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Quaternary International 190 (2008) 112–122

Pleistocene glacial relief of the central part of Mt. Prokletije(Albanian Alps)

Milovan Milivojevic, Ljubomir Menkovic, Jelena Calic�

Geographical Institute ‘‘Jovan Cvijic’’, Serbian Academy of Sciences and Arts, Belgrade, Serbia

Available online 10 May 2008

Abstract

The central and highest area of Mt. Prokletije (Albanian Alps) is situated in northern Albania and eastern Montenegro (at 421300N).

The highest peak is Maja e Jezerces (2694m). Detailed geomorphological mapping was used to reconstruct the positions of former

glaciers. The longest Ropojana glacier had a length of 12.5 km and surface of 20 km2; others include Valbona Glacier (9.5 km, 10.5 km2),

Grbaja Glacier (5 km, 6.7 km2) and Bogicevica Glacier (6 km, 6.9 km2). Three series of moraines can be distinguished: the lowest at an

average altitude of 990m (average ELA 1750m), the middle series at 1350m (ELA 1942m), and the highest at 1900m (ELA 2123m). As

no advanced dating methods have yet been used to provide a numerical chronological framework for these features, hypotheses are made

based on the comparison with the advanced studies of other similar mountains in the Mediterranean region. The moraines of the first

stage (lowest series) correspond to one of pre-LGM glaciations (Middle or even Early Wurmian), the second stage moraines probably

correspond to LGM, and the third stage could be attributed to Younger Dryas. The mapping included a number of inactive and active

rock glaciers, as well as three small active glaciers (surface 5 ha and less), at 1980–2100m altitude, in the area close to Maja e Jezerces.

r 2008 Elsevier Ltd and INQUA. All rights reserved.

Keywords: Mt. Prokletije (Albanian Alps); Pleistocene glaciation; Recent glaciation; ELA reconstruction

1. Introduction

Mt. Prokletije (also known as the Albanian Alps orBjeshket e Nemuna) is situated in southeastern Europe,between the Dinaric Mountains and the Pindus Mountains,spreading across three countries: Albania, Serbia (Kosovo)and Montenegro. The highest part of Mt. Prokletije issituated in northern Albania, close to the border withMontenegro, where several peaks exceed the altitude of2500m a.s.l. The highest peak is Maja e Jezerces (2694m).The study area is situated between 421250N and 421370N,and 191450E and 201070E. Geographically, Mt. Prokletije isamong the least explored areas on the Balkan Peninsula.Apart from difficult accessibility, the most important factorresponsible for the poor level of exploration is politicalinstability. In the last two centuries, there were very fewperiods when all parts of the area were safe enough forfieldwork.

e front matter r 2008 Elsevier Ltd and INQUA. All rights re

aint.2008.04.006

ing author. Tel.: +381 658215762; fax: +381 112637597.

ess: j.calic@sezampro.yu (J. Calic).

The aim of this study is to reconstruct the positions oflate Pleistocene glaciers in the region of central Mt.Prokletije, and to distinguish different series of moraines,attributable to three glaciations. Suggested hypotheses onglacial chronology in the area will serve as an introductionto the future research and expected use of advanced datingtechniques.

2. Regional setting

2.1. General geological and geomorphological

characteristics

The area of central Prokletije can be divided into twozones, approximately along the line Plav Lake–Maja Sapitpeak (2149m). To the west of this line, the terrain is mostlycomposed of limestones and dolomitic limestones ofMesozoic age (from Lower Triassic to Upper Cretaceous),with some occurrences of carbonate and sandstone flyschand quartz schists (Djokic et al., 1976). The area shown onFig. 6 (rectangle A on Fig. 1) consists completely of

served.

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Fig. 1. Location of the study area. Rectangles A and B refer to Figs. 6

and 8, respectively.

