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Glacial geology and deglaciation chronology of the area between inner and Jostedalsbreen Strynefjellet, western

NORALF RYE, ATLE NESJE, RUNE LIEN, LARS HARALD BLIKRA, OLIANNE EIKENÆS, PER AUDUN HOLE & INGRID TORSNES

Rye, N., Nesje, A., Lien, R., Blikra, L. H., Eikenæs, 0., Hole, P. A. & Torsnes, 1.: Glacial geology and deglaciation chronology of the area between inner Nordfjord and Jostedalsbreen - Strynefjellet, . Norsk Geologisk Tidsskrift, Vol. 77, pp. 51-63. 1997. ISSN 0029-196X.

A lower limit of blockfields is inferred to indicate the maximum heights and thus thickness of the Late Weichselian iee sheet in the inner Nordfjord region. lee movements in this area have been topographically controlled during the entire Weichselian glaciation. Prominent lateral de1imit the Younger Dryas in inner Nordfjord. Subsequent to the Younger Dryas Chronozone, the glaciers retreated rapidly due to calving in the and climatic amelioration. In a later phase of deglaciation, in all probability around the early and middle part of the Preboreal Chronozone, an iee eentre east of Strynefjellet dominated, while the Jostedalsbreen area is thought to have played a minor role as a eentre of iee dispersal. The final deg1aciation was dominated by vertically down-wasting iee remnants in the lake basins and tributary valleys. Terminal moraines in front of several outlet glaciers of Jostedalsbreen beyond the 'Little lee Age' moraines indicate a climatic deterioration at the end of the Preboreal Chronozone.

N. Rye, Department of Geology, University of , A/legt. 41, N-5007 Bergen; A. Nesje, Department of Geography, University of Bergen, Breiviken 2, N-5035 Bergen-Sandviken; R. Lien, Statens Vegvesen, P.O. Box 608, 9800 Vadsø; L. H. Blikra, Geological Survey of Norway, P.O. Box 3006, N-7002 Trondheim; O. Eikenæs, Norges vassdrags- og energiverk, P.O. Box 5091 Majorstua, N-0301 Oslo; P. A. Hole, Statoil, N-5020 Bergen; l. Torsnes, Mø//esvingen 2, 0854 Oslo, Norway.

Introduction ioner Nordfjord is complicated and the rocks have been subject to several deformation phases during the Precam­ Recent investigations in the area between ioner Nord­ brian and Caledonian orogenies. fjord and Jostedalsbreen (breen = ) - Strynefjellet (fjellet=mountain) (Rye et al. 1984, 1987; Nesje 1984; Lien 1985; Hole 1985; Blikra 1986; Nesje et al. 1987, Landforms 1991, Nesje & Kvamme 1991; Nesje 1992; Dahl & Nesje 1992; Nesje & Dahl 1992; McCarroll & Nesje 1993; The landscape of ioner Nordfjord (Figs. l, 2) has evolved Torsnes et al. 1993) make it possible to present a deglaci­ from a plateau landscape which was developed close to ation history from the Late Weichselian maximum up to sea level during the Mesozoic and during a subsequent the present in this part of western Norway. uplift in the Tertiary. At present, remnants of this Marine terraces have previously been mapped by Kal­ plateau landscape can be seen as rather smooth, undulat­ dhol (1912). Rye (1963, 1978) and Fareth (1970, 1987) ing sumrnit areas along Nordfjord, gently sloping from described the deglaciation in the middle and inner parts 1800-2000 m at Jostedalsbreen to 400-600 m at the of Nordfjord, while the areas between Jostedalsbreen and coast (Fig. 3). During the Quatemary glaciations, the Strynefjellet have been less well known. Stokke ( 1982) plateau landscape was exposed to glacial erosion. During mapped the Quatemary deposits in the valley bottom in the ice-free interglacial periods, fluvial and avalanche and Hjelledalen. activity modified the landscape. The valleys in ioner Nordfjord have topographic features characteristic of glaciated areas: steep valley sides with U-shaped trans­ verse profiles, bedrock basins occupied by lakes or filled Bedrock in with sediments, rock thresholds, , and hanging The bedrock in Nordfjord consists of Precambrian valleys. The fjord and the main valleys in ioner Nord­ gneisses and granites which are l 000-1800 million years fjord are good examples of topographic features, whose old. The rocks are divided into two main units; the direction and glaciated form were controlled by fracture Fjordane Complex (at surface) and the Complex zones more so than in the homogeneous and resistant (at depth). Ioner Nordfjord belongs to the Jostedal Com­ areas. In the main valleys there are both wide, deep plex. The dorninating rocks are banded gneiss and basins and short, narrow gorges where rivers form water­ granitic gneiss. The tectonic history of the bedrock in falls. 52 N. Rye et al. NORSK GEOLOGISK TIDSSKRIFT 77 (1997)

SUNNMØRE

Skjlk

o 10 20 30km

Fig. l. Location map of Nordfjord.

