Polarforschung 48 (1/2): 170-180, 1978

Extent and Regional Differentiation ofClacio-Isostatic Shoreline Variation In Spitsbergen *

By Gerhard Stäblein ..

Abstract: The v ar ious c auses of land-uplift in Svalbard, traces of which are found up to 100 m andhigher above sea level, are discussed. A method of identifying tenace sediments by means of morphometryand statistical comparison tests is demonstrated. The marine terraces in a profile from Bellsund toFreemansund are compared and described, and the former ice thickness is deterrnined from the ice-scourllm it . The land-uplift i s cons ldered to b e an old epirogenic lift tendency later modified by qlaclo­isostatic movement.

Zusammenfassung: Fragen nach den verschiedenen Ursachen der Landhebung in Svalbard, deren Spurenbis mehr als 100 m über NN reichen, werden diskutiert. Eine Methode zur Identifikation der Terrassen­sedimente mittels Morphometrie und statistischen Verqletchs tests wird vorgeführt. Für ein Profil vomBellsund Zum Freemansund werden die marinen Terrassen vergleichend beschrieben und die ehemaligeEismächtigkeit anhand der Schliffgrenze bestimmt. Die Landhebung wird als eine alte epirogene Hebungs­tendenz gewertet, der die qlazial-iscste tische Bewegung modifizierend aufgeprägt wurde.

1. ELEVATED SHORELINES IN SPITSBERGEN

A characteristic feature of the relief on Spitsbergen and the other islands of Svalbardis the occurrence of elevated shorelines on the co asts (Fig. 1). Some of these are wide,definitely marine terraces with a thick sediment cover, others are only narrow clifflines or rock terraces, found weil over 100 m above the present shore and whose marineorigin is not proved (Fig. 2). The evidence of changing levels of land and sea has oftenbeen investigated in Svalbard (BUDEL, 1960, 1968; SCHYTT, HOPPE, BLAKE & GROSS­WALD, 1967; SEMEVSKIJ, 1967; TROITSKIY et al., 1975; etc.).

In spite.of detailed research in various areas the question has not yet been settled as tothe respective importance of each of the different causes:

is this an endogenously caused uplift, or an exogenously caused sea-Ievel variation?is it an epirogenic movement, an after-effect of orogenesis, whose activity is shownby the adjustment of Tertiary and older strata, by neotectonic faults and by subre centvolcanism?is it a glacigenous movement, due to the formation and disappearance of one or morelarge arctie iee sheets during the Pleistocene ice ages?

Today, land-uplift in Svalbard, unlike that in Scandinavia, has come to an end. On manyexposed co asts of the archipelago active cliff formation shows that the coasts areretreating. This is due to the worIdwide rise in sea-level of about 1-2 mm!a as a resultof generally higher temperature and other developments of the ocean 1100rs.

In the 19th century JAMIESON (1882) had already linked the occurrence of beachterraces with the development of the ice cover. NANSEN (1922) applied these viewsto Spitsbergen, and HUDEL (1977: 45) emphasized again the role of glacial isostasy asthe decisive cause of raised shorelines in Spitsbergen. Locally, two effects overlap.Water from melting ice sheets causes a worIdwide rise in sea level. Compared with themaximum global glaciation of the last ice age 18000 years ago, glacio-eustatie trans-

• Paper presented at th e "Conference on Geophysics, Geology, Geomorphology and Geodesy of Spits­bergen", held by lhe German Soeiely of Polar Research in Hamburg, Oelober 2-3, 1978.

•• Prof. Dr. Gerhard Stäblein, Institut für Physische Geographie der Freien Universität, Altensteinstr. 19,D-1000 Berlin 33.

170

gression measures about 100 m (EMBLETON & KING, 1975: 168). Regionally, iee-reliefeauses land-uplift, which is at first an elastie reaetion. It is generally assumed that thepress ure of iee sheets thicker than 1000 m eauses compensation eurrents in thesuberust, resulting in a gravity deficieney. After the disappearanee of the iee burden,this deficieney leads, with a time lag, to glaeio-isostatie uplift of land, amounting to upto a third of the original, regionally varying iee thiekness, aeeording to differenees indensity (WOLDSTEDT, 1961: 295; EMBLETON & KING, 1975: 175).

Fig. 1: Series of beach ridges in Spitsbergen 5 km E of Langneset with view SW over Van Mijenfjordto Bromelld alen : on the southern fjord coast in the background is the main level, the 20 m beacnterrace. (Photo: STABLEIN, August 1968).

Abb. 1: Strandwallserien in Spitzbergen 5 km östlich Langneset mit Blick nach SW üher den Van Mijen­fjord gegen das BromelIdaIen; an der südlichen Fjordküste im Hintergrund das Hauptniveau, die 20 mStrandterrasse. (Foto: STABLEIN, Aug. 1968).