M. Milivojevic et al. / Quaternary International 190 (2008) 112–122 113

limestone and dolomitic limestone with chert nodules. Thearea east of the line Plav Lake–Maja Sapit is geologicallymore complex. Palaeozoic phyllites and argillaceous schistsare locally covered with Permian-Triassic red quartzconglomerates. Further to the east, phyllites are inter-calated with marbles and crystalline limestones, while thearea to the SW and NE from the peak Maja e Rops(2501m) is composed of igneous, mainly granitoide rocks(cataclastic granite) (Antonijevic et al., 1969; Gjeologjia eShqiperise, 1970). A simplified view of lithology of this areais presented as Fig. 8.

The relief is considerably vertically dissected, withelevation differences that reach almost 1800m: Valbonavillage is situated at 920m a.s.l, although the horizontal(orthogonal) distance to Maja e Jezerces, at 2694ma.s.l, isonly 3700m. Palaeo-glacial landforms are dominant in themorphology of the area. Active geomorphological pro-cesses include frost heaving and the associated massmovements, as well as karst process and gully erosion.Frost heaving in the areas composed of limestones leads toextensive rockfall and formation of large screes. In easternpart of the study area, which is dominantly composed ofphyllites with soil cover, frost action is manifested mainlythrough gelifluction. In late spring and summer months,during the intensive snowmelt, this area is subject to gullyerosion, which washes large quantities of material towardsthe local erosional basins: Plav Lake and its outflow, theLim River. Limestone terrain in the region of Maja eJezerces, Mt. Bjelic and Karanfili ridge hosts a typicalglacio-karstic relief. Apart from karstic depressions mod-ified by cirques, there are also post-glaciation dolines andlimestone pavements with karren, as well as typicalcorrosion terraces, studied by Kunaver (1991). Particularlyduring late spring and summer, this area is characterised bydeep circulation of karst groundwaters. Deep karstificationis favoured by high hydraulic gradients, but intensivespeleological explorations (which could potentially lead toobtaining certain palaeoclimatic information from spe-leothem) are still in progress.

2.2. Present-day glaciation in the study area

In Mt. Prokletije cirques above 2000m altitude, whichare situated within ridges of more than 400m of relativeheight, the snow usually remains until autumn. Only invery dry and warm years (e.g. 2007), does the snow meltduring September, which allows direct observation of smallglaciers. On September 15 2007, three glaciers withmoraines and two rock glaciers were detected in the areafrom Maja e Jezerces to the small dividing ridge within thecirque Buni i Jezerces (see Figs. 2 and 3 for glacier featuresand Fig. 7 for position).The largest glacier is 410m long (number 1 in Fig. 7),

with an area of 5 ha (0.05 km2). Its frontal moraine lies at1980m, while the highest parts of the glacier are at 2100m,below a scree slope. Inclination of the glacier surface is notuniform; it has a prominent 15m high step in its upperpart. Four glacial tables are present on the surface of theglacier, two of which are only in the beginning phaseof formation. The average block dimensions are 1.8m�1m� 0.6m, and the height of the ice pedestal is 15–20 cm.Small glacier tables have sediment caps, brought by wind(Fig. 2). The frontal moraine of this glacier is 2.5m high,made of limestone boulders and relatively fine-graineddebris. The light colour of the material indicates that it iscovered with snow during most of the year. In front of thismoraine, there is another one, at the distance of 25m,which is of darker colour and with less fine-grainedmaterial. It is considered that this darker morainerepresents the maximum extent of this glacier during theLittle Ice Age. This glacier is similar in dimensions andaltitude to Debeli Namet glacier on Mt. Durmitor inMontenegro (Hughes, 2007).These glaciers are active despite their position below the

theoretical present-day snow line (which is higher than thehighest peaks in the area). Using the mean annualtemperature of 7.2 1C in Kolasin, Montenegro (situatedat 945m a.s.l.) and a lapse rate of 0.6 1C per 100m, themean annual temperature on the surface of the biggestProkletije glacier (at 2040ma.s.l.) would be +0.6 1C.Applying the same procedure with the starting point inVermosh, Albania (6.7 1C, 1152ma.s.l.; Palmentola et al.,1995), gives +1.4 1C mean annual temperature for theglacier surface. Obviously, these temperatures are too highconsidering the established rule that rock glaciers (and,subsequently, ice glaciers as well) form in the areas wherethe mean annual temperatures do not exceed �2 1C(Barsch, 1978; Hughes et al., 2006c). However, the activityof Prokletije glaciers can be attributed to particularmicroclimatic conditions within deep north-exposed cir-ques, whose surrounding walls are up to 500m high.