One branch of the Nordfjord, (dalen = terrain and an ice surface above the level of mountain valley), stretches about 20 km southward to Brigsdalen summits. He notes the presence of erratics and in where two outlet glaciers from Jostedalsbreen, Brigsdals­ same blockfields reaching a level of at least 600-700 m. breen and Melkevollsbreen are situated. Another branch, However, Pollestad seems to have included al­ Lodalen, reaches 15 km southeast where the three valleys lochthonous blockfields and boulder-rich in his Bødalen, Nesdalen and Kjenndalen coalesce. In these blockfield definition, and consequently his blockfield valleys the glacier outlets from Jostedalsbreen; Bø­ limit is 200-300 m lower than the autochthonous dalsbreen, Ruteflotbreen and Kjenndalsbreen are lo­ blockfield boundary described by Nesje et al. ( 1987) in cated. Strynedalen branches north from Nordfjord, the same region. In a recent paper, Larsen et al. (1995) swings east, continuing about 20 km to the east, where conclude that the lower limit of the blockfield cannot be the valleys Hjelledalen/Videdalen and Erdalen coalesce. taken as the upper glacial surface during the Weichselian Glomsdalen is a north-south oriented, hanging valley to max1mum. Strynedalen at the eastern end of Strynevatnet ( vat­ Glacial striations show that ice movements in this area net = lake). The valleys Skjerdingsdalen, Grasdalen and have been topographically controlled throughout the Sunndalen are tributary valleys to Hjelledalen. Late Weichselian glaciation, especially during the late phases (Fig. 5). The oldest striations in the area are found on Langvasseggi (1600 m a.s.l.). Striations north­ west of Videdalen and Djupvassegga (1500 m a.s.l.) show Late Weichselian glacier extent, glacial ice movements toward the northwest crossing Videdalen maximum and ice movements and Grasdalen towards during the most exten­ Mapping of blockfields in the mountain areas has sive phase of the last glaciation (Blikra 1986). The tribu­ demonstrated that the weathering limit is found to be tary valley Glomsdalen has two northern pass-points at about 1750 m a.s.l. at Strynefjellet, descending to about 1360 and 1400 m a.s.l. toward Holedalen and Hellesylt, 1500 m a.s.l. between inner Nordfjord and Sunnmøre while Skjerdingsdalen has a pass-point of 1200 m a.s.l. (Nesje et al. 1987; Rye et al. 1987, Fig. 4). The lower toward Flydalen and Geiranger. Hole (1985) and Blikra limit of the blockfields is interpreted by Nesje et al. ( 1986) mapped glacial striations in these pass-points (1987) to represent the upper limit of the Late Weichse­ (Fig. 5), showing ice movements from south to north. lian maximum . At that time, the glacier front Lateral moraines deposited during the Y ounger Dryas reached the edge of the continental shelf off the Møre Chronozone, indicating an ice surface around 800 m coast (Andersen 1979, 1981; Rokoengen 1979; Bugge a.s.l. in Holedalen and around 900 m a.s.l. in Flydalen 1980). (Kalstad 1993). This indicates that the striations mapped Resistance to the concept of Late Weichselian nuna­ in the pass-points must be older than the Y ounger Dryas taks has none the less persisted, most recently by F ol­ Chronozone. These northerly striations might possibly lestad ( 1990), who stresses the consistent pattern of represent the Late Weichselian maximum ice movement. striations and till fabrics in the Nordmøre region, sug­ In two pass-points between Glomsdalen and Skjerdings­ gesting ice movement largely independent of the local dalen (1340 and 1260 m a.s.l.) striations show glacier NORSK GEOLOGISK TIDSSKRIFT 77 (1997) Glacial geology. Nordfjord-Jostedalsbreen 53

Fig. 2. Location map of inner Nordfjord and the area. 54 N. Rye et al. NORSK GEOLOGISK TIDSSKRIFT 77 (1997)

2500 Jostedals· breen

2000

I 1500 Ålfotbreen 'O"' � ;;' 1000

500

o

I :; ·500 "'"- Fig. 3. Longitudinal profile of Nordfjord showing altitude of Cl mountains on the northem and southem sides of the fjord together with the fjord bottom. The submarine part is 50 1 00 Distance (km) adapted from Giskeødegaard (1983).

movements towards the west and southwest (Fig. 5). The yond the inland ice, local glaciation, especially lateral­ northern pass-point is probably so high that no active ice frontal , was common (e.g., Reite 1967; Fareth movement from Skjerdingsdalen to Glomsdalen took 1970, 1987; Mangerud et al. 1979; Larsen et al. 1984). place during the Younger Dryas Chronozone. Evidence of Yo unger Dryas local glaciation, especially The other pass-points between these two valleys are lateral-frontal moraine, is found in the valleys lower and situated further south, which favour an active south of Holedalen (east of Hellesylt). ice movement from east to west. In addition, Glomsdalen Fareth ( 1970, 1987) mapped the ex tent of the Nord­ has a pass-point toward a valley between Flo and fjord glaciers during the Younger Dryas readvance on Holedalen ( 1160 m a.s.l.). Glacier movements towards the basis of lateral moraines. In Stryn, lateral moraines the southwest out of Glomsdalen, as demonstrated by from this advance are deposited in Vikadalen (760-800 glacial scouring, probably took place both during the m a.s.l.) and Staurnibba (1084 m a.s.l.) (Fig. 5). On the Late Weichselian glacial maximum and the Younger basis of these moraines, Fareth ( 1970, 1987), in his Dryas Chronozone (Fig. 5) (Hole 1985). reconstruction, indicates an ice surface at 1000-1100 m a.s.l. in Stryn. In Olden and he placed the ice surface at 1100-1200 m a.s.l. In Olden two sets of lateral moraines 1170 and 1120-1130 m a.s.l. on the plateau north of Sisiliekruna may also be correlated to the Y ounger Dryas glaciation Yo unger Dryas lateral moraines at Skarsteinfjellet fur­ The investigated area is situated at the borderline of the ther to the north. On the eastern side of Oldedalen, inland ice during the Y ounger Dryas Chronozone. Be- lateral moraines at altitudes from 1080 to 1200 m a.s.l.

w E 2400 2200 _ Lodalskåpa 2000 mountain peaks _Snønipa _Skåla _Brenibba E _ G.Jer d ea k sa1 � 1800 Melheimnibba Q) 8/ockfie/d boundary "C 1600 t Sisiliekruna 2 Jostedals-breen -.;::: 1400 <( 1200 Younger Dryas glacier surface 1ooo L------8oo St ryn Olden Loen Hjelle 600 4------��-----r------�------.------�------,.------�----__, o 1 o 20 30 40 Distance (km)

Fig. 4. The blockfield boundary in ioner Nordfjord. NORSK GEOLOGISK TIDSSKRIFf 77 (1997) Glacial geology. Nordfjord-Jostedalsbreen 55

o 10 20km. �------��------� Contour interval 200 m Leg end:

= Submarin marginal moraine n Mounds and ridges

Marginal moraine depos�ed by fjord - , movement towards the observation point '"..., or valley glaciers -- Crossing glacial striations, increasing number of � Glaciofluvial depos� with terrace slope -... ticks indicate increasing relative age.