2. DATING OF SHORELINES AND COASTAL UPLIFT CURVES

The ehronologieal development of this postglacial proeess was reeonstrueted for Sval­bard by means of radioearbon dates. Whale bones, driftwood and shells found in themarine terraee sediments (SCHYTT et al., 1967) were 14C dated, together with a keyhorizon, especially widespread in the north, of pumiee deposited on the former shore­linse and due to a volcanie event oeeurring 6500 yearsago (BIRKENMAJER, 1958).

Corresponding diagrams by SEMEVSKIJ (1967), SCHYTT et al, (1967) show that upliftstarted earlier in the western part of Spitsbergen, and the upper marine limit shows lessuplift than in the east of the arehipelago (Figs. 1 and 7). In the west uplift oeeurredrapidly at first and then more and more slowly , further to the east uplift was moreregular. The height above present sea level does not represent the entire amount ofuplift, the eustatie sea-level rise must be added.

171

3. REGIONA<L DIFFERENTIATION

Within this general framework, I should now like to describe observations made in thecentral part of Spitsbergen from Bellsund with Van Mijenfjord and Van Keulenfjord asfar as Freemansund in SE Svalbard. Special attention will be given to

- the identification of marine terraces- the reconstruction of ice thickness- terrace division,

and the regional mechanism of movement will be considered. Our investigations followup those by BUDEL (1960, 1968). WIRTHMANN (1962, 1964, 1976) and GLASER (1968).carried out in thesixties within the framework of the Stauferland Expedition, whichI also took part in (cf. BUDEL 1972, 1977: 42-47; STÄBLEIN 1969).

Fig. 2: Recent cliff, beach terraces in 3 levels (8, 20, 47 m) and accordant structural terraces on thenorth coast 01 Van Keulenljord ne ar Strandvollsletta. (Photo: STABLEIN, August 1968).

Abb. 2: Rezentes Kliff, Strandterrassen in drei Niveaus (8, 20, 47 m) und akkordante Strukturterrassenan der Nordküste des Van Keulenljordes bei Strandvollsletta. (Foto: STABLEIN, Aug. 1968).

3. 1 Series of beach ridges

The present shore shows series of ascending beach ri.dges {Fiq. 1) at suitable sites in baysand at parts of the coast where ice has prevented wave action. Differences in age,increasing with height, are often also indicated by differences in colcur. Like BUDEL(1962: 343) we can distinguish a "white, green and brown series" 0Fig. 7). The lightcolour of the bottom series, up to 4 m above sea level, is intensified by a considerablequantity of bleached driftwood. The ·green series contains shore pools and is covered bya humid tundra with succulent green rnosses. In the W the series extends up to 15 m, in

172

the E to about 40 m above sea level. Weathering has al ready browned the pebble surfaceof the higher beach ridges and the vegetation changes according to drier habitat condi­tions. This brown series rises in the W up to 37 m above sea level; corresponding levelsin the E reach 60 m.

~Vergletscherteu.eisfreieGebiete

~ GLACIATED AND UNGLACIATEDAREAS

/?~O~ 200m ;~~~~~~e

__':......-, Verwerfungen- FAULTS

maximale Eisausdehnung mit__ ......... untermeerischen Moränen

MAXIMUM OF ICE EXTENSIONWITH SUBMARIN MORA/NES

Höhe des SchliffgrenzniveausALTfTUDE OF THE fCE -SCOUR UMIT

obere marine GrenzeUPPER MARINE LIMIT

höchste marine FossilfundeHfGHEST OCCURENCE OF MARINEFOSSILS

Fig. 3: Glaciation limit in Spitsbergen, ice-scour limits and upper marine limit fram Bellsund 10 KongKarls Land.

Abb. 3: Vereisungsgrenze Spitzbergens, Schliffgrenzhöhen und obere marine Grenze vom Bellsund bisKong Karls Land.

3. 2 Main level, clift and bar terraces

In the Bellsund area the 20 m terrace is particularly broad ~Fig. 4), a sign that thesea-Ievel remained active at this level for an especially long time (cf. Fig. 7). Therefollow terrace remnants at different heights up to 60 m above sea level. These often endin a fossil cliff, In almost all medium-sized valleys, prominent terrace bars occur atabout 85 m (Fig. 5). The bar does not occur in some of the large valleys.

These bars consist of coarse pebbles up to 20 cm in diameter in a sandy groundmass.Marine traces could not be found in the W but were clearly visible in the bar terraces

173

in the E (BUDEL, 1968: 1). The formation of the bars must have been a complex geo­morphological process, taking place at different per iods. We assurne that the barsoriginated as glacially compressed valley fills, which were previously deposited fluviallylike deltas, and, after compression, were levelled off to a lateglacial marine terrace by85 m sea level, which prevailed in different regions at different firnes. Since, to someextent, glaciers were still flowing in the larger valleys at this time, bar terraces couldnot be Iormed there.