3. Methods of study

The basic method applied in this study is detailedgeomorphological mapping of palaeo-glacial features,mostly cirques, moraines and roches moutonnees, as well

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Fig. 3. Glacier tables fallen from the ice pedestals (the glacier is marked

with no.2 on Fig. 7). September 15, 2007.

Fig. 2. Glacier tables on the active glacier in the foothill of Maja e

Jezerces (this glacier is marked with no. 1 on Fig. 7). September 15, 2007.

M. Milivojevic et al. / Quaternary International 190 (2008) 112–122114

as mapping of recent glaciers and rock glaciers. Themapping was done using 1:25.000 topographical mapsissued in the former Yugoslavia, contoured at 10m. Ahandheld GPS receiver and an altimeter were used as well.Mapped positions of cirques and moraines enabled thereconstruction of former glaciers. Reconstructions ofthe equilibrium line altitudes (ELA) were done using the

median-altitude variant of the altitude ratio method(Porter, 2001).According to the definitions of three phases of glacial

landforms studies in the Mediterranean area (observation,mapping, and advanced dating), given by Hughes et al.(2006a), the studies of glaciations on Mt. Prokletije arepresently in the second phase—detailed geomorphologicalmapping of glacial landforms and sediments.

4. Pleistocene glaciation of the study area

4.1. Former research of glaciation in the central part

of Mt. Prokletije

Glacial traces in this mountainous area were first noticedand studied by Jovan Cvijic (1903, 1913), and later byMilojevic (1937), Menkovic (1994), and Menkovic et al.(2004). There is a considerable level of scientific disagree-ment regarding the reconstruction of former glacierlengths. One of the obvious examples of this discord is,on one hand, the report by Cvijic (1913) that the Decaniglacier deposited its front moraine close to the settlementof Decani, at 630ma.s.l, while on the other hand theresearch of Menkovic (1994) places the lowest frontmoraine of this glacier at 1600m a.s.l. Regarding thehighest parts of Prokletije, the Plav glacier, with anattributed length of 35 km, was considered the longestglacier on the Balkan Peninsula. The elevation of itsend moraine was estimated to 900ma.s.l, about 1 kmdownstream of Plav Lake (Cvijic, 1913). Due to poorknowledge of the area where the glacier originated, itsdimensions were considerably overestimated. This issue isexplained in more detail below. Considerations on Wur-mian glaciation in Mt. Prokletije are presented inPalmentola et al. (1995), within a study of inactive rockglaciers.

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Fig. 4. Cirque Dober Dol on southern slopes of Mt. Bogicevica.

Fig. 5. Roches moutonnees in a dry lake in the cirque Buni i Jezerces.

September 15, 2007.

M. Milivojevic et al. / Quaternary International 190 (2008) 112–122 115

4.2. Morphology of largest cirques in the central part

of Mt. Prokletije

The area around the highest peak of Mt. Prokletije,Maja e Jezerces (2694m) hosts three great cirques: Buni iJezerces, Buni i Gropavet, and Llugu i Zajave. Buni iJezerces is the most complex cirque in the area. An Upperand Lower cirque can be distinguished. The Upper cirqueis exposed to the northwest, and the average elevationof its bottom is 2150ma.s.l. Longitudinal inclinationis significant along all its length of 1700m. The upperpart of the cirque hosts one small active glacier and twoactive rock glaciers. In the lower part of the cirque, whichsharply changes direction towards the northeast, there is agroup of glacial lakes, Buni i Jezerces. The lakes areconstantly being filled with great quantities of debris fromnumerous screes. The largest lake, Veliko Jezero, is also thehighest one, at 1792ma.s.l. From field observations andtopographic map analysis, it can be concluded that thesurface of the lake has been reduced by 50% during theHolocene, due to filling by screes. The lowest lake, closestto the outflow rim of the cirque, dried during summer 2007,which revealed several well-preserved roches moutonnees(Fig. 5).

The cirque Buni i Gropavet is exposed towards the west,with considerable longitudinal inclination in the upperpart. Sediments and morphology in the lowest part of thecirque point to the existence of a great cirque lake, whichceased to exist during the Holocene. In the late summer, allsnow patches melt completely.

The cirque Llugu i Zajave is open towards the valley ofValbona. Due to such morphology, all the morainematerial has been washed away from the cirque. Thehighest part hosts two small active glaciers. At the outflowrim of the cirque, there is a 400m high escarpment.

Dober Dol cirque (Fig. 4) is the largest cirque in thestudy area (4.5 km2), situated to the south of Mt.Bogicevica. Its general aspect is towards the NW, but atthe outflow rim the aspect turns SW at 901. The geological

composition (phyllites and schists) resulted in high erosionrates, so all the moraines have been washed away from theoutflow part of the cirque and from the valley downstream.Along the upper part of the cirque, several smaller cirqueswere formed. These cirques are of much smaller dimen-sions, but their moraines (two series) have been relativelywell preserved. The morphology of the valley Llumi iGashit, and comparison with altitudes of frontal morainesof other valley glaciers, indicates that the Dober Dolglacier reached the altitude of 1320m. Morphometriccharacteristics of the cirques are given in Table 1.

4.3. Reconstructions of Pleistocene glaciers

4.3.1. Ropojana glacier

The glacier that started fromMaja e Jezerces towards thenorth deepened the pre-glacial valleys and formed a giantcirque, Buni i Jezerces. Fusha e Runices was anotherglacier, originating from the cirque Buni i Gropavet, to thewest from the peak Maja e Jezerces. The confluence ofthese two glaciers occurred near Zastan, at 1370ma.s.l.The glacier extended through the Ropojana valley (Fig. 9)and is therefore named the Ropojana glacier. There weresome smaller tributaries to the Ropojana glacier: fromsmall hanging cirques on Mt. Karanfili on the north-western side, and one glacier from Mt. Bjelic on thesoutheastern side.Three series of moraines have been noted along the

course of Ropojana glacier. The lowest is Vusanje morainein the village of Vusanje in Montenegro, at 1150ma.s.l.Behind this moraine, there was a lake in the terminalbasin, which has completely disappeared during theHolocene. Moraines of the Ropojana glacier are muchbetter preserved than the moraines of other glaciers in thearea, thanks to favourable geological composition (lime-stones, no surface runoff) and relatively mild longitudinalinclination.The total length of Ropojana glacier, counting from the

cirque Buni i Gropavet to the Vusanje moraine was about

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Table 1

Morphometric characteristics of cirques in the central part of Mt. Prokletije (numbers in the first column correspond to those marked on Figs. 6 and 8)

Cirque Orientation Width (m) Length (m) Minimum altitude

of bottom (ma.s.l.)

Maximum altitude

of bottom (ma.s.l.)

Buni Jezerces (upper) NW 500 1400 1980 2300

Buni i Jezerces (lower) NE 800 2000 1750 1900

Buni i Gropavet NW 1400 2750 1760 2350

Llugu i Zajave NE 1100 1300 1880 2350

1 NE 550 950 1520 1600

2 NE 650 1300 1900 2250

3 N 250 300 1950 2120

4 NW 300 500 1840 2200

5 N 330 420 1600 1700

6 NW 450 750 1800 2000

7 NW 400 500 1700 1900

8 E 340 650 1650 2000

9 SE 400 320 1700 1900

10 SE 300 450 1700 1900

11 SE 450 500 1900 2100

12 NW 450 1050 2000 2200

13 NW 300 400 1900 2100

14 E 300 350 2050 2150

15 NW 350 550 2050 2200

16 SE 350 450 2020 2200

17 NE 550 1550 1970 2160

18 NW 350 450 1780 1840

19 NW 500 550 1700 1900

20 SE 650 2000 1880 2300

21 E 300 400 2200 2300

22 E 550 500 2150 2320

23 E 450 700 2100 2200

24 NW 500 450 2180 2300

25 NW 900 1300 1980 2300

Bogicevica N 1800 2000 1800 2150

Dober dol NE 2000 3300 1800 2200

26 NW 400 400 2000 2120

27 N 450 500 2080 2200

28 NE 230 350 2000 2100

29 N 250 250 2050 2120

30 N 550 800 2000 2100

31 NW 1100 500 2080 2200

M. Milivojevic et al. / Quaternary International 190 (2008) 112–122116

12.5 km. This was the longest Pleistocene glacier onMt. Prokletije, with a maximum area of 20 km2.

Clastic material which is deposited as an alluvial fanabout 1 km downstream from the Plav Lake (Fig. 1) hasbeen considered a frontal moraine of the Ropojana glacierfor almost a century. In the literature, this is known as thePlav glacier and was thought to be 35 km long (Cvijic,1913). Its longer tributary came from Vermosh valley inwestern Prokletije, while the shorter tributary was fromRopojana valley. The latest research has shown that thereconstruction of Plav glacier was based on erroneousestimations, due to lack of field evidence.

Detailed field research of the area showed the mistakes indetermination of origin of the clastic deposits in the vicinityof Plav. According to the size and roundness of particles, itis obvious that this material was accumulated by the riversKomaracka Reka and Babinopoljska Reka, transportedfrom Mt. Bogicevica in eastern Prokletije. The geologicalcomposition also indicates that the material consisting of

Palaeozoic schists cannot be transported from the area ofMaja Jezerces, simply because there is no such formationthere. On the slopes of Mt. Bogicevica, in the valley ofBabinopoljska Reka, numerous gullies are incised inPalaeozoic schists. The large accumulation of clasticmaterial, with more than 50m of relative height, whichwas earlier considered to be the end moraine of Plav(Ropojana) glacier (Cvijic, 1913), is an alluvial fan thatoriginated from the area of Mt. Bogicevica and depositedby the River Babinopoljska Reka.

4.3.2. Valbona glacier

From the cirque Llugu i Zajave, a glacier extendedthrough Valbona valley, down to the village of Valbona(Fig. 9). Sides of the glacial valley are almost vertical 2 kmupstream from Valbona. This leads to the conclusion thatthe thickness of the glacier was at least 50m, and that theupper rim of the vertical part can be regarded as a trimline.Vertical sides do not exist downstream from Valbona

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Fig. 6. Glacial features in the area of Maja e Jezerces. Rectangle C refers to Fig. 7. Numbers in cirques correspond to those in Table 1.

M. Milivojevic et al. / Quaternary International 190 (2008) 112–122 117

village, indicating that the moraine close to the village, at900m a.s.l., is the end moraine of the maximum advance ofValbona glacier. Most of the moraine has been eroded bythe Valbona River. In the downstream direction, the valleyfloor altitude decreases abruptly to about 500ma.s.l., sothe existence of the glacier was not possible downstreamfrom Valbona, regardless of favourable conditions in thearea of ice accumulation. The Valbona glacier was never-theless one of the longest glaciers of Mt. Prokletije, with alength of 9.5 km and surface 10.5 km2. It was fed also by anumber of hanging cirques, the greatest of which was onMt. Bjelic.

4.3.3. Grbaja glacier

Grbaja valley is parallel to the Ropojana valley, alongthe northwest side of Karanfili ridge. In the phase ofmaximum glaciation, the Grbaja glacier covered an area ofabout 6 km2 and was 5 km long. Apart from the two maincirques (Fig. 6), the glacier was fed by four lateral hangingcirques situated on Karanfili ridge (2200m averagealtitude). The ridge on the left side of Grbaja valley is atmuch lower altitude (1850m average), and no cirques wereformed in it. Due to steep inclinations and related massmovements, in three out of four Karanfili cirques nomoraines are preserved. The height difference betweenKaranfili cirques and the bottom of Grbaja valley is600–850m. The 35m high front moraine of the maximum

extent of Grbaja glacier is situated at 1020m elevation,close Skala (Fig. 10(3)).

4.3.4. Bogicevica glacier

Mt. Bogicevica is situated in the eastern part of the studyarea. Apart from the main Bogicevica glacier, originatingfrom Bogicevica cirque and extending to Babino polje inthe valley of Babinopoljska Reka, there were two moreglaciers. One started from the great cirque Dober Dol andcontinued through the valley Llumi i Gashit (no endmoraine is detected), and the other moved northeast,through the valley of Decanska Bistrica in Kosovo(Menkovic, 1994). The last mentioned glacier is notincluded in this study.This area differs geologically to a considerable extent

from the area around Maja e Jezerces. Rocks prone tofluvial erosion are dominant (phyllites, schists), whichconsiderably influences the general morphology. Bogicevi-ca cirque is oriented northwards, and is characterised byintensive gelifluction. No traces of moraines are recogniz-able in the field. In three tributary cirques (numbers 26–28on Fig. 8) recessional moraines have been preserved in thezone between 1950 and 2000m. They consist of largequartz conglomerate blocks (average dimensions 9m3).The maximum length of Bogicevica glacier was 6 km. Itdeposited a 20m high end moraine at the altitude of 1560m(Fig. 10(4)).

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Fig. 7. Detailed geomorphological sketch of the cirque Buni i Jezerces.

M. Milivojevic et al. / Quaternary International 190 (2008) 112–122118

5. Discussion

5.1. Pleistocene equilibrium line altitude (ELA)

Three series of moraines can be distinguished in thestudy area. Median-altitude variant of the altitude ratiomethod (Porter, 2001) was used to determine the equili-brium line altitudes (ELA) for each of the defined moraineseries.

The lowest moraines are at 920m a.s.l. and belong to theValbona glacier. The matching moraines of Ropojanaglacier are the Vusanje moraines (1050m), those of theGrbaja glacier are the Skala moraines (1020m; marked asMG1 on Fig. 6 and shown in Fig. 10(3)), and the endmoraines of Bogicevica glacier at 1560m (Fig. 10(4)). Thisseries of moraines represent the dimensions of glaciersduring the maximum glaciation. The average ELA for thisglaciation is 1750m.

The second series of moraines, at Zastan (1350m; Buni iJezerces branch of Ropojana glacier), Fusha e Runices(1300m) and in Dober Dol (1950m) indicate an averageELA of 1942ma.s.l. The third series of moraines isrepresented by recessional moraines accumulated at out-flow areas of large cirques. Behind these moraines, thereare large quantities of material left from cirque glaciers androck glaciers. Elevations of recessional moraines are the

same (1800m) in three great cirques: Buni i Jezerces, Buni iGropavet and Buni Retit Bard on Mt. Bjelic. The averageELA was at 2123m a.s.l.An overview of moraine series altitudes and the

corresponding equilibrium line altitudes is presented inTable 2. In each particular phase, the strongest glaciationtook place in the zone of the peak Maja e Jezerces and thesurrounding ridges Karanfili and Bjelic. Another zone, onMt. Bogicevica, was considerably less glaciated, with ELAsthat are about 200m higher than in the Jezerces area.Bogicevica is situated at lower altitudes. Furthermore,ridges around the cirques are of smaller relative height thanin the Jezerces area. Another interesting reason for muchhigher ELAs on Mt. Bogicevica is the smaller quantity ofprecipitation: it is situated 20 km to the east from thedirection of wet air masses from the Adriatic Sea. In thearea between the Adriatic and Maja e Jezerces there are nobarriers for wet maritime air masses.

5.2. Correlation with neighbouring mountains

Glaciations of Mt. Prokletije may be compared, in extentand chronology, with similar events on other mountains inthe Mediterranean region. Mt. Prokletije is situated atalmost the same latitude as the Appenines, mountains onCorsica, and Mt. Sara, but correlations can be made also

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Fig. 8. Glacial features in the area of Mt. Bogicevica. Numbers in cirques correspond to those in Table 1.

Fig. 9. Glacial valleys in Mt. Prokletije: (1) Ropojana valley and (2) Valbona valley.

M. Milivojevic et al. / Quaternary International 190 (2008) 112–122 119

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Fig. 10. Some of the significant moraines of Mt. Prokletije: (1) moraine in the cirque Buni i Jezerces (marked as MB3 on Fig. 7; 3rd series; view towards

SW); (2) moraine at Zastan, Ropojana valley (marked as MR2 on Fig. 6; 2nd series; view towards NW); (3) end moraine of the Grbaja glacier at the

location Skala (marked as MG1 on Fig. 6; 1st series; view towards SW); (4) front moraine of the Bogicevica glacier (marked as MB1 on Fig. 8; 1st series;

view towards NW).

Table 2

Altitudes of glaciers (terminus and head) and corresponding ELAs in various glaciations (from maximum to minimum glacier extent; in metres above

sea level)

First glacial event Second glacial event Third glacial event

Glacier A (t) A (h) ELA A (t) A (h) ELA A (t) A (h) ELA

Ropojana (B. i Jezerces) 1050 2450 1750 1350 2450 1900 1800 2450 2125

Ropojana (F. e Runices) 1050 2450 1750 1300 2450 1875 1800 2450 2125

Bjelic NW 1850 2350 2100

Bjelic SE 1950 2400 2175

Valbona 920 2450 1685

Grbaja 1020 2350 1685 1800 2350 2075

Bogicevica 1560 2200 1880 1970 2200 2085

Dober Dol 1950 2250 2050 2100 2250 2175

Average ELA 1750 1942 2123

M. Milivojevic et al. / Quaternary International 190 (2008) 112–122120

with other locations in the area (Pindus Mountain inGreece, Velebit Mountain in Croatia, Retezat Mountain inRomania, the Pyrennees, etc; Fig. 11).

Equilibrium line altitude during the maximum glacierextent on the Apennines was at the elevation of 1750m(Giraudi and Frezzotti, 1997), which exactly correspondsto the ELA in Mt. Prokletije. Chronologically, theseauthors have placed this maximum glaciation in the LastGlacial Maximum (c. 22.000 14C BP). The similar resultswere obtained also by Jaurand (1998). In both works, theYounger Dryas is distinguished as another phase ofglaciation, but with lesser extent.

On the island of Corsica, the maximum extent of glaciersis attributed to Early Wurmian, while the correspondingELAs vary from 1400 to 1500m in wet parts of the island,to 1750m in the dryer NE and SW parts (Kuhlemann et al.,

2005). The ELA in the dry parts of Corsica was the same asin Mt. Prokletije during the maximum glaciation.Although the latitude is almost the same, the comparison

of this study area with the Pyrenees is difficult, because thePyrenees have higher precipitations due to the influences ofthe Atlantic. However, the reported ELA (1600m onnorthern side) from the eastern (Mediterranean) parts ofthe mountain range (Calvet, 2004) allows partial compar-ison with Mt. Prokletije.Extensive studies with advanced dating techniques

(Uranium series) in the area of Pindus Mountain in Greece(Hughes et al., 2006b, c, 2007a, b) point to the existence of twosignificant pre-LGM glaciations. The strongest one predates c.350,000 BP. The altitude of ELA during that glaciation(1675–1741m) is generally in accordance with ELA during themost extensive glaciation on Mt. Prokletije (1750m).

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Fig. 11. Positions of equilibrium line altitudes (ELA) on some of the mountains in the Mediterranean region, during maximum glaciers extent (regardless

of numerical chronology).

M. Milivojevic et al. / Quaternary International 190 (2008) 112–122 121

Mt. Sara (2748m) is situated almost at the same latitudeas Mt. Prokletije, about 100 km further to the east.Preliminary observations point to lowest ELAs of1900–2000m (unpublished data, J. Kuhlemann).

The results of studies of glaciation in Croatia (Marjanacand Marjanac, 2004) differ to a considerable extent fromthe other results in the Mediterranean area. The authorsreport very low altitudes of end moraines, very close to sealevel. Therefore it is impossible, at this stage, to make anycorrelations with Mt. Prokletije, until more advancedresearch is done at both locations.