B Glaciofluvial deposit 1120 Pass·point

Bs Glaciolacustrine deposit eoo Contour interval

••

Fig. 5. Glacial geology of inner Nordfjord and adjacent district. 56 N. Rye et al. NORSK GEOLOGISK TIDSSKRIFT 77 (1997)

Fig. 6. Reconstruction of the valley glaciers in inner Nord­ fjord during formation of the early Preboreal moraines.

are mapped and correlated with the Y o unger Dryas At the mouth of the Geirangerfjord, Giskeødegaard marginal moraines (Fig. 5). In Fosdalen, east of Loen, (1983) mapped a submarine end moraine, and in the lateral moraines at 1020-1100 m a.s.l. (Lien 1985; Nesje valley sides further to the east (Fig. 5) are several promi­ & Dahl 1992), indicate a somewhat lower ice surface nent lateral moraines which can be correlated with this than that suggested by Fareth. end moraine. In Flydalen the corresponding lateral Extrapolation of the Y ounger Dryas lateral moraines moraines are situated 900 m a.s.l., showing that there from the head of the fjord toward Jostedalsbreen this was possibly no active glacier moving across the pass­ gives an ice surface of 1300-1400 m a.s.l. in the inner point from Skjerdingsdalen to Geiranger during the parts of the valleys, suggesting that fairly steep glacier Y ounger Dryas Chronozone. Lateral moraines north of falls may have existed along the western margin of the Dalsnibba, descending from 1300 to 1000 m a.s.l. at a Jostedalsbreen plateau. North of Flo at Strynevatnet, the distance of l km, show that the glacier had a steep pass-point toward Hellesylt is situated at 540 m a.s.l. In surface profile toward Geiranger. his reconstruction, Fareth (1970, 1987) placed a Younger Marginal moraines in the valley bottom and the valley Dryas valley glacier through the pass-point to a location sides in the Tafjord area (Fig. 5) were deposited during 4 km north of Hellesylt, where Giskeødegaard ( 1983) the late Y ounger Dryas Chronozone and early Preboreal mapped a 100 m high submarine frontal deposit. This Chronozone (Eikenfæs 1991). reconstruction is not, however, based on any lateral The ice surface along the Stryn valley was probably ca. moraines. In Holedalen, Kalstad (1993), however, 1300 m a.s.l. south of Glomsdalen during the Y o unger mapped prominent lateral moraines around 800 m a.s.l. Dryas. With pass-points at 1360-1400 m a.s.l. to the (Fig. 5). In addition, marginal moraines were deposited north, no active ice movement toward Holedalen could by local glaciers in the small cirques south of Holedalen. have taken place. On the other hand, the pass-points NORSK GEOLOGISK TIDSSKRIFT 77 (1997) Glacial geology. Nordfjord-Jostedalsbreen 57

Table l. Radiological datings. For other radiological datings in this area, see Fig. 12 in Rye et al. (1987).

No. Lab. no. Matr. 14C-age Refr.

T-5812 Peat 9340 ± 130 Rye et al. (1987) 2 T-5811 Peat 8080 ± 60 Blikra (1986) 3 T-5606B Peat 9260± 140 Kvarnme (1984) 4 T-5810A Peat 9030± 100 Lien (1985) 5 T-616 Shells 9390± 200 Fareth (1970) 6 T-4839 Limnic sediments (gyttja) 8810 ± 130 Nesje (1984) 7 T-4234 Coal (forest) 2450± 40 K vamme & Randers (1982)

north of Glomsdalen and Skjerdingsdalen were domi­ Innvikfjorden and Lake Hornindalsvatn (Fig. l) of nated by local glaciers merging with the valley glaciers. 9340 ± 130 14C yr BP (Table l, T-5812). Marginal de­ In Glomsdalen this might have resulted in a fairly hori­ posits are mapped at the mouths of Strynedalen, Lodalen zontal ice surface. During this period glaciers drained and Oldedalen (Fig. 5). These marginal deposits are from Skjerdingsdalen to Glomsdalen (pass-point 1260 m relatively prominent and were deposited during the early a.s.l.) and from Glomsdalen to the valley between Flo part of the Preboreal Chronozone (Fig. 6). In Stryn, two and Hellesylt (pass-point 1160 m a.s.l.) (Fig. 5). ice-marginal deposits are mapped, the Vinsrygg moraine In the mountain areas between Oldedalen, Lodalen and the Årheim terrace (Fareth 1970, 1987; Nesje 1984; and Strynedalen, extensive areas are presently covered by Rye et al. 1987). In Loen, a submarine and a supra­ cirque- and plateau glaciers. During the Yo unger Dryas marine were deposited (Lien 1985). In these glaciers probably had outlet glaciers merging with Olden two marginal deposits at Melheim-Løken and the valley glaciers from the inland ice, but no deposits Eide are mapped. have been found which can confirm or refute this, be­ In previous work, Preboreal marginal deposits have cause these areas lay above the equilibrium-line altitude been thought to indicate a climatic deterioration (e.g., (ELA) at that time. Vorren 1973; Bergstrøm 1975), white recent investiga­ During the Yo unger Dryas the ice surface reached tions (Kjenstad & Sollid 1982; Sollid & Reite 1983; Anda about 1600 m a.s.l. at Strynefjellet, based on an interpre­ 1984; Rye et al. 1987) include glaciodynamic principles as tation of glacial scouring. At this time, the glacier front a possible explanation for their formation. Thus, as a was located at Anda-Lote, in the middle part of Nord­ result of rapid calving in Nordfjord, the glacier had a fjorden. When the Preboreal end moraines at Olden, steep and dynamically unstable profile at the front. As Loen and Stryn were deposited, the glacier surface the three valley glaciers in Stryn, Loen and Olden be­ reached about 1200-1300 m a.s.l. in the inner parts (Fig. came grounded on bedrock thresholds or in a narrow 6). Steep glacier falls may have existed between Jostedals­ portion of the valley, the frontal retreat ceased or became breen and the valley glaciers. This illustrates that the strongly reduced. In order to achieve dynamic stability, elevation of the ice surface in inner parts of the valleys the glaciers advanced in order to adjust their surface shows little variation while the response at the glacier profile to the new dynamic conditions. The glaciody­ fronts was extensive. This 'hinging' -effect is clearly namic theory as a model for these marginal deposits demonstrated in a smaller scale at the recent glaciers, makes it impossible to correlate them chronostratigraph­ e.g., the Bødalsbreen glacier (Lien 1985). In Fosdalen, an ically. According to the glaciodynamic model, the mar­ easterly tributary to Loen, Nesje & Dahl ( 1992) calcu­ ginal deposits at Stryn (Vinsrygg) were probably lated the equilibrium-line depression at 425 m during the deposited somewhat earlier than the deposits in Olden Younger Dryas. In (Fig. 1), Dahl & Nesje (1992) and Loen. calculated the Y ounger Dryas ELA depression at about 500 m. They also calculated that the winter precipitation Stryn was reduced to about 60% of the present values. East of Stryn, Fareth (1970, 1987) mapped prominent marginal moraines deposited by a valley glacier in Strynedalen (Fig. 5). In the valley sides to the east, Deglaciation after the Y ounger Dryas lateral moraines 200-300 m below the Younger Dryas Chronozone lateral moraines have been mapped and correlated with Subsequent to the Younger Dryas glacier advance, a the marginal moraines at Stryn, which he termed the period of rapid retreat of the Nordfjord glacier occurred, Vinsrygg moraines. Fareth (1970, 1987), in his recon­ probably as a result of extensive calving in the deep struction, placed the icefront during the Vinsrygg event and in the deep lake, Hornindalsvatn. A radiocar­ across northeast of Innvik. Recently, the bon date on peat west of Stryn gives a minimum age of corresponding ice-marginal deposit has been found on the deglaciation of the pass-point Markane, between the eastern side of the Stryn bay. Ir. our opinion, there- 58 N. Rye et al. NORSK GEOLOGISK TIDSSKRIFT 77 (1997) fore, the glacier front was a calving front located in the would expect the terraces in the eastem part to be higher bay at Stryn when the Vinsrygg moraine was formed. than in the west, but this is not the case. The terraces are Fareth ( 1970, 1987) interpreted a terrace lying 69 m interpreted to be lateral deposits built up along down­ a.s.l. at Øvreeide, in the western end of Strynevatnet as wasting ice remnants in the valley bottom. Such a rapid an ice-frontal deposit (Fig. 5), which he correlated to the down-wasting could have been the result of deglaciation Eide moraine in Olden. Stokke ( 1980) reinterpreted the of the pass-point at Videdalen-Strynefjellet. deposit to be a terrace built up to 65 m a.s.l. (Fig. At Skora a small esker and a relatively large glacioftuvial 5). No lateral moraines are recognized in connection with lateral terrace are present (Fig. 5). Deep meltwater chan­ this deposit. nels in the terrace are evidence for lateral meltwater Lateral moraines thought to have been deposited during drainage. The terrace is interpreted to be a lateral deposit the Preboreal Chronozone have been mapped in Sun­ to an ice remnant in Hjelledalen deposited after deglacia­ ndalen, Hjelledalen, and Glomsdalen between 900 and tion of the pass-point at Strynefjellet-Videdalen. At the 1200 m a.s.l. (Fig. 5) (Rye et al. 1984; Hole 1985). The pass-point in Videdalen, and hurnmocky moraine deposits are, however, too scattered to justify finn corre­ were deposited. lations with any frontal deposits at Stryn. In G1omsdalen, Skjerdingsdalen, Grasdalen, Hjelledalen and Erdalen there are deposits (mounds and ridges) showing that the last part Breidalen of deglaciation took place as vertical down-wasting of In Breidalen the pass-point at ( 1160 m a.s.l.) stagnant ice remnants in Strynevatnet and Hjelledalen toward Geiranger was deglaciated while there still was ice (Rye et al. 1984, 1987; Nesje 1984; Hole 1985). to the east. As a result, a glacier-dammed lake developed in the eastem part of Djupvatnet, where well-sorted fine Hjelledalen and silt was deposited. At further east in Breidalen, eskers and hummocky moraine were formed, At Hjelle, glacioftuvial terraces with a relatively horizon­ indicating a vertically down-wasting, dynamically inactive tal surface were built up to 75 m a.s.l. (Stokke 1982; Rye glacier. et al. 1984) (Fig. 5). Kaldhol (1912) described these terraces noting large boulders along the edge of the terrace toward Strynevatnet which he interpreted as a Glomsdalen result of an ice remnant in the Strynevatnet basin during terrace . Thus, the terrace slope toward Stryn­ In Glomsdalen Hole ( 1985) mapped lateraljsublateral evatnet was believed to be an ice-contact slope. At glacioftuvialdeposits at differentaltitudes ranging altitudi­ Vollsnes, northeast of Hjelle, a section in another terrace nally between 1200 min the north and 300 m in the south built up to at least 70 m a.s.l. shows glacioftuvial gravel (Fig. 5). Lateral glacioftuvialterraces were deposited in two and stones with westward dipping foresets. Covering the smaller tributary valleys east of Glomsdalen at altitudes foreset beds is l-2 m of horizontal, laminated fine sand between 1200 and 900 m. On the valley bottom in the and silt at the top. In the eastem part of the terrace, northem part of Glomsdalen there are hummocky deposits segments and blocks of bedded glacioftuvial material with a complex composition (Hole 1985). Further south have been tilted and thrust by glaciotectonic activity. glacioftuvial deposits as eskers and are common About 3-4 km further east in Hjelledalen several (Fig. 5). In the mouth of Glomsdalen finematerial has been terraces were built up to about 75 m a.s.l., mainly along deposited in a glacier-dammed lake about 400 m a.s.l. The the northem valley side (Fig. 5). Rye et al. ( 1984), Nesje pass-points in the north end of Glomsdalen at 1360 and ( 1984), and Hole ( 1985) concluded that the glacier in 1400 m a.s.l. must have been deglaciated at the end of the Strynevatnet melted down vertically. The terraces at Yo unger Dryas Chronozone, while a glacier was still Hjelle were probably deposited into a freshwater lake moving across the pass-point (1260 m a.s.l.) from Skjerd­ with a communicating water level to the sea further west ingsdalen in the east. As this pass-point was itself deglaci­ while there still was an ice remnant in the Strynevatnet ated, the last part of the deglaciation in Glomsdalen took basin. The deposits at Vollsnes show that the valley place as vertical down-wasting. Finally, the ice surface glacier in Hjelledalen advanced across the glacioftuvial sloped up-valley, and a was formed in the terrace eroding the top and leaving a layer of till. The southem part. Small glacioftuvial lateral terraces 300 m fine-grained sediments on top were deposited as the a.s.l. at the mouth of Glomsdalen were deposited along the glacier retreated. The tilted units of glacioftuvial material margin of the ice remnant in the Strynevatn basin (Hole are related to another glacier advance shortly afterwards. 1985). At Strynevatnet a glacioftuvial terrace was formed Stokke ( 1982) interpreted the terraces in the eastem part at a water level of about 75 m a.s.l. of Hjelledalen to be remnants of a glacioftuvial deposit filling the entire valley. The evidence indicating glacier advances and subsequent sedimentation of fines shows, Grasdalenf Skjerdingsdalen however, that this cannot have been the case. If Blikra ( 1986) mapped glacial striations indicating that Hjelledalen were filled up with glacioftuvial deposits, one glaciers moved from Breidalen over Oppljosvatn and NORSK GEOLOGISK TIDSSKRIFT 77 (1997) Glacial geology. Nordfjord-Jostedalsbreen 59 down Grasdalen (Fig. 5), possibly during the Younger (1240 m a.s.l.) was deglaciated earlier than the sea could Dryas Chronozone. At the same time, ice flowed across penetrate into Hjelledalen. The lower part of Sunndalen Grasdalsvatnet through a pass-point 1440m a.s.l. toward was proba bly covered by an ice remnant in connection with Videdalen/Hjelledalen in the south. During this period the glacier occupying Hjelledalen, thus preventing deposi­ the ice surface must have been about 1600 m a.s.l. in the tion of a terrace at the mouth of Sunndalen. In Sunndalen area around Oppljosvatnet. Below 1500 m a.s.l. indica­ a radiocarbon date on peat yielded 9260 ± 140 14C yr BP tions of glacial meltwater drainage are recognized in the (Table l, T-5606 B) giving a minimum date of the form of rounded boulders and stones in pass-points and deglaciation in this area (Kvamme 1984). along mountain slopes (B likra 1986). The pass-point south at Oppljosvatn ( 1440 m a.s.l.) was one of the first to be deglaciated. The closing of this pass-point may Erda len have led to the deposition of a lateral moraine 1420 m In Erdalen Nesje (1984) mapped glaciofluvial deposits at a.s.l. south of Oppljosvatn. altitudes ranging from 690 to 130 m a.s.l. (Fig. 5). He Southerly glacial striations in the pass-point between interpreted these as lateral/sublateral terraces deposited Djupvassegga and Oppljosegga ( 1340 m a.s.l., Fig. 5) along the edge of a down-wasting glacier with a relatively may have been formed at the end of the Yo unger Dryas horizontal surface. In Vetledalen, a tributary valley to or early Preboreal Chronozones before the pass-point the northeast of Erdalen, a glaciofluvial terrace was was closed. When the pass-point northwest of Grasdals­ deposited 690 m a.s.l., dammed by a valley glacier in vatnet ( 1240 m a.s.l.) was closed, all ice passing Oppljos­ Erdalen. In the distal part of the terrace, the glacier vatnet flowed down Grasdalen. In this phase of occupying Erdalen pushed up a lateral moraine. At that deglaciation the glacier in Skjerdingsdalen melted down time, there was no connection between the glacier in vertically. Lateral deposits between 600 and 1000 m a.s.l. Erdalen and the glacier in Vetledalen. Nesje (1984) ex­ indicate that the glacier surface was somewhat lower in plained this by ice supply from an ice culmination east of the south than in the north. This demonstrates that the the Jostedalsbreen plateau. According to radioecho valley glacier flowing through Grasdalen was not very soundings on Jostedalsbreen (Sætrang & Holmquist dynamically active. The presence of hummocky 1987), the subglacial bedrock pass toward Vetledalen is till in the northern part of Skjerdingsdalen demonstrates dose to 1500 m a.s.l., while the pass-point to Erdalen is that the glacier was almost dynamically inactive at the between 1300 and 1400 m a.s.l. As a result, Vetledalen final stage of deglaciation. When the glacier in Skjerd­ did not receive ice from the east, while the lower pass­ ingsdalen had melted down, a valley glacier still flowed point toward Erdalen allowed ice to drain across the down Grasdalen. A prominent lateral-frontal moraine pass-point into Erdalen. If the glacier movement down deposited where Grasdalen and Skjerdingsdalen coalesce Erdalen was climatically determined, one might assume illustrates this. The Grasdalen valley glacier was not that the Vetledalsbreen glacier had merged with the connected to the Videdalen/Hjelledalen glacier at this glacier in Erdalen. This indicates that Jostedalsbreen did time. This is proved by glaciolacustrine sediments de­ not play a dominant role in ice supply to Erdalen in this posited in the southern part of Skjerdingsdalen. The lake late phase of the deglaciation, except during the Erdalen was dammed by the down-wasting glacier in Videdalen/ event (Holmquist 1987, p. 27). Hjelledalen. Glaciofluvial lateral terraces east of Grasdalsvatnet show that the lake was dammed in a period during the Loen melting of the valley glacier. When the pass-point north­ west of Grasdalsvatnet was deglaciated, the glacier At the fjord bottom 1.5 km west of the Loen village, moved through Grasdalen. This is demonstrated by there is a 15 m high submarine ridge covered by boulders glacial striations east of Grasdalsvatnet (Fig. 5). When (Fig. 5). No lateral moraines have been found attributed the pass-points at Oppljosvatnet were deglaciated, the to this ridge, but it is interpreted as a terminal moraine deglaciation in Grasdalen was characterized by vertical deposited by a valley glacier in Lodalen (Lien 1985). On down-wasting (B likra 1986). A radiocarbon date from the northern side of the village of Loen a 4-5 m high peat in Skjerdingsdalen gives a minimum deglaciation terminal moraine was deposited. South of Loen a lateral age of 8080 ± 60 14C yr BP (Table l, T-5811). moraine was deposited starting at the valley bottom and terminating at a level of 230 m a.s.l. on the valley side. This lateral moraine is correlated to the terminal moraine north of the Loen village. At Sæten, in the northwestern Sunndal en part of , a glaciofluvial terrace was formed No evidence of lateral meltwater drainage is recognized in 86-89 m a.s.l. The terrace is regarded as a frontal Sunndalen, but possible deposits may have been removed deposit, built up during a halt in the deglaciation. A by subsequent Holocene avalanche activity. No terraces radiocarbon date on peat east of Loen gives a minimum were built up to the marine limit at the mouth of age for the terminal moraines at Loen of 9030 ± 100 14C Sunndalen. This indicates that the pass-point to Sunndalen yr BP (Table l, T-5810 A). 60 N. Rye et al. NORSK GEOLOGISK TIDSSKRIFT 77 (1997)

120 �------.

Legend: The Nor moraines c c c c 100 1!1 Tapes � o c - • Younger Dryas • • E 80 - • + ·- " Hornindai/Utfjorden • • 1111 ... . Q) • 1111 "O 60 Loen -:::s ;; Stryn C( 40 Olden

20

o o 20 40 60 BO 100 120 Distance (km)

Fig. 7. Shoreline diagram for Nordfjord showing the Younger Dryas and Tapes marine levels in Nordfjord. Adapted from Fareth (1987) and Rye et al. (1987).

In the tributary valleys of Lodalen; Fosdalen, Breng Olden and Austerdalen (Fig. 5), lateral moraines were deposited About 2 km south of the village of Olden, a large at levels between 300 and 1120 m a.s.l. The lateral marginal deposit at Melheim-Løken is presently moraines at the mouth of Fosdalen 460-500 m a.s.l. can damming Lake Floen. About l km south another mar­ proba bly be correlated with the terminal moraine in Loen. ginal deposit was formed at Eide in front of Oldevat­ The other lateral moraines have a scattered distribution, net (Fareth 1970, 1987). Shells found at Håheim, and it is therefore difficult to correlate them with a proximal to the Eide moraine are radiocarbon dated to particular terminal moraine in Loen. Bødalen, east of 9390 ± 200 14C yr BP (Table l, T-616), thus giving a Lodalen, has a marked 'break' in the longitudinal profile minimum age of the Eide and Melheim/Løken 580 m a.s.l. (Fig. 5). In the lower part of the valley, below moraines. 500 m a.s.l., eskers and lateral/sublateral glaciofluvial In Sundsdalen east of lateral moraines, deposits have been mapped (Lien 1985). A lateral deposit which probably can be correlated to the Melheim/Løken in Nesdalen indicates that at this time, an active glacier moraine, were deposited 1040 m a.s.l. (Fig. 5). As a result was still moving down Bødalen merging with the glacier of the steep valley sides, no other lateral moraines are in Lodalen. Eskers and lateral deposits in the lower part recognized in Oldedalen, and those which exist are too of Bødalen show that in a later phase the Bødalen glacier scattered to make any reliable correlations. Terraces at was isolated from the glacier in Lodalen, probably at the Åbrekk and Melkevoll at the inner part of Oldedalen 'break' 580 m a.s.l. In the lower part of Bødalen the ice (Fig. 5) reach as high as 86 and 100m a.s.l., respectively, melted down vertically as deglaciation in Lodalen pro­ thus indicating a rapid retreat of the glacier in Oldedalen. ceeded. In Nesdalen a significant, narrow terraced mar­ ginal moraine is situated in the eastern valley side (Fig. 5). It is located 600 m a.s.l. descending to 550 m a.s.l. at the valley bottom further to the south. Beneath this terrace Degree of rock surface weathering the thick till cover is heavily gullied. The terrace is interpreted to represent the upper surface of a valley The degree of rock surface weathering was measured at glacier in Lodalen in a late p hase of the deglaciation when sites in Oldedalen and Brigsdalen and on an altitudinal the connection to the glacier in Nesdalen had been cut off. transect from Loen to Skåla (McCarroll & Nesje 1993). At that time the ice surface in Lodalen at the mouths of The Schmidt hammer was useful only for distinguishing Nesdalen and Bødalen was at least 600 m a.s.l. The last sites covered during 'the Little lee Age' from those ice remnants in Nesdalen melted down as stagnant ice. deglaciated during the Lateglacial and early Holocene. As a result of the steep valley sides between 100 and Roughness of granitic augen gneiss surfaces was 1300 m a.s.l. in Kjenndalen, no deposits from the deglaci­ quantified from profiles measured in the field using a ation phase have been preserved. The deglaciation in micro-roughness meter and profile gauge. In the western Nesdalen and Bødalen indicates that ice supply from valley slope below Skåla there is a significant increase in Jostedalsbreen through Kjenndalen may have been main­ surface roughness above a distinct trimline at ca. 1350 m. tained longer than in Nesdalen and Bødalen. At the However, there was no significant increase above the mouth of Bødalen a glaciofluvial terrace is built up to l 00 higher blockfield boundary at ca. 1560 m. The vertical ice m a.s.l. This terrace has probably been deposited in a limits at Skåla await 10Be and 26 Al exposure da ting glacier-dammed lake (Lien 1985). (Brook et al. in prep.). NORSK GEOLOGISK TIDSSKRIFT 77 (1997) Glacial geology. Nordfjord-Jostedalsbreen 61

w E Preboreal Chronozone. (Rye et al. 1987). During this stage 8 the mean ELA depression has been calculated to 325 m. On the proximal side of the terrace at Melkevoll is an o.: ai 9 end moraine deposited by Melkevollsbreen. In addition, o two closely spaeed end moraines are deposited at the o o mouth of Brigsdalen, a tributary valley to Oldedalen. E 10 These two end moraines are deposited by Brigsdalsbreen f! as Local (Pedersen 1976). At both localities, the end moraines are Q) >. glaciation located well beyond the moraines of the 'Little lee Age', c: 11 . o formed at about AD 1750. Just above the 'break' in -e as o profile in Bødalen, prominent marginal moraines were o :c 12 deposited 600 m a.s.l., at a position 1-1.5 km beyond the as a: maximum extent of Bødalsbreen during the Little lee Age. A radiocarbon date on coal from a forest fire 13 l proximal to the moraine ridges gives a minimum age of o 20 40 60 80 100 120 140 2450 40 14C yr BP (Table l, T -4234) (Kvamme Distance (km) ± & Randers 1982). Fig. 8. Time/distance diagram for the deglaciation of Nordfjord. Thus, in front of Erdalsbreen, Bødalsbreen, Brigsdals­ breen and Melkevollsbreen terminal moraines have been mapped distally of the maximum extent of these glaciers during the 'Little lee Age'. Terminal moraines of possi­ Sea level bly the same age have been mapped east of Jostedals­ Fareth ( 1970, 1987) made a shoreline diagram on the basis breen also (Elgersma & Nesje 1978; Aa & Sønstegaard of marine terraces in Nordfjord. This was later somewhat 1987), and they are probably the result of a short-lived modified by Rye et al. (1987, Fig. 7). By extrapolating the climatic deterioration and reactivation of glaciers on the Younger Dryas shoreline, this reaches 11 O m a.s.l. at the Jostedalsbreen plateau at the end of the Preboreal inner part of Oldedalen and Lodalen. The terraces at Chronozone. This glacier readvanee has been termed the Melkevoll and Bødal were built up to 100 m a.s.l. This Erdalen event (Nesje 1992). shows that the deglaciation of the inner fjord- and valley areas subsequent to the Younger Dryas was very rapid, or that there has been a period of stable sea level, as recorded at Sunnmøre (Lie and Lømo1981; Lie et al. 1983; Svendsen The Holocene 1985; Svendsen & Mangerud 1987). Lien (1985) discussed Lithostratigraphic and palaeobotanical studies show that the possibility that the terrace 100 m a.s.l. in Bødalen may during the Hypsithermal (ca. 8000-6000 yr BP) the ELA have been deposited in a glacier-dammed lake with an ice was about 400-500 m higher than at present. As a result, remnant in Lovatnet, but it has not been possible to Jostedalsbreen probably disappeared entirely during that determine which alternative is correct. So far, no sign of period. The glacier formed again about 5300 yr BP. The vertical down-wasting of the glacier in Oldedalen has been firstsignificant glacier advance occurred between 3700 and found. The lack of terraces at the marine limits at the 3100 yr BP. The ELA intersected the mean modem mouth of Erdalen (Nesje 1984) and Sunndalen is inter­ elevation five times from ca. 2600 yr BP to the present. preted to be a result of down-wasting ice remnants in the basin of Strynevatnet, while higher-lying pass-points were already deglaciated. The 'Little lee Age' Torsnes et al. (1993) calculated the modem and 'Little lee Age' ELA of 20 valley glaciers from Jostedalsbreen. Using The Erdalen event an accumulation area ratio (AAR) of 0.6 ± 0.05 yielded At Vetledalssetra a prominent terminal moraine is de­ a mean 'Little lee Age' ELA depression of 70 m. By using posited across the valley bottom in Erdalen, built up by lichenometric evidence, Bickerton & Matthews (1993) a glacier draining down Erdalen (Fig. 5). A radiocarbon demonstrated that the maximum 'Little lee Age' advances date on gyttja proximal to the terminal moraine gave a at seven outlet glaciers occurred beween AD 1741 and minimum age of 8810 ± 130 14C yr BP (Table l, T-4839, 1863. Nesje 1984). The end moraine is situated about l km distal to the maximum extent of Erdalsbreen during the 'Little lee Age'. Conclusions This end moraine is deposited during readvances of glaciers at the Jostedal plateau, caused by a short climatic In Nordfjord,the fronts of the Yo unger Dryas fjord/valley deterioration, which probably happened very late in the glaciers were located in the fjord at , at 62 N. Rye et al. NORSK GEOLOGISK TIDSSKRIFT 77 (1997)

Anda/Lote, and at the western end of Homindalsvatn. metric- dating study of ice-marginal moraine sequences and their climatic Prominent lateral moraines along the fjord delimit the significance. Journal of Quaternary Science 8, 45-66. Blikra, L. H. 1986: Glasialgeologi og skråningsprosesser i Grasdalenog Skjerd­ glacier during this stage, the altitude of the glacier at the ingsdalen. Stryn, indre Nordfjord. Unpubl. thesis, University of Bergen. fjord head in inner Nordfjord being 1000-1100 m above Bugge, T. 1980: Øvre lags geologi på kontinentalsokkelen utenfor Møre og 44 sea level. Beyond and above the Y ounger Dryas valley Trøndelag. Continental Shelf Institute, publication no. 104, pp. Dahl, S. O. & Nesje, A. 1992: Paleoclimatic implications based on equilibrium­ and fjord glaciers in Nordfjord, local glaciers were line altitude depressions of reconstructed Y ounger Dryas and Holocene cirque formed, of which the glacier covering the Ålfoten area glaciers in inner Nordfjord, western Norway. Palaeogeography, Pa/aeoc/imato/­ 94, was the most extensive. The Yo unger Dryas ELA depres­ ogy, Pa/aeoeco/ogy 87-97. Elgersma, A. & Nesje, A. 1978: Kvartærgeologiske undersøkelser i Fåberg­ sion in middle and inner Nordfjord has been calculated stølsområdet, i kommune. Unpubl. thesis, og Fjordane at 450 ± 50 m, while the winter precipitation was reduced distriktshøgskule, . to about 60% compared to the present. Eikenæs, O. 1991: Kvartærgeologiske studiar på Strynefjellet og i tilgrensande område på Sunnmøre. Unpubl. thesis, University of Bergen. During the early Preboreal, the fjord glaciers retreated Fareth, O. W. 1970: Brerandstadier i midtre og indre Nordfjord. Unpubl. thesis, rapidly to the head of the fjord (Fig. 8), forming two ice University of Bergen. marginal deposits in each of the main valleys in inner Fareth, O. W. 1987: Glacial geology of the middel and inner Nordfjord. Norges geologiske undersøkelse Bulletin 408, 55 pp. Nordfjord. The final deglaciation in lower-lying valleys Giskeødegaard, O. 1983: Aukustiske undersøkelser av sedimentene i noen fjorder in Loen and Stryn was characterized by vertical down­ på ordvestlandet. Unpupl. thesis, University of Bergen. wasting in the bedrock basins presently occupied by the Hole, P. A. 1985: Kvartærgeologien i Glomsdalen. Stryn, indre Nordfjord. Unpubl. thesis, University of Bergen. lakes Lovatnet and Strynevatnet, respectively. Terminal Kaldhol, H. 1912: Nordfjords kvartæravleiringer. Bergen Museums Aarbok No. 3. moraines located up to l km beyond the 'Little lee Age' Kalstad, S. J. 1993: Kvartærgeologiske undersøkelser og verneverdier i Bygdaelv­ moraines surrounding Jostedalsbreen, dated at 9100 ± vassdraget, , Sunnmøre. Unpubl. thesis, University of Bergen. Kjenstad, K. & Sollid, J. L. 1982: lsavsmeltingsforløpet i Trondheimsfjorden. 200 14C yr BP, have been termed the Erdalen event after Glasialdynamiske prinsipper. Norsk Geologisk Tidsskrift 36, 153-162. the type site in Erdalen. The mean ELA depression Kvamme, M. 1984: Vegetasjonshistoriske undersøkelser. In Berge Meyer, O. during this stage has been calculated to 325 m, while the (ed.): - Stryn. Konsesjonsavgjørende botaniske undersøkelser. Rapport 34 Botanisk institutt, i Bergen, 238-275. mean winter precipitation was reduced to about 70% of Kvamme, M. & Randers, K. 1982: Breheimenundersøkelsene 1981. Arkeologiske modem values. During the 'Little lee Age', marginal rapporter 3, Historisk museum, University of Bergen. moraines were formed in front of the outlet glaciers from Larsen, E., Eide, F., Longva, O. & Mangerud, J. 1984: Allerød-Younger Dryas climate inferences from cirque glaciers and vegetational development in the Jostedalsbreen and by local cirque glaciers. The most Nordfjord area, western Norway. Arctic and Alpine Research 16, 137-160. representative 'Little lee Age' ELA depression in the Lie, S. E. & Lømo, L. 1981: En lito- og biostratigrafisk undersøkelse av marine Jostedalsbre region is calculated to be 150 m (Nesje et al. og limniske sedimenter i Ålesundområdet. Unpubl. thesis, University of Bergen. Lie, S. E., Stabell, B. & Mangerud, J. 1983: Diatom stratigraphy related to Late 1991), while Torsnes et al. (1993) calculated the average Weichselian sea-level changes in Sunnmøre, Western Norway. Norges geolo­ 'Little lee Age' ELA depression of 20 outlet glaciers from giske undersøkelse 380, 203-219. the Jostedalsbre as 70 m by means of the AAR Lien, R. 1985: Kvartærgeologien i Bødalen, Loen, indre Nordfjord. Unpubl. thesis, University of Bergen. approach. Mangerud, J. , Larsen, E., Longva, O. & Sønstegaard, E. 1979: Glacial history of western Norway 15,000-10,000 B. P. Boreas 8, 179-187. McCarroll, D. & Nesje, A. 1993: The vertical extent of ice sheets in Nordfjord, Acknowledgements. - This work is part of 'Fjordaneprosjektet' led by N. Rye with financial support from the University of Bergen. The work was also made western Norway: measuring degree of rock surface weathering. Boreas 22, possible by financial support from the Norwegian State Power System (Statkraft) 255-265. in connection with the planning of hydroelectric power development in the inner Nesje, A. 1984: Kvartærgeologiske undersøkingar i Erdalen, Stryn, Sogn og Nordfjord area (Breheimen-Stryn). Parts of the investigations were carried out in Fjordane. Unpubl. thesis, University of Bergen. connection with this planning. A. Reite kindly read the manuscript critically and Nesje, A. 1992: Younger Dryas and Holocene glacier fluctuations and equi­ suggested many improvements. Comments by reviewers improved the clarity of librium-line altitude variations in the Jostedalsbre region, western Norway. the paper. E. King corrected the English text of the final manuscript. E. Lier and Climate Dynamics 6, 221-227. & J. Ellingsen drew the figures and E. Loodtz typed the manuscript. To these Nesje, A., Anda, E., Rye, N., Lien, R., Hole, P. A. Blikra, L. H. 1987: The persons and institutions we proffer our sincere thanks. vertical extent of the Late Weichelian ice sheet in the Nordfjord-Møre area, western Norway. Norsk Geologisk Tidsskrift 2, 125-141. Nesje, A. & Dahl, S. O. 1992: Equilibrium-line altitude depressions of recon­ Manuscript received May 1995 structed Younger Dryas and Holocene glaciers in Fosdalen, inner Nordfjord, western Norway. Norsk Geologisk Tidsskrift 72, 209-216. Nesje, A. & Kvamme, M. 1991: Holocene glacier and climate variations in western Norway: Evidence for early Holocene glacier demise and multiple References Neoglacial events. Geo/ogy 19, 610-612. Nesje, A., Kvamme, M., Rye, N. & Løvlie, R. 1991: Holocene glacial and climate Aa, A. R. & Sønstegaard, E. 1987: Elvekrok BDE 085086-20, kvartærgeologisk history of the Jostedalsbreen region, western Norway; evidence from lake kart M. l :20 000. Norges geologiske undersøkelse. sediments and terrestrial deposits. Quaternary Science Reviews 10, 87-114. Anda, E. 1984: En topografisk-dynamisk modell for de preboreale breframrykk i Pedersen, K. 1976: , Vest-Norge. Glasialgeologiske undersøkelser. indre Sogn/, Vest-Norge. Meddelanden från Stockholms Universitets l og 2. Unpubl. thesis, University of Bergen. Geo/ogiska Institutionen N:r 225, 7. Reite, A. J. 1967: Lokalglaciasjon på Sunnmøre. Norges geologiske undersøkelse Andersen, B. G. 1979: The deglaciation of Norway 15,000-10,000 B.P. Boreas 8, 247, 267-287. 79-87. Rokoengen, K. 1979: Isens utstrekning og nedsenkne strandlinjer på kontinental­ Andersen, B. G. 1981: Late Weichselian ice sheets in Eurasia, Greenland and sokkelen. In Nydal, R., Westin, S., Havsten, U. & Gulliksen, S. (eds.): Fortiden Norway. In Denton, G. H. & Hughes, T. J. (eds.): The Last Great lee Sheets, i søkelyset. 14C-datering gjennom 25 år, 249-261. Laboratoriet for Radiologisk 20-27. John Wiley & Sons, New York. Datering, Trondheim. Bergstrøm, B. 1975: Deglasiasjonsforløpet i Aurlandsdalen og områdene om­ Rye, N. 1963: Kvartærgeologiske undersøkelser i noen dalstrøk i Sogn og kring, Vest-Norge. Norges geologiske undersøkelse 317, 33-69. Fjordane. Unpubl. thesis, University of Bergen. Bickerton, R. W. & Matthews, J. 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Rye, N., Lien, R., Nesje, A., Skjerlie, F., Faugli, P. E. & Husebye, S. 1984: Svendsen J. I. 1985: Strandforskyvning på Ytre Sunnmøre. Bio- og litostrati­ Breheimen-Stryn. Konsesjonsavgjørende geologiske undersøkelser. Rapport graliske bassengundersøkelser på Gurskøy, Leinøy og Bergsøy. Unpubl. thesis, Geo/. inst., avd. B. Univ. of Bergen, 158 pp. University of Bergen. Rye, N., Nesje, A., Lien, R. & Anda, E. 1987: The La� Weichselian ice sheet in Svendsen, J. l. & Mangerud, J. 1987: Late Weichselian and Holocene sea-level the Nordfjord-Sunnmøre area and deglaciation chronology for Nordfjord, history for a cross-section of western Norway. Journal of Quaternary Science 2, western Norway. Norsk Geografisk Tidsskrift 41, 23-43. 113-132. Sollid J. L. & Reite, A. J. 1983: The last glaciation and deglaciation of Central Sætrang, A. C. & Holmquist, E. 1987: Kartlegging av istykkelse på nordre Norway. In Ehlers , J. (ed.): G/acia/ Deposits in North-West Europe, 41-59. Jostedalsbreen. Norges Vassdrags- og Elektrisitetsvesen. Oppdragsrapport 8- A. A. Balkema, Rotterdam. 87. Stokke, J. A. 1980: Kvartærgeologisk kartlegging med oppfølgende sand- og Torsnes, I., Rye, N. & Nesje, A. 1993: Modem and Little lee Age equilibrium-line grusundersøkelser i Hjelledalen, M l :20 000. Norges geologiske undersøkelse, altitudes on outlet valley glaciers from Jostedalsbreen, western Norway: an Rapport 1560/31. evaluation of different approaches to their calculations. Arctic and Alpine Stokke, J. A. 1982: Løsmassekartlegging med oppfølgende sand- og grusun­ Research 25, 106-116. dersøkelser i Strynsdalen, . Norges geologiske undersøkelse, Vorren, T. O. 1973: Glacial geology of the area between Jostedalsbreen and Rapport 1560/21. , South Norway. Norges geologiske undersøkelse 291, 1-46.