3.3 Structural slope-steps or higher marine terraces?

On the slopes terraces occur even higher, over 250 m above sea level. Orten their non­horizontal position, concordant with the rock basement, shows that they are structural

Flg. 4: Calypsostranda and Scottbreen w i th Renardodden and Cape Lyell S 01 Bellsund (view to SW).Be adi terraces partlyon ice-scoured bedrück with pebbles of the shoreline up to 80 m, above on themountain flanks to the W (photo, right) 01 Seottbreen a pronouneed iee margin terraee at 110-130 m ,(Photo: Norsk Polar Institutt, 1936).

Abb. 4: Calypsostranda und Seottbreen mit Renardodden und Kap Lyell südlich des Bellsunds (Blick nachSW). Strandterrassen z. T. auf glazial geschliffenem Anstehenden mit Brandungsgeröll bis 80 ruf darüberan den Bergflanken westlich (rechts im Bild) des Seottbreen markante Eisrandterrasse in 110 bis 130 mHöhe. (Foto: Norsk Polar Institutt 1936).

174

slope-steps and not marine terraces. At Bellsund we found marine evidence only up to60 m, and at Freemansund the marine limit was set at 110 m (BUDEL, 1977: 45). On theKong Karls Land Islands, the marine limit was established at 145 m (BUDEL, 1968: 7)(cf. Fig. 1).

Pebbles are still frequently found on the higher slope-steps. So me of them could :comefrom weathered conglomerates (GLASER, 1968: 4: STABLEIN, 1969: 128). The questionolten remains open: are the pebbles pebbles of the shoreline or not? To answer thisquestion we used morphometry and test statistics (cf. STABLEfN, 1970, 1972).

The recent shore gives us the norm for typical shoreline pebbles. In shape they areclearly distinguishable Irorn the pebbles of a glaciofluvial river bed. If the frequencydistribution of the roundness values o f a sediment is compared with the frequency

Fig. 5: N coast of Edgebya on Freemansund in SE Sv alb ar d. view VI over Storfjord. Beaeh t er r a ces up to60 m , rising e as tw ar d , above, structural terraces and in the valley exit rernnants of th e bar series at 70 m.(Photo: Norsk Polar Instilutl, 1936).

Abb. 5: Nordküste der Edgeöya am Preemansund in SE-Svalbard, Blick nach W über den Storfjord.Strand terrassen bis rd. 60 m , nach E zu ansteigend; darüber Strukturterrassen und in den TalmündungenReste der Riegelserie um 70 m, {Poto : Norsk Polar Inslitutt 1936).

175

distribution of indisputably shoreline pebbles (Fig. 6). the Kolmogorov-Smirnov testdecides whether the two distributions differ significantly or not. The xlecision is basedon the fact that if the supremum of both the curves, i. e. the greatest distance, is greaterthan the valid critical value of the test based on the required level of significanceaccording to a theoretical probability function, there is a significant difference. If thesupremum is smaller, both distributions of the shape index show no significant diffe­rences, i. e. they are similar in shape. This means that the coarse sediment which wascompared with the shoreline pebbles is with high probability also shoreline pebbles.With this method of identification, lithologieal differcnccs must be considered and onlycorresponding sampies should be compared. With this method it was possible to identifya terrace as a marine form although there were no definitely marine fossils such as shellsor whale bones and only shoreline pebbles occur.

%

z,

500

2rZj = 1'1000

250

/-----1 --:?x/-1 ,__1 .../

-----,---- l~-::J----·-

//1 I/l/'---// 1/ /// /1 TB / CDTerrassengerölle

/ /1 -- T PEBBLES OF MARINE TERRACE;'

,i dSB ~ / ® Brandungsgerölle•• uvu /1.

1

// BPEBBLES OFTHESHORELINE

/ / !// n ® glazifluviale Schotter;' i. / // GLACIOFLUVIAL PEBBLES

/ i /

/i I //,'! /1_-I // 1/........ __ 1-

Ot-I---r',''--/-~l'''''''- ~---,- ---~.--.- -1-------r-u.

o

11

501

1001:2: %

Fig. 6: Morphometric diagrams of pebble sam p le s (sandstone 2-15 cm 0) from Van Keulenfjord; s amplaT marine terrace at Strandvollsletta, samp le S highwater bed in Ulladalen, semple B re cent beach ineastern Van Keulenfjord. Test value clx? greatest distance betwecn two compared cumulative curvesof {}/o~frequencies; critical value of the test D = 23.05 for s amp les of 100 pebb les and with a level ofsignificance of 99"/0 (SACHS. 1972: 228). As d S ß ~ 58 and dTB = 22. th e sampies T and B do not differsignificantly, following the Kolmoqorov-Smirnov tcs t : sampIes Sand B, however, are significantlydifferent as regards roundness index z.

Abb. 6: Morphometrische Diagramme von Geröllproben (Sandsteine 2-15 cm 0) vom Van Keulenfjord.Probe T marine Terrasse an der Strandvollsletta, Probe S Hochwasserbett im Ulladalen, Probe B rezenterStrand im östlichen Van Keulenfjord. Testgröße dx y größter Abstand zweier verglichener Summenkurvender v/o-Lleunqkaiten , Testsschranke D '-= 23,05 für Proben von je 100 Geröllen und mit einer Sicherheits­wahrscheinlichkeit von 99°/0 (SACHS 1972: 228). Da d S Il ~ 58 und d TI l = 22. unterscheiden sich nach demKolrnoqorov-Smirnov-Test die Proben T und B nicht signifikant; die Proben Sund B jedoch sind signifikantunterschiedlich bzgl. des Zurundungsindex z.

3.4 lee margin terraces

As well as structural slope-steps a further feature is found, particularly in the Bellsundarea. These forms are not beach terraces, in spite of a similarity of shape. They arepronounced steps at a height of 120-100 m, sloping down westwards and rising towardsthe valleys. In places (e. g. Cape Lyell, Fig. 4) such steps in the bedrock are glaciallyformed into ice-scour steps and spread with moraine material. The present form is a

176

lateglacial iee margin phenomenon from aperiod of iee retreat during only low regionalglaeiation. TROITSKIY et al. (1975) classified this as a marine terraee and thus spokeof a marine terraee at 120 m here at Bellsund.

3. 5 Terraee diagram and regional comparison

A eomparison of observations shows that the elevated shorelines in the Bellsund andFreemansund areas are similarly struetured, but the eorresponding terraees reaehgreater heights in the E. The upper marine limit in the E is 110 m (aeeording to 14C datesthis was the sea level 11.000 years aga). In the W, in the Bellsund area, it is probably90 m but up to now only 60 m eould be proved. Aeeording to the elimatie conditionsat the time of their origin, the various terraee series vary as to the domihance of thefossil molluscs, marine snails and shells, as has been proved in detail for the Isfjordarea (FEYLING-HANSSEN, 1955, 1965a).

264 Strukturterrassen (?)$TRUCTURAL TERRACES

250

BELLSUND

9400 7500 5000

Pn s t pla z i a l e WarmezeitPO$TGLACIAL WORM PERIODE

685-112 m

FREEMAN SUND

Braune StrandwallserieBROWN SERiES OF BEACH R/DGES

RiegelserieBAR SERIES

Grüne StrandwallserieGREEN SERfES OF BEACH RiDGES

110-120{?) EisrandterrassenICE MARGIN TERRACES

GrenzplattenUNIT PI.ATS

mf90

'30

c:

~ 10170 C/)

» co

~2of60 (I)

--l

2400

SUBBO REAL SUBATLANTIC

8

BOREAL ATLANTIC

+----------10 9

Fig. 7: Series of beach terraces at Bellsund and Freemansund compared to curves of eustasy andisostasy (aiter FAIRBRIDGE, 1961, quoted fr om EMBLETON & KING, 1975: 169; SCHYTT et al., 1967;SEMEVSKIJ 1967b; BUDEL, 1968 and own surveys).

Abb. 7: Strandterrassenserien am Bellsund und Freemansund im Vergleich zu Kurven der Eustasie undIsotaste (nach FAIRBRIDGE 1961, zitiert nach EMBLETON & KING 1975: 169. SCHYTT et a1. 1967. SE­MEVSKIJ 1967b. BUDEL 1968 und eigenen Auinahmen).

JAHN (1959) has found terrace structures in Hornsund which correspond to those atBellsund. He tao does not settle the question of the origin of the top levels above 65 mwhich eontain pebble layers but no conclusive marine evidence. The comparative mo r­phometric tests suggested above could perhaps help here (cf. JAHN, 1968).

A comparison with results from FEYLING-HANSSEN (1965b) fram the Bille- and Sassen­fjord in the inner Isfjord area praves interesting because of the available absolute 14C

dates (cf. Fig. 7). An analogaus age to the Bellsund terraces seems probable. The curveof uplift shows the eustatic transgression, which, partieularly in the pcstqlacial warmperiod (Atlantic 7500-5000 years b. p.) led to a temporary standstill in coastal

177

development. Isostatie land-uplift and eustatie sea-Ievel rise took plaee fairlyregularly during this period.

Especially remarkable is the age of the 84.5 m terraee of the Billefjord, whieh was datedat 21300 b. p. Prior to this dating, it had been assumed that iee pressure was then stilleffