1 warming, digital mapping. anthropogenic causes. dueto naturalratherthan was mostlikely the endofLittleIceAge. The warming after began inthemiddleofXIXcentury coolingperiods, alternated withshort-term suggest thatglobalclimate warming, which volume haseven slowed down. These facts evenly through timewhilethedecrease inits practically the area reductionwasoccurring the 1850–1887period. Beginning in1887, the greatest rates ofitsretreat coincidedwith volume oftheElbrusglaciationindicated that Quantitative dataonchangesinthearea and glaciation). is representative ofall Central Caucasus largest (which Elbrusglacier)andDzhankuat (the ofglaciersBolshoiAzau fluctuations approximatelycyclical, 55years long, frontal and digital methods. There were glaciation were studiedusinglichenometry withinthelargest inEurope Elbrus century from themiddleofXIX been occurring Changes inthearea andvolume thathave 2 Yevgeniy A.Zolotarev Corresponding author * [email protected] Moscow State University e-mail of Cartography, Faculty ofGeography, M.V. Lomonosov of Cartography, Faculty ofGeography, M.V. Lomonosov Moscow State University KEY WORDS: ABSTRACT MONITORING GLACIO-CARTOGRAPHICALOF THE CHANGING CLIMATE. KEY FINDINGS SINCE THE MID XIX CENTURY UNDER EVOLUTION OF THE ELBRUS GLACIATION Research for Associate , oftheLaboratory Department for Remote Sensing, scientistoftheLaboratory Senior Department

Elbrus glaciation,global 1 and Yevgeniy G.Kharkovets* glaciers’ response to climate 1849 change. In are crucialindefining the observations ofsomeElbrusglaciers. observations These has establishedafoundation for long-term Russian Academician G.Abich[Abich, 1875] to thepresent time. end oftheXIXcentury –from for the been conducted over acentury 140 km exceeds Elbrus glaciationwhichphysical surface satellite ofthelargest monitoring inEurope can betested andaerial- through cartographic specifically, thearea andvolume. This hypothesis should affect theirreg change. inglobaltemperatures Increase glaciersareMountain sensitive to climate 2003;Climate Change, 2001]. [World..., world models have emerged inRussiaandthe effect. Anumberofglobalclimate warming asaresult ofgreenhousethe XX century gases inthesecondhalfof warming, whichstarted by climatologists suggest globalclimate Numerous recently studiesconducted TO CLIMATE CHANGE THE GLACIER’S RESPONSE THE FRONT FLUCTUATIONS – INTRODUCTION 2 . ofthisglacierhas The monitoring 2 imes and parameters, imes andparameters,

13 14 GEOGRAPHY at 2322mfrom barometric leveling anda Abich conducted thoroughAbich conducted studiesof related glacier. to theBolshoiAzau its parts G. adetailedpresentation especially of deserves to most researchersunknown and, therefore, G. Abich’s for somereason, work, stillremains reconcile withoutG.Abich’s data. assessments are hard to interpret and of thespatialpositionglacier. Such assessments 1866] provided contradicting 1890;Mushketov, [Dinnik, 1882;Salatskyi, to 1887andmany researchers ofthattime inElbrusprior were surveys nocartographic State (MSU)Elbrusstation. University There the present-day M.V. Lomonosov Moscow of 2295–2300 melevationinthevicinity valleyat at thebottom oftheriver Azau glacier’s wasatawell definedmoraineline wasassumedthatthe 1958].It [Tushinski, Caucuses inthemiddleofXIXcentury the glaciationexpanseinCentral end accepted asafundamental evidenceof on amature pineforest. waslater This fact Abich found thattheglacier hadintruded glacier.Bolshoi Azau hisfirsttrip, During G. to the trips and 1873,G.Abichmadetwo Azau the glacier’s elevation( Hedefined using instrumentalobservations. tongue on October 21,1849.Picture by G.Abich tongue onOctober Fig. 1.Location Azauglacier oftheBolshoi

glacier tongue [Abich, 1875]. fluctuations in 1849–1873 in1849–1873 fluctuations on October on October 21 1849) 21 1849) the Bolshoi the Bolshoi located there in1849. 27 m. Therefore, theglaciercouldnotbe oftheMSUElbrusstationis in thevicinity crest andthelowwater Azau lineoftheriver The difference intheelevationofmoraine “Elbrus”.cable-way only inthearea ofthelower stationofthe moraine slopeofsuchrelative heightexists This difference appeared to be37,5m. The moraine covered withmature pineforest. abutted againstamore ancientend-lateral the elevationofpointupperapex moraine lineattheglacierendin1849and difference intheelevationsoffoot ofthe byG.Abichwasthe measurement taken to 1873wasmeasured at180m. The third result. The glacierlinearretreat from 1849 accepted thismeasurement asthefinal elevation measurement (2317m).G.Abich to 1849resulted inadifferent endmoraine pressure andtemperature) in1873compared environmental conditions(atmospheric Differentinstrument andbenchmark. same barometric leveling usingthesame retreating glacier(Fig. 2).Hemadethe September 17,1873,G.Abichfound the hissecondvisitto theglacierin During across from hotel Cheget. amodern of Mt. Terskolak’s slopeabove theforest level ledge rocky a pointlocated atawell-marked glacier (Fig. 1). This drawing wasmadefrom to ofthe draw generalboundaries sextant of angularmeasurements withaportable the future andlimited hisstudiesto theuse to return toHe didnotexpect thearea in ofPyatigorsk. nearthecity benchmark known tongue on October 17,1873Picture by G.Abich tongue onOctober Fig. 2.Location Azauglacier oftheBolshoi [Abich, 1875]. beginning XX documented by centuries Later research oftheendXIX– activities glacier in1849(Fig. 3). oftheBolshoiAzau of theendice-flow precise ofthespatiallocation determination of 2317m. These dataare sufficientfor a corresponds well withG.Abich’s measurement line atthebottom ofthevalleyis 2315m,which elevationofthefootcentury. Modern ofthis valleyinthefirsthalfofXVII in theAzau growth issimilarto thatofpinesappeared the analysisshowed thatthistree’s annualrings line where pinewasfound aburied in1968; Furthermore, itwasthefarmostmoraineend ofthecable-way vicinity “Elbrus” iswell visible. cone); buttheendmorainelinein mudflow Garabashi bytheriver is obstructed oftheMSUstation(it be seeninthevicinity from thispoint, the endmorainelinecan’t tracesofrecent glaciation.However,preserved from thispointinAugust 1981showed well glacier. conducted Aphototheodolite survey showing theendmorainelineinfront ofthe his drawings oftheglacierin1849and1873 We found thepointfrom whichG.Abichmade Fig. 3.Endmoraine inthemid. at XIXcentury thebottomofAzauriver valley. Phototheodolite imagetaken onJuly15,1981. elevation ofthesamewaterfall. of 2345m,whichis75mhigherthanthe canyon. mapshowstheelevation The modern inthe Azau oftheriverMalya the waterfall tongues atapproximately 70–80mhigherthan location. The 1911mapshowstheglaciers also correspondsglacier’s well withtheactual m (or2325ontheG.Burmester’s map). This 2345 glacierin1911wasactually Boshoi Azau ofthe elevation oftheendice-flow map.than thatofthemodern Therefore, the elevations ofthe1991mapto be20mlower the I.A.Labutina(1968)determined Year (IGY). Geophysical theInternational during conducted compiled from thephototheodolite survey should bereconciled map withthemodern systems ofthesemaps Elevation benchmark [Burmester, 1913]. byG.Burmester phototheodolite survey map compiledfrom thedataof1911 anda1:20000scale Engineers surveys of the 1887–1890Corps Topographical scale topographic mapcompiledfrom glacier tongue. These mapsare a1:42000 locationofthe theexact maps describe

15 GEOGRAPHY 16 GEOGRAPHY Bolshoi Azau ice-flow endelevationcan ice-flow Bolshoi Azau well witheachother. Therefore, the1887 systems correspond slope) mapsbenchmark (oftheElbrussouthern The 1887andmodern Fig. 5. The Azauglacier. tongueoftheBolshoi Phototheodoliteimageby A.V. Blryuhanov. August 1958. Fig. 4. The Azauglacier. tongueoftheBolshoi Image by A.V. Pastuhov onAugust 5,1890. glacier belowtheicefall, andthepresence oftheentireend moraine, intense cracking were: asteep glacier’s front, absenceofthe to thegrowing phase. The evidenceofthat growing orasaboutto beready to transition theglacieras described G. Burmester elevation from thelowriver level. 1911, In open rocks whichwere atabout2327m wasadjacentto the oftheice-flow part a steep slopecrossed bycracks;theright endedwith oftheice-flow the lower part any instrumentalmeasurements),conduct didnotglacier in1881,butwhounfortunately G.AbichtoN.I. Dinnik(firstafter visitthe of otherinvestigators According to 1881 It is alsohelpfulto review observations (Fig.clearly 4). canyon, canbeseen theAzau had blocked end ofthelava line, whichsometimeago the locationofglacier’s front atthe on August 5,1890byA.V. Pastuhov (1893), This elevationis2330m.Onthephoto taken caused bydeadiceneartheglaciertongue. 1957 maps, whichexcludes distortion be obtained byoverlaying the1887and completely free ofdeadice. whenthevalleywas phototheodilite survey riverusingdataofthe1987 site attheAzau topographic map, whichwe created for a were reconciledThe surveys usinga1 : 5000 fromtongue fluctuations 1849to 2002(Fig. 7). glacier oftheBolshoiAzau compile achart of 1973,1980,1987,1997,and2002(Fig. 6)to the glaciertongue in1969,andoursurveys in1957–1959 (Fig. of survey 5),thesurvey oftheElbrusphototheodolitematerials the glacierretreat attheendof1940s), P.V. [1961](whoprovided Kovalev dataon theglacierin1932–1933), (who surveyed We by usedworks Ye.P. [1936] Oreshnikova [Altberg, 1928]. in thecanyon andwasagainretreating glacier was20mhigherthanthewaterfall thatthethe glacierin1925–1928)reported 1925, 1933]. In V.Ya at Altberg (whoworked 15 maheadcompared to 1911[Soloviev, S.P. Soloviyev in1913,theglacieradvanced to V.P. Rengarten’s communication with 2600 and2700melevation.According swell wave slidingbetween of asurface Fig. 6. The Azauglacier. tongueoftheBolshoi Phototheodoliteimageby Ye.A. Zolotarev. August 31,2002. at arepresentative oftheCentral Caucuses withaninsignificant timeshift similar cycle specialresearchDuring efforts,we found a the cycles. in the1970s, between with55-years intervals phases and itsearly small advancesduring delays and andinterrupted byshort cyclic rate wasabout19m/year. This retreat was retreated 2860m,i.e., theaverage retreat 150years, during Overall theglacierhas area wassimplygettingfree ofdeadice. retreat thistime, in1959–1969.During the help to explainthepeakrates oftheglaciers The aforementioned information may also glaciation...,1968]. researchers [The elevations oftheglaciertongue byearlier its bed. This madeitdifficultto systematize end positioninthevalleyand40mabove glacier front was700mabove itsactual for example, onthe1957–1959map, the the identificationofitsfront location. Thus, large volume ofdeadicethathampered simultaneous formation inthevalleyofa featureA distinct ofthe glacierretreat isa

17 GEOGRAPHY 18 GEOGRAPHY cartographic measurements onthe1887cartographic possibleto make that itwasinprinciple 1887–1957. Analysisofthemaps confirmed spatial changesoftheElbrusglaciersduring map to obtainquantitative parameters of mapwiththeold themodern superimpose it hadto ifitispossibleto bedetermined compiled into a1:42000scalemap. First, Engineers in1887–1890. was The survey by ateam of oftheCorps Topographical entire Elbrusglaciationwasconducted ofthe survey instrumental (plane-table) scale, topographic map. survey ofthe1887–1890,1 Analysis : 42000 advances. iftheglacierretreats determines or ice-flow the iceinflowandlossatendof area oftheglacier. The difference between oftimeintheaccumulation a longperiod the iceinflowstays relatively constantduring endablationwhile changes oftheice-flow 2003]. Changesinairtemperatures cause glaciers response [Zolotarev andPopovnin, main climaticparameter thatinfluencedthe suggests thatairtemperatures were the glacier.glaciers theDzhankaut This fact MATERIALS ON ELBRUS GLACIATION ANALYSES OF CARTOGRAPHIC Fig. 7.Fluctuations Azauglacierfrom oftheBolshoi 1849 to2002.1–theglacieradvancement.

The first indicated that above this mark, changes indicated thatabove thismark, 4000 melevation. The research conducted the glaciers’ tongues, i.e. upto approximately map canonlyproduce reliable estimates for shouldbenoted, thatthe1887 glaciation. It changes inthearea andvolume ofthe and usedincomputer modelsto determine Then, thisandthe1957mapswere digitized available. were reconciled whennewdatabecame on; especiallywhentheglacierboundaries This newlycompiledmapwasrefined later exposurelocated onthesouthern slopes. was appliedto allglaciersexcept to those contours, a5msystematic error correction oneanddrawinginto elevation themetric Russian elevationsystem (Russian fathom) and oldmaps. theoldWhen converting identical control pointsonthe modern was donebyzones usingatleastthree of themore map. modern This transition coordinate system andelevationbenchmark 1 : 42000 into a1 : we themapfrom decidedto convert a 25000 scaleusingthe solutions for ourcase, thisproblem. In there material; arecartographic nostandard maps ischallenging even for themodern shownonmultitemporal similar surfaces Elbrus map. of superimposition Acorrect digital methods(147,5кm mapusing measured onthenewly-compiled that thearea ofglaciationin1887,whichwe shouldalsobenoted glaciation evolution. It is alsosuitablefor thestudiesofElbrus area below4000 m. Therefore, the1887map changes are associated specificallywiththe and 1997indicated thatover 90%ofvolume photographycompiled usingaerial of1979 of multitemporal digital modelsofElbrus special research aimedatcomparison efforts measurements [Zolotarev, 1997]. However, in elevationmay bewithinanerror of orthophtographic mapcompiledfrom the orthophtographic All thesedatatogether withthedigital Age” XIX)[Solomina,1999]. (XIII-mid to themaximalparameters ofthe “Little Ice appeared thattheseparameters were close area andvolume inthemidXIXcentury. It were used to theElbrusglaciation determine materials moraines wasaccomplished. Its survey, studyofstadial alichenometric the1986–1987phototheodoliteDuring was conducted. photographic1979–1987, itsaerial survey additionin the entire Elbrusglaciation.In wasrepeatedphototheodolite for survey 1986–1987,the etal., 1984].In [Knizhnikov wasundertaken forwork thesecondsurvey recognizance 1980–1983,apreliminary In glaciation..., 1968]. oftheElbrusglaciation[The monitoring map for thefuture cartographic-aerial-space 1:10 000scalemap, whichbecameabase of theElbrusglaciation. They compileda to assesstheevolutionphototheodolite survey MSU Faculty ofGeography a conducted andGeoinformaticsof Cartography ofthe Aerial-Photo oftheDepartment Methods) of (atthattime,Methods theLaboratory forscientists from Aerospace theLaboratory glaciation. Modern cartographic materialsontheElbrus negligible error ofestimates. grid.measuring This isconsistent withthe Podozersky [1911]ontheoriginal mapusing 1 %different from thearea measured byK.I. During theIGY(1957–1959),During 2 ), isapproximately a substrate where lichensmay appearinthe only atimeofformation ofarelief form, i.e., sources provide andcartographical historical shouldalsobeconsideredage dating. that It unjustifiably accurate claimedprecision of resultingthe source inan dataaccuracy evaluationof acritical islacking work ouropinion,thisundoubtedly valuable In 1982]. [Golodkovskaya, slopemorainesdating ofthesouthern appeared to beunacceptablefor age slopeoftheCentral Caucuses the northern growth. Thus, dataongrowth obtainedfor of environmental conditionsonlichen demonstrated theinfluence These efforts 1981]. radiochronological [Golodkovskaya, methods, e.g., historical, or cartographical, sites; usingother theageisdetermined using lichensfrom different age-control its growth substrate. This isachieved by ofage thallus diameter asafunction amaximallichenmodel thatdescribes Beschel’s ideasto establishamathematical given to methodological research builton shouldbe difficult. Specialimportance widescaleapplicationofthismethod makes specific region isthemainreason that for each suchdependency determining Challengesof used for proper age-dating. for different lichendiameters have to be means thatdifferent annualgrowth values the growth rate decreases. Practically, this environmental conditions, which after reaches itsmaximaldiameter for given the middleofgrowing tilllichen cycle the speedishighbecomingconstantin different thebeginning speeds. ofgrowth, In through theirlives, lichenthallusgrows at R. Beschel[Beschel, 1961]believed that The founder method ofthelichenometrical millennium andmiddleoftheXIXcentury. maximum limitsoftheglaciationinlast Lichenometrical methodofdeterminingthe a100-yearshappened during time-period. in theglaciationchanges, whichhave to studytendencies a uniqueopportunity provided photographic1997 aerial survey RESEARCH METHODS

19 GEOGRAPHY 20 GEOGRAPHY mudflow andfluvioglacialsediments with Besides, threeinterval. sites withtheancient moraines withinthe1930s to 1850age sites (insixglacialvalleys)onthestadial 1909 to 1979were usedtogether with14 descendfromsediments withknown Twenty five control sites onmudflow were processed. a hundred of1400–2000 melevationsites the valleysofPreelbrus’e withinwhichover Overall, there were 20mudflowbasinsin widely usedinourresearch ascontrol sites. advantage ofbeingeven-aged, were which compared to icehave acertain Along withthemoraine, mudflowdeposits, the lastcentury. Baksan riverbasinglacierschangesduring method wasappliedto studytheElbrusand Specificallythisvery age determination. aprobabledeviations characterize error in of agiven size canbedetermined. These from themeanvaluesofannual growth may this case, beapplied. deviations In with different environmental conditions annual lichengrowth datafrom control sites specifically, a statisticalprocessing ofthe Then, asimplifiedsolutionispossible, i.e., that are withinthelimitsoftheseerrors. conditions may result indatingdifferences for thesites withdifferent environmental end, differences intheannuallichengrowth also reasonable to concludethatatthe applied to dataprocessing. Therefore, itis despite any reliable mathematicmodels level ofconfidence more orlesssatisfactory with period, onecanonlydate to acentury dating. Forlast century a thousand-year datingerror for the may bea decade-long facts, itisreasonable to concludethatthere 1500–2000 years). allthese Considering temperate climate (according to Beschel, limited life spanoflichensgrowing under Such inconsistencies may bearesult ofa diameters oflichensthatgrow onthem. theageofbouldertrainsand between especially careful to exclude inconsistencies several thiscase, decades. onehasto In be related to oldercontrol sites may comprise future andatdifferent times. Datingerrors quantitatively express thistendency. order In datadoesnotallowoneto lack ofactual elevation noted by V.I. Turmanina [1971].A fast increase inthegrowth below2000m However, to there inreality a isatendency the growth rates andabsolute elevations. changesin between is nocleardependency elevations inthe1800–2000minterval. There growth values correspond to theabsolute datausedto obtaintheannual The actual obtained. thecredibilityofresultswhich confirms graph (diameter ofabout100mm)coincide, datingforcarbon arespective pointonthe the sedimentsageanderror oftheradio- The valuesofthemean-root-square error of their formation. than10years after sediments notearlier was assumedthatlichensinhabited the It values ofthemean-root-square error (year). data onthesedimentsageandabsolute growth dataare supplemented withthe possible standard deviation.Also, theannual annual growth valuesare presented witha presented inatabularformat 1). (Table The growth values. For convenience, thisgraph is oftheannual allowed assessingreal accuracy The upperandlower enveloping curves growth average valuesfor different diameters. wasdrawn usingtheannual generalized curve and Zolotarev, 2001]. The annualgrowth different environmental conditions[Seinova the annuallichengrowth wascompiledfor Based onthesedataageneralized graph of stabilized andwas0,15–0,11mm/year. and bigger, theannualgrowth haspractically beginning from thediameter ofabout100mm first decadesoftheirlives (to 50years); andd) annual lichengrowth the occurred during declineinthe lichens was1mm;c)asharp than 10years; b)theminimalvisiblesize of lichens were found onthedepositsyounger through processing ofthesedata:a)no The following dependencieswere established data “IGAN-747” were used. etal. 1973]andourdating 1971; Kotlyakov etal. datingdata[Kaplin radiocarbon known Table 1.Annualgrowth ofdiff growth graph (see Table 1)addingabsolute to onthe usethelower enveloping curve on absolute elevations)itseemsfeasible data ofouractual (the middleoftheinterval to date thesedimentslocated above 2300m ihndaee,m Ana rwh mAge ofdeposits, yrs Annualgrowth, mm Lichen diameter, mm deposits for the northern slopeoftheCentraldeposits for thenorthern Caucasus (absolute elevations 1800–2900m) 0 ,020 Ic. III-IIc. IVc. Vc. VIc. 2000 VIIc. 1900 VIIIc. 1650 1550 X–IX c. XIc. 1450 XIIc. 0,10 1360±150 XIIIc. 0,10 1200±140 0,11 1000±130 0,11 900±120 XIVc. 0,11 820±110 0,12 760±100 200 700±90 0,12 190 0,13 180 0,13 666±80 170 0,14 160 0,14 150 0,15 140 130 0,15±0,01 120 112 110 105 100 95 0,16 ± 0,02 570 ± 70 XV c. XV c. XVI c. XVII 570±70 500±60 420±55 c. XVIII 360±50 330±45 0,16±0,02 290±40 0,18±0,03 240±35 0,20±0,03 210±31 XIXc. 0,22±0,03 180±29 0,23±0,04 160±26 0,25±0,04 95 140±23 0,27±0,05 90 120±18 0,29±0,05 85 100±15 0,31±0,06 80 80±12 0,33±0,06 75 60±10 0,34±0,07 70 45±7 0,37±0,07 65 30±5 0,39±0,08 60 20±2 0,43±0,09 55 0,47±0,10 50 0,55±0,11 45 0,65±0,12 40 0,78±0,11 35 30 25 20 15 10 0XX c. 10 15±1 1,00±0,10 – 5 2–121 erent sized geographicum lichenRhizocarpon anddating oftherespective on maximaldiameters of Using datafrom publishedsources values. values ofthestandard deviationto theage Rhizocarpon

21 GEOGRAPHY 51 71 1930th 14 17 15 15 22 GEOGRAPHY Table 2. The ageofthestadialmoraines oftheriver Baksanvalley glaciersidentifi Fig. 8.ChangesintheElbrusglaciation century. from theend oftheXVII 1–area ofice that melteddur- oso zuMliAa eso rkYsniDhnat Bashkara Dzhankaut Yusengi Irik Terskol MalyiAzau Bolshoi Azau ing 1700–1887;2–lava; 3–glacialdivides. Glacierboundaries:4–1987, 5–1957,6–1887,7–stadial Maximal diameter oflichens(mm)onthestadialmoraines intheglaciersvalleys 43 03 23 01880th XIXc. Mid c. EndofXVIII 30 21 33 41 20 32 40 50 33 40 24 50 30 40 51 21 34 20 34 38 50 method. 66 64 End of XVII c. EndofXVII 64 66 1 2 XIIIc. 125 115 58 08 First c. halfofXV 80 90 85 85 moraine lineofthemid. XIXcentury. 11910th 21 ed with the lichenometry ed withthelichenometry Time offormation of themorainic ridges XVII andmiddleXIXcenturies attheend ofthe Elbrus glaciationboundaries the stadialmorainesallowed the determining of The results survey ofthelichenometric magnitude inthemiddleofXIXcentury. retreat, hascomebackto almostthesame some andafter century mid oftheXVII Caucasus hasreached itsmaximuminthe millennium ADinthisregion oftheCentral theglacialtioninsecond their surface, the endmorainesandlichensize on glaciers. Judging of bythemorphology advancing was interrupted byperiodically millenniums thelasttwo glaciation during suggest thataconsecutive declineofthe general, thedatafrom1971]. In Table 2 lichen growth of0,3mm/year [Turmanina, basedonthedataannual century XVII tomoraines hadbeendated themid earlier these For andBashkara, theglaciers Djankaut state ofthestudiedglaciers. of thestationary apparently formed thelongestperiod during the greatest relative elevation,andwere lines were well visibleintherelief, have seven studiedglaciers. The endmoraine of 85–90mmwere found nearfive outof The endmorainelineswithlichendiameters elevation). tongueto oftheglacial(2540m themodern sideofthevalleyin1km deposits oftheleft valley –amidsttheavalanche andscree (2400 melevation)andintheriver Terskol to thetongue oftheBechoglacial 2 km frontal apron valleysidein neartheright river Yusenga, thismorainetowers over the infragments asremnants.preserved the In lichen diameters of115–120mmwere published literature. The moraineswith noted previously –thefact inpreserved represented mostfully. They were well stadialmoraineswere of theXIXcentury As shownin Table 2,themiddleandend 2). glaciation wasobtained(Table ElbrusandBaksanriverin thesouthern the following representation ofchanges supplemented withourownobservations, 1971] moraine ofseveral glaciers[Turmanina, geographicum lichengrowing onthestadial (Fig. 8). T heir computers). Let usreview indetaila (developed alsofor personalpackages photogrammetric computer software withthehelpofdigital is performed Processing ofdigital photographic pairs orphototheodoliteaerial surveys. through scanninganddigital “digital imagery”, thatisobtainedinAlpine imagery. This stageisassociated with processing ofground, aerial, andspace bydigitalis characterized photogrammetric research state incartographic The modern an exampleofsuchmaps. as 000 scaleElbrusglacialsystem mapserves of thematicmaps. The aforementioned 1:10 analysesandcompilation in cartographic asabasisfor largeserved scalemapsused glaciers. The results of thedataprocessing used to capture spatialpositionsofmountain werephototheodolite commonly surveys the XX century, stereo-autograph processed and aerialphotography. photogrammetricDigital processing ofground 3). elevation (Table glaciers tongues from theirendsto 4000m elevation andicevolumes ofallElbrus allowed changesintheaverage determining models the estimates thesetwo between data for eachglacier. The difference in digital modelswere developed from these the 1957topographic map. Multitemporal together withrespective sites shownon the mapswere compiled anddigitized the upperlevel ofthestadialmoraine, Thus, for eachglacierfrom itstongue to andmiddleoftheXIXcenturies. of theXVII the areas occupiedbytheglaciersatend contour linesfrom elevation for theridges ofthe was accomplishedbyinterpolation theirmaximumdevelopment.during This identify thearea andvolume oftheglaciers symbols. cartographic The mapwasusedto the stadialmorainesare shownwithspecial of whereallridges practically 1957 survey of theElbrusglaciationcompiledfrom the (1:10 000),10mcontour topographic map identification wasbasedonalarge scale Untiltheendof

23 GEOGRAPHY 24 GEOGRAPHY Table 3.Changeinthearea andvolume oftheElbrusglaciation beginningfrom themid. XIXc. stereo modelsandcontour digitizing during model pointsets;stereo editor for editing measurement ofparallaxes anddigital relief bundle adjustment;programs for automatic images; programs for photogrammetric for coordinate measuring pointsondigital components: program stereocomparator which includesthefollowing main we developed for apersonalcomputer, that package photogrammetric software data. The mapwascreated using adigital compiled from photographic the1997aerial the glaciersusingadigital Elbrusmap digital methodappliedtocartographic glaciation Elbrus Total for 2 lua ,5 ,8 ,2 ,6 ,4 ,6 ,5 ,4 ,4 0,144 0,146 0,141 0,151 0,160 0,469 0,697 1,440 0,517 0,769 1,561 1,067 №№ 1–9 0,479 0,700 0,168 Clif glaciers 1,233 1,620 0,561 0,826 0,196 yube 1,174 0,621 1,882 15. Bityukt- 0,832 0,196 1,405 4,689 tlyu 3,950 6,975 0,256 13. Kyukyur- 1,425 4,744 6,901 0,260 12. Ullukam 10,671 4,911 1,680 6,988 10,763 Azau 11. Bolshoi 5,781 10,995 1,735 7,818 0,548 12,425 Azau 6,321 1,806 8,428 10. Malyi 12,605 0,595 2,816 9. Garabashi 0,552 1,230 8. Terskol 3,006 0,605 1,318 7. Irik 0,610 1,227 6. Irichkat 5,485 1,269 kez 5,538 Dzhikiugan- 1,589 5. Icefi eld 5,748 12,301 4. Mikelchiran 12,277 5,918 derku 12,124 Ullumalien- 6,638 + 3. Ullu-Kol 12,944 13,914 2. Karachaul 1. Ulluchiran elevation) 5200 m (area above Elbrus peaks of glacier Name 8018 9717 9715 87195719791997 1887 1850 1997 1979 1957 1887 1850 3122,6 1022,7 0403202902302222,046 0,836 2,222 0,913 2,330 0,866 2,900 0,974 3,270 1,074 20,460 8,363 20,677 8,508 21,032 22,662 8,806 2,558 23,102 3,032 9,826 3,207 10,256 4,339 4,929 25,581 27,295 29,042 31,762 34,832 ,5 ,7 ,9 ,5 ,8 ,3 ,5 ,9 ,0 0,378 0,407 0,221 0,390 0,231 0,450 0,691 0,221 0,530 0,700 0,251 3,783 0,696 0,254 4,058 0,747 2,212 0,752 5,395 1,997 6,913 7,475 2,170 7,226 8,450 2,330 7,039 2,560 7,269 8,119 0,460 0,503 0,479 0,488 0,607 0,439 0,613 0,412 4,604 0,475 4,670 0,481 0,481 4,882 4,834 0,480 4,960 5,564 0,470 5,186 6,014 0,480 5,826 0,480 6,146 4,811 4,818 4,818 4,818 4,818 5,5 4,1 3,1 2,2 2,51,8 62613,540 16,296 17,880 124,85 127,728 132,514 147,516 159,159 Area ofglaciersinhorizontal projection, km projection, 3 of imagesandcomputation ofspatial The elementsfor relative orientation photogrammetric scanner. photographs scanning oforiginal aerial ona was obtainedbeforehand through imagery Digital and compilinganorthophotomap. pointsfor measuring phototriangulation, DEM, processing control includedmeasuring points, imagery. Photogrammetric of orthographic a digital elevation model(DEM)andcreation shutter glasses;andaprogram for building a personalcomputer monitor usingLCD visual interpretation ofthestereo modelfrom Volume ofglaciers, km 3 13,741 12,482 important for assessingtheirvolume changes. important ofglaciers elevations is Monitoring surveys. Adjustment ofmultitemporal dataofrepeated (Fig.included intheboundaries 9). (as itwasconsidered to bestagnant) were previously shownonthe1957–1959map covered bythemorainemantleandnot ends oftheglacierstongues icethatisentirely 1968] were alsoapplied. Additionally, the glaciation..., the Elbrusglaciationmap[The thecompilationof during and ofCartography of theDepartment for Aerospacein theLaboratory Methods The interpretation methodsdeveloped theirdetaileddelineation. which permitted to approximatelystereo-editor 1:5000scale, examination oftheimagesenlarged with from visualinterpretation andstereoscopic wereThe glaciationboundaries defined orthotransformation. imagery perform DEM wasusedto buildcontours andto processed. the entire territory The obtained There were about1mlnpointsintotal for automated processing ofeachstereo-pair. measurement results usingstereo editor after throughselected visualexaminationofthe all DEMpoints. The rest ofthepointswere methods thatwere appliedto obtain96%of the usageofautomated stereo-measurement building adetailedelevationmodeldictated ofalarge numberofpointsforselection relatively images. oriented of The necessity sets were definedwiththestereo-pairs on data asanintermediate step. The DEMpoint The relief mappingwasdoneusingtheDEM interpreted glacierboundary. relief represented by10mcontours, andan images ofthearea;resolution orthographic mapwerecompiled orthographic the1m The baseelementsofthecontent ofthe for compilationofa1 : 10 000scalemap. coordinate sufficient measurement accuracy allowed reaching 1,5mhorizontal andvertical the entire photographic aerial area, which using alarge numberofcontrol pointsover defined basedonblockphoto-triangulation coordinates ofmeasured pointswere associated withtechnical capabilitiesof This laborintensive methodand itslimitations 1957–1987[Zolotarev,glaciers during 1997]. towas conducted identifychangesintheElbrus methods.precisely Such work thancartographic elevationchangesmore allow determining elevation changes. Bothversions ofthismethod of the reconstructionofacontinuoussurface but theyaresuch interpolation, preferable for nodes ofaregular grid, oncontrary, require Measurementsinterpolation. basedonthe relief at contours eliminates amap-based over Pointing astereotick mark modelsurface. while simultaneouslypointingastereograph over amapcontour or anodeofregular grid by pointingacoordinatograph finderdevice Measurements werefrom surveys. made earlier were using mapscompiled oriented survey this method, thestereo-pairs from repeated based photogrammetric instruments. Under multitemporal dataadjustmentusingbroad- of intermediate mapsrequired applying data from withoutcreation repeated surveys of measurements ofchangesbyusing raw together withtheneedto improve accuracy photography istimeconsuming. This fact glaciers withphototheodolite dataoraerial material. However,cartographic mappingof to measure elevationsonmultitemporal methodsare traditionallyused Cartographic Fig. 9.Fragment ofthe1 : 10 000scaledigital ortho mapofElbrus(1997)(reduced size).ortho

25 GEOGRAPHY 26 GEOGRAPHY retreat. V.I. 1967]estimated [Kravtsova, Kravtsova or,stability incontrast,ofitssubstantial provide evidenceoftheglaciation relative a 100-yearvolumes during could period because theassessmentofchangesin interesting Elbrus glaciationisparticularly The assessmentofthetotal volume ofthe coordinates isreached. planimetric inapointwithnecessary surface are adjusted anditspositionattheglacier orientation. Thus, coordinates thetickmark under specifiedparameters ofexternal stereoscopic onto aglaciersurface tickmark and real pointingofa spacedirectlyduring coordinates interconversion images between directly to acomputingsystem andconduct transfer valuesofmeasured imagecoordinates became possiblewithstereocomparators that system. The implementationofthismethod coordinate grid nodeswithinaplanimetric the locationofpointsmay betiedto regular necessary,application ofanalyticalmethods. If provided by substantially higheraccuracy without intermediate witha interpolations change inapointare obtained directly thiscase, thevaluesofelevation 1996]. In coordinates [Zolotarev andKharkovets, with previously establishedplanimetric of thestereo-pairs –atthesamepoints coordinatedconducting measurements surface. actual The solutionwasfound in analytically differs substantiallyfrom the ofchanges obtained appears thatthesurface ofmeasurements.increase theaccuracy It measured stereo pairs, didnotsubstantially detalization obtainedfrom independently linesorsomeotherways ofspace structural andusing network or someotherarbitrary pointsonaregularestablished thatselecting stereo hasbeenexperimentally pairs. It of theDEMsdeveloped from multitemporal changesthroughdetermine thecomparison There have beenseveral attempts to processing.to analytical methodsofimagery transitioning thatdetermined the mainfactors repeated imagesandmapsadjustmentsare DIFFERENT PERIODS OF ITS EVOLUTION GLACIATION VOLUMEDURING ASSESSMENT OF THE ELBRUS the Elbrusglaciationvolume at6km at approximately 12,5m the glaciationin1997canbethenestimated is possiblyaround 100m,andthevolume of for theentireice thickness Elbrusglaciation two, approximately. meansthattheaverage It in 1957were underestimated of byafactor the results ofassessmentstheicethickness plateau, indicated thatfor theDzhikiugankez The assessmentofthevolume ofmelted ice slopeshould beeven greater.on thenorthern 200 m[Rototaeva etal., 2003]. The icethickness icecapewas90m,sometimesreaching the firn Academy ofSciences, of theaverage thickness of Geographyexpedition oftheInstitute ofUSSR Caucasian obtained in1987–1989bytheNorth andBolshoiAzau) Azau, Malyi Garabashi, slopeoftheElbrus(theglaciers the southern andradiosounding dataat Based ondrilling dataforthe actual someglaciationsites. possible to compare theseassessmentswith was estimated at50m.Atthepresent time, itis oftheicefor average theentire thickness Elbrus 100 malongtheaxes ofthelarge glaciers. The icecapwas20–50 mandreached of thefirn oftheicefor thelargerthat thethickness part the glaciers’ valleysprofiles. wasassumed It elevations anddepthofclefts, andanalysisof oftheicecliffs of phototheodolite surveys theIGYfrom compiled during theresults thatwas a mapoftheElbrusicethickness topographic map compiled by the Laboratory topographic mapcompiledbytheLaboratory 18 years. We digitized a1 : 10 000scale 22and approximately even time-intervals: dates: 1957,1979,and1997,thatform two glaciation evolution isbasedonthree fixed The assessmentofthepostIGYElbrus to disappear.unlikely the nearest centuries, the Elbrusglaciersare losses itisreasonable to concludethatduring glaciation volume andiceannualaverage From oftheestimates ofthe comparison decreased byabout22 % (or0,2peryear). thelast110years,during theglaciationvolume km AND THEIR ACCURACY ASSESSMENT GLACIATION EVOLUTION DIGITAL MAPS COMPILATION OF THE POST IGY ELBRUS 3 for 1957and1887,respectively. Therefore, 3 ; and at 13,6 и 16,2 ; andat13,6и16,2 3 using using error of changes in the glaciation surface error ofchangesintheglaciationsurface 1966]. Therefore, arelative measurement measurements errors [Reference Book..., zero, asfollows ofrandom from theproperties points, thealgebraicsumoferrors tends to entire area oftheglaciationinatleast1mln measurements were withinthe conducted maps andphotographs. Becauseelevation from 20contour pointsrecognized onthe multitemporal modelswas2,5mcalculated oftheses thesuperimposition during errorsstandard horizontal andvertical models comparison. The maximalpossible points, whichsubstantiallyfacilitated the controlcoordinate system andsurveying three modelswere compiledusingthesame All for eachofthetime-intervals. surface andelevationoftheglaciation boundaries changesinthe maps allowed measuring glaciation. oftheseThe superimposition we created digital modelsfor theentire 1997. As a result, for eachofthedates photographicaerial datafor 1979and the IGY. addition,we digitally In processed Faculty ofGeography oftheMSUduring andGeoinformaticsof Cartography ofthe for Aerospace oftheDepartment Methods 2 –Karachaul, 3–Ullukol andUllumalienderku, 4–Mikelchiran, 5–Dzhikiugankez, 6–Irikchat, 7–Irik, Fig. a)1957–1979 10.Changesintheelevation ofElbrusglaciersduringtheintervals: ofthesurface within the1957boundaries, b) 1979–1997withinthe1979boundaries. Glaciers:1–Ulluchiran, 8 –Terskol, 9–Garabashi, 10–MalyiAzau, Azau, 11–Bolshoi 12–Ullukam,13Kyukyurtlyu, 14 –Bityuktyube. algebraic summationofΔ the digital models of1957and1997by independent methods, i.e., of bycomparison were1957–1997 period obtainedusingtwo (Δ thatthevaluesofchangesinthickness the fact discussions, inourcase, by were supported elevations canbeignored. T and 1979–1997. In theidealcase, Δ and 1979–1997.In for in1957–1979 thecorresponding periods based on interpolation ofscatteredbased oninterpolation points. elevation andavoiding errors indigital models a detailedpictureofchanges inthesurface from 10mcontours. This allowed obtaining topographic map, inthiscase, wasdigitized should benoted,estimates. thatthe1957 It order ofmagnitude compared to theinitial ofmeasurementsend result byan accuracy large volume ofmeasurements increased the glaciation volume was1,8%. Thus, thesufficiently 2,6 %.Asimilarerror ofmeasurements for the elevationat error for theentire glacialsurface This allowed usto definearelative measurement for eachoftheglaciersandentire glaciation. reality, we hadto dealwithadiscordance (δH) ofmultitemporal models,superimposition in Δ H H 2 ) and volumes of the glaciers during the ) andvolumesthe oftheglaciersduring , however, dueto errors associated with H 1 andΔ hese theoretical hese theoretical H H =Δ 2 values values H 1 +

27 GEOGRAPHY 28 GEOGRAPHY eraei lvto ftesrae /r0500300,320 0,350 0,530 Decrease in volume, km Decrease inelevation of thesurface, m/yr (1979–1997), auniversal decrease inthe ofobservations thesecondperiod During Elbrus glacierswere advancing[Panov, 1993]. the1960s[Kotlyakov,during 1994]whenthe Hemisphere temperatures oftheNorthern aresultwas clearly ofthetotal decrease inair at +0,94mofwater equivalent. The process assessed entire thisperiod glaciationduring resulted inalowpositive massbalanceofthe slopeoftheUlluchiranglacier.northern This prevailed reaching 40matthe in thesurface oftheglaciation,increase south-western part andHotyu-Tau part in itsnorth-eastern inthe Plateauglaciers except for theDzhikiugankez general decrease inthearea, atalmostall 1957–1979,despite a change periods. In glaciation response climate even for short The compiledmaps(Fig. showthe 10)clearly Table 4.Average annualchangesinthearea, elevation andvolume ofthesurface, oftheElbrusglaciation Decrease inarea, km Fig. 11.Changeinthearea and volume oftheElbrus glaciation for 1850–1997. 1–changeinthe below 4000melevation, for diff aaee 8018 8715 1957–1997 1887–1957 1850–1887 Parameter 2 y ,1 ,1 0,190 0,210 0,310 /yr 3 y ,5 ,3 0,027 0,035 0,058 /yr area, km erent periods 2 , 2–changeinthevolume, km on the two aforementionedon thetwo glaciersofthe 45%ofthisamountfalls ofwater; to 1km3 whichisequivalent has decreased by1,2km3 (1957–1997), theElbrusglaciationvolume 40years theIGY generalduring after In tongues. area was16,8mreaching 40matthe decrease for theentirethe surface glaciation Dzhikiugankez”. Here, theaverage valueof the commonname “Ice Field ofthe and Birdzhalychiran, combinedunder of theglaciationslope–Chungurchatchiran greatest decrease wasnoted attheglaciers insignificant area neartheElbrussummit. The elevationtook place, except forsurface an CONCLUSIONS 3 . 10. Knizhnikov, Yu.F., V.I. A.P. Kravtsova, andS.M.Myagkov. (1984)Changesinthe Martyshev P.A., Kaplin, I.V. O.B. Grakova, Paronin, etc. (1971) ofthe dating,The listofradiocarbon Laboratory 9. N.A.(1982) Golodkovskaya, slopeoftheCentral The dynamicsofglaciersthesouthern 8. ofmorainesandglacierdynamicsthenorth- N.A.(1981)Lichenometry Golodkovskaya, 7. Reserve. N.Ya. Dinnik, andancientglaciersoftheCaucasus. Kakvakzskyi (1890)Modern 6. Climate change–2001. (2001) The ScientificBasis. of Contribution GroupWorking Ito the 5. Burmester, H.(1913)Rezent glazialeUntersuchungen undphotogrammetrischeAufna- 4. bylichengrowth Beschel, anditsapplicationto R.E.(1961)Datingrock glaciology surfaces 3. Altberg, V.Ya. (1928)Onthestate oftheElbrusglaciersinGreater Caucasusrangeof 2. umjahre 1873.Moskau. Abich,H.(1875)Geologische BeobachtungenaufReisenimKaukasus 1. there even decrease hasbeenpractically in (1850–1887).Beginning period in1887, earlier glaciation decrease wasassociated withthe data indicate thatthegreatest rate ofthe These reasonably reliable quantitative of theglaciationtongues 4). (Table and area oftheglaciationwasdueto melting becausethedecrease inthevolume century glaciation retreat thatbeganinthemidXIX 4000 m. allowstracingtherate of This fact the endsoftongues to theelevationof oftheglaciation,specificallyfrom lower part this volume (i.e., 98%)iscontainedinthe slope. of northeastern The majorportion REFERENCES Geography, Russian). №2(In Elbrus glaciationin25years theIGY. after ser. State Bulletin (Vestnik), University Moscow 5, ser. State Bulletin(Vestnik), University Moscow 5,Geography, Russian). №4 (In Faculty ofGeography, oftheUSSR. ofOceanology State andtheInstitute University Moscow Russian). № 45(In ofGlaciological Research,Caucasus inthelast700yearsdata).Materials (Lichenometrical Academy ofSciences., ser. Geogr., Russian). №6(In oftheUSSR oftheCentral macro-slope Caucasusoverern thepast700years. Izvestia Russian Geographical Society, Tiflis, Vol. Russian). 14,№1(In ofIPCC. Press.Third University Cambridge Assessment Report 1. Bd. furGletscherkunde, Zeitschrift 8,Ht. men imBaksanguellgebiet(Kaukasus). oftheArctic,and physiography (lichenometry), Toronto Univ. Press, Vol. 2. Russian). GGI,№22(In basininthe1925–1927 period.the BaksanRiver Izvestia Research (project #10-05-00453a). oftheRussianFoundationsupport for Basic This paperwasmadepossiblebythefinancial anthropogenic causes. was moredueto naturalthan likely theendofLittleIceAgeafter and ofcooling, periods beganinXIXcentury change, whichalternated withshort These datasuggestthatglobalclimate down (Fig. 11). the area whilevolume hasslowed reduction ACKNOWLEDGEMENT 

29 GEOGRAPHY 30 GEOGRAPHY 2 K 12. Kotlyakov, V.M. (1994) The Russian). (In World Moscow ofSnowandIce. Nauka, 11. 2 Zolotarev, Ye,A. and V.V.32. Popovnin. response to climate (2003)OntheglacierDzhankaut World Conference onClimate Change. (2003)Moscow. Abstracts. 31. Tushinsky, (1958)Post G.K. mud-slideglaciationofElbrusanditsdynamics. –Information 30. Turmanina, V.I. usingphyto-indica- (1971)Studyoftheevolution oftheglacierDzhankaut 29. Press. Elbrus. University TheglaciationofMount (1968)Moscow Russian). (In Moscow 28. Solovyev, S.P. (1933)StatusoftheElbrusArea GlaciersandtheQuestionaboutReason 27. EurasiaintheHolocene, Scientific Solomina,O.N. GlaciationofNorthern (1999)Mountain 26. Seynova,I.B. and Ye.A. Zolotarev. (2001)GlaciersandsatElbrus(Evolution ofglaciersand 25. Salatsky, N.D. Re- (1886)Essays onorography andgeologyoftheCaucasus. Kakvakzskyi 24. Rototaeva, O.V., A.B. Bazhev, S.A.Nikitin, G.A.Nosenko, O.A. Nosenko, A.V. Vesnin, and 23. Russian). (In (1966)Nedra,Moscow Reference ofSurveyors Manual 22. Podozersky, Rus- Reserve. (1911) K.I. The glaciersof theCaucasusMountains. Kakvakzskyi 21. Russian Reserve. Pastukhov, A.V. oftheascentElbrusJuly31,Kakvakzskyi (1893)Report 20. Panov, V.D. (1993) CaucasusGlaciation.S.Gidrometeoizdat,The Evolution oftheModern 19. Oreshnikova, Ye.I. (1936)GlaciersoftheElbrusarea based onresearch of1932–1933.Pro- 18. Mushketov. I.V. ofRussianGeo- (1882)Geological to theCaucasusin1881.Izvestia trip 17. A.P. Martyshev, glacierinElbrus. (1980)Fluctuations Materi- ofthetongue oftheBigAzau 16. Labutina,I.A.(1968)Studyofchangesinthesize ofglaciersusingamappingmethod. 15. Kra 14. Kovalev, P.V.13. slopeofthecentralCaucasus. Materials (1961)Onmud-slidesonthenorthern change. ofGlaciological Russian). Research, Materials №95(In Bulletin ontheIGY Works oftheFaculty ofGeography ofMSU, №2. tion methods. ofGlaciological Russian). Research, Materials №18(In for theirRetreat. Russian Geographical Society, Vol. 65,№2. World, Russian). (In Moscow Scientific mudflow activity), World, Russian). (In Moscow RussianGeographical Society,serve. Vol. Russian). 7,№1(In ofGlaciologicalterials Russian). Research, №93(In I.F. Khmelevskoy. (2003) Elbrus. slopeofMount Ma- ofice onthesouthern The thickness sian Geographical Society, Vol. Russian). 29,№1(In Geographical Society, Russian). (In Tiflis, book.15 St. Petersburg Russian). (In Russian). ceedings oftheGlacierExpeditions. Caucasus. (In Moscow graphical Society, V. 18,№2(INRussian). als ofGlaciological Russian). Research, №39(In Press, University Elbrus Glaciation,Moscow Russian). (In Moscow Kharkov, of theCaucasusExpedition.(ProgramVol. Russian). IGY), III(In times.mountainous Caucasusinhistorical ofGlaciological Russian). Research, Materials №21(In otlyak vtsova, V.I. (1967)Ice Map. ofGlaciological Research, Materials No.Thickness Russian). 13(In ov, V.M. V.A. Gerasimov, etal. (1973) Onclimate changeandglaciationin A.L.Devirts, 34. Zolotarev, 34. Ye.A. ofGlaciological (1997)ChangesglaciersElbrusinthelastcentury. Materials Zolotarev, 33. Ye.A. and Ye.G. (1996)Applicationofautomated Kharkovets. mappinganddigital 204 p. (Evolution of Zolotarev) Moscow State University Bulletin (Vestnik), ser.Zolotarev) State Bulletin(Vestnik), University Moscow 5,Geography., 2007,N5. Assessment ofElbrusglaciationsdegradation bydigital methods(coauthor cartography Ye. ofglaciological research1997), Materials (coauthor Ye. Zolotarev) 2000, Vol. 89p.175–181, (A digital mapofElbrus, publications:Elbrusglaciationsattheendof20-thcentury Main formethods ofdigital geographical andphotogrammetry cartography research applications. attheFacultyworking interested ofGeography indeveloping since1987.Heisparticular of Cartography, Faculty ofGeography, M.V. Lomonosov State University. Moscow Hehasbeen Yevgeniy Kharkovets isResearch for Associate Remote Sensing, oftheLaboratory Department Research, № 83 (In Russian). Research, №83(In Russian). 26–29June1996)(In Conference (Irkutsk, GIS for thestudyandmappingofenvironment. Proceedings oftheInternational inElbrusregion. glaciermonitoring for INTERCARTO 2: theDzhankaut glaciation and mudflow activity) (coauthor I.B. Seinova)glaciation andmudflow (2001), activity) Moscow, (2009)238p;Glaciersandmudflows sensing and cartographic methodsofglacialmonitoring, sensing andcartographic publications: Evolution oftheElbrusglaciations:remote catastrophic glacialprocesses inhighmountainregions. Main the fieldofevolution anddynamicsofmountainglaciers hazard inhighmountainregions. research His interests are in Ph. D.His thesis(1979)wasdevoted to mappingofavalanche stationofMSU. 10 years atElbrusMountain helived and worked graduated in1967.For from University Moscow more than Geography, M.V. Lomonosov State University. Moscow He for ofCartography,of Remote Sensing, Department Faculty Yevgeniy Zolotarev, Ph.D. isSeniorScientistoftheLaboratory of the Elbrus region of theElbrusregion

31 GEOGRAPHY