In spite of being located at somewhat higher latitude,Mt. Retezat in the Southern Carpathians in Romania isone of the possible examples for correlation with Mt.Prokletije. Reuther et al. (2007) present a complex studyusing exposure dating and pedological investigationspointing to substantial pre-LGM glacial advances.

5.3. Hypotheses on the glacial chronology

According to the cited references related to glaciationson a number of Mediterranean mountains, three glacia-tions in the central part of Mt. Prokletije can behypothetically linked to some already defined glaciationsthat took place during the Late Pleistocene. Regarding thefact that the most complex numerical and relative dating ofglacial events in the Mediterranean mountains was done onPindus Mountain in Greece (Hughes et al., 2006b, c), andthat the results showing the maximum glacier extent priorto the global LGM are obtained elsewhere ( Reuther et al.,2007), it is assumed that the maximum Prokletije glaciationtook place in Early or Middle Pleistocene (MIS 6, orpreviously). Subsequently, the second series of Prokletijemoraines can be attributed to the period of the Last GlacialMaximum (MIS 2), while the third glaciation probablytook place during the Younger Dryas. Alternatively,accepting the results that point to maximum glaciationsin the Mediterranean during LGM or slightly prior to thisstage (Giraudi and Frezzotti, 1997; Palmentola et al.,1990), then the Prokletije maximum would also be placed

in the LGM, the second glacial event in Oldest or OlderDryas, and the most recent glacial event in the YoungerDryas.Younger Dryas cooling in the area of Mt. Prokletije was

suggested also by Palmentola et al. (1995), within the studyof inactive rock glaciers. The altitudes of the rock glaciersmainly correspond to the altitudes of final recessionalmoraines, cirque moraines and rock glaciers attributed tothe youngest glaciation within the present paper. On theother hand, Hughes et al. (2003) linked the maximumdevelopment of rock glaciers on Mt. Tymphi in Greecewith the period of the Last Glacial Maximum, instead ofthe Younger Dryas.

6. Conclusions

Detailed geomorphological mapping of glacial land-forms in the central area of Mt. Prokletije has lead to thedefinition of three series of moraines, which correspond tothree different glacial events. Moreover, the mappingshowed that the present-day glaciation is active as well,although with very limited extent: in the area in the vicinityof the peak Maja e Jezerces there are three small activeglaciers that cover a total surface of about 11 ha.During the most extensive glacial event, the average

ELA was at 1750m, in the second event at 1942m, andduring the youngest glacial event it was positioned at2123m altitude. As numerical dating methods were notavailable for this study, some suggestions about thechronology of glaciation are given after comparison withother mountains of similar elevation throughout theMediterranean. In that sense, the maximum glacial eventof Mt. Prokletije could have taken place during early ormiddle Wurmian, the second during the Last GlacialMaximum, and the third one in the Younger Dryas.The appropriate combination of numerical and relative

dating techniques would evaluate the defined hypothesis.The broad limestone areas of Mt. Prokletije are favourablefor U-series dating of calcite cements, as shown by Hugheset al. (2006b). The presence of quartz veins and rubble in

ARTICLE IN PRESSM. Milivojevic et al. / Quaternary International 190 (2008) 112–122122

some parts of central Prokletije could enable the applica-tion of surface exposure dating methods using cosmogenicnuclides ( Kelly et al., 2004). Moreover, detailed sedimen-tological and pedological analyses of glacial and fluviogla-cial sediments are needed to supplement the numericaldating methods. Further research would in future bringMt. Prokletije into the third, advanced phase in Hugheset al. (2006a) classification—understanding of geochronol-ogy using radiometric dating and detailed sedimentologicalanalyses.

Acknowledgments

We are grateful to the reviewers for very helpfulsuggestions and comments which lead to the improvementof our paper. Special thanks to J. Kuhlemann and E.Jaurand for useful advice and help. Part of this work isincluded into the project no. 146011, financed by theMinistry of Science of The Republic of Serbia.

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