-P, Es- The future long-term monitoring of the Monte Perdido Glacier is likely to provide glacier area and volume205–215, in, doi:10.5194/tc-3-205-2009 the 2009. Austrian Ötztal Alps (1969-1997-2006), Theespañolas. Cryosphere, 3, El programa ERHINRural y (1984–2008), Marino, Ed. Madrid, 231 Ministerio pp., 2008. de Medio AmbienteChange, 59, y 5–31, Medio 2003. snow and precipitation days35, in 259–274, the 2015. western and central Spanish Pyrenees, Int.the J. Pyrenees, Clim. Climatol., Dynam., 31, 615–631, 2008. climatico” (Ministry of Economyde and su Competitivity), and dinámica “El actualcambio glaciar global” y de (MAGRAMA procesos Monte 844/2013). criosféricos Perdido: Authors estudio thank asociados the como support indicadores provided de by the procesos sta de important information on the year-to-yearto response a of the wide mass varietypositive balance of and of climatic this negative glacier conditions, feedbacksglacier in and may this will serve much allow as deteriorated a detailedthe model glacier. analysis world for Thus, that of studies study have of the similar of the role characteristics this evolution now of of andAcknowledgements. glaciers in in the other future. regionstudio of del manto de nieve en la montaña española, y su respuesta a la variabilidad y cambio is restricted to thisobserved smaller for area, other it Pyrenean glaciers is (López-Moreno likely et that al., its 2006). rate of shrinkage will decrease, as Arenillas, M., Cobos, G., and Navarro, J.: Datos sobre la nieve y los glaciares enBeniston, las cordilleras M.: Climatic change in mountainBoyé, M.: regions: Nevés et a érosionBuisan, glaciaire, review Rev. 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Perdido Obviously,conditions. this Glacier A indicates that is ground-penetrating the radar seriously future ported (GPR) threatened, a survey even maximum of ice under the depthareas stationary close lower of climatic to glacier this 30 m in glacier (unpublishedbe may 2010 report), accelerated even re- by suggesting disappear negative that within feedbacks large themiddle such of next as the few the glacier years. recent and Thisablation rise the by process of thin decreasing may cover the rocky of albedo. outcrops The debris,the in highly both last the consistent 30 of spatial years which pattern suggests maythe of that accelerate eastern-most ice the glacier part losses western-most will in part survive of asaccumulation this a during glacier small residual positive will ice disappear years mass first; and because of a greater lower snow rate of degradation. When the glacier rates in the Spanish side oflocation the Pyrenees of compared the to the remnant later iceelevated may and be bodies explained the in by best the Southern topographic sideet locations of al., in the 2006). their range, Oppositely, respective the confined cirquestongue in Ossue (López-Moreno in the glacier an most still easting has slope.tion maintained In of a this the considerable context, Monte glacier the Perdidosince Glacier only the after explanation end 1999 for of is the theablation that rapid LIA the degrada- ratio was progressive (AAR), warming responsible of observed and3050 ma.s.l. a most dramatic during of reduction the in thisin period the glacier that 2011–2014, accumulation- significant is Fig. ice currently 5d).years losses This below (with occur leads little the during accumulation to unfavorable current years orthe a ELA glacier and warm clear cannot even (at ablation imbalance, recover during seasons). ice “normal” cumulation Because losses and/or during of little periods this ablation). with imbalance, This favorableTLS conditions hypothesis measurements (high is from ac- strongly the supported lasttwo by four our consecutive years. detailed In anomalously particular, positive thesecovery years TLS of (2012/13 data the showed and that losses 2013/14)glacier from depth did during not a this allow negative three re- year years (2011/12). period was Thus 2.1 the average decrease of 5 5 10 25 20 15 20 25 10 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | erences, Terra Glacialis, 2008, 137– ff 5040 5039 erent scales in the Alps, Ann. 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P., Linda, A., Berthier, E., Sharma, P., 5 5 10 20 30 15 25 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 0.23 0.09 0.15 0.24 ± ± ± ± 0.01 0.77 0.060.130.19 2 3.4 5.4 ± ± ± ± 0.211.48 1.5 1.69 3 4.5 ± ± ± 0.291.63 4.8 1.93 33.7 38.5 ± ± ± 5046 5045 Surface Area Loss of Surface Area 0.361.76 6.8 2.12 37.1 43.9 1981 1999 2006 1981–1999 1999–2006 ± ± ± ) 0.25 1 − Monte Perdido study area and extent of ice cover at the end of the Little Ice Age Surface area (ha), loss of surface area (ha), and annual rate of surface area loss ) of the Monte Perdido Glacier. 1 − Upper glacier (ha) 8.3 Entire glacier (hayr Lower glacier (ha)Entire glacier (ha) 40.1 48.4 Figure 1. (according to the map of Schrader, 1874) and in 2008. (hayr Table 1. Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper |

F B D Year 1985 1990 1995 2000 2005 2010 2015 Tmax ablation Tmax Tmin ablation Max. snow depth (April) (April) depth snow Max. 0

8 6 4

50 16 15 14 13 12 11 10

10

Temperature (ºC) Temperature Temperature (ºC) Temperature 250 200 150 100 Max. snow depth depth snow Max.

E A C 5048 5047 2011/12 2012/13 2013/14

Year 2011 1981 1985 1990 1995 2000 2005 2010 2015 Tmax acumulation Tmax Precip. acumulation Precip. Tmin acumulation

0

8 7 6 5 4 3 0

Temperature (ºC) Temperature -1 -2 -3 -4 -5

800 600 400 200

Temperature (ºC) Temperature 1800 1600 1400 1200 1000 Precipitation (mm) Precipitation Interannual fluctuations and overall trends (straight lines) of minimum and maxi- Photographs of the Monte Perdido Glacier during the late summer of 1980 and 2011. Figure 3. mum air temperatures duringaccumulation the period, and accumulation maximum and snowteorological depth ablation during station periods, April (1983 precipitation based to on duringvariability data 2014). the during from Boxplots the the at Gorizlaser most me- the scanning recent measurements right were 3 of available. Box:10th each years 25th percentiles percentiles panel (2011/12, and and show 2012/13, 75th the percentiles,median, 90th and bars: red interannual percentiles, 2013/14) line: dots: average. when 5th terrestrial percentiles and 95th percentiles, black line: Figure 2. Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | . (d) , and 2011 to 2014 5050 5049 (c) , 2013 to 2014 (b) , 2012 to 2013 Changes in ice thickness in the upper and lower Monte Perdido Glacier from 1981 to Changes in ice thickness based on terrestrial laser scanning from September of 2011 (a) to 2012 Figure 5. Figure 4. 1999 and from 1999 to 2010 based on comparison of DEMs. Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Upper 2014-2011 Whole Lower Upper 2014-2013 Whole Lower Upper 5051 2013-2012 Whole Lower Upper 2012-2011 Whole Lower

4 2 0

-2 -4 -6 Changes in ice thickness over the whole glacier, lower glacier, and upper glacier for Change in elevation of glacier surface (meters) surface glacier of elevation in Change Figure 6. the same 4 timeline: periods median, examined red in line: average, Fig. bars:and 5. 10th 95th percentiles Box: and percentiles. 25th 90th percentiles percentiles, dots: and 5th 75th percentiles percentiles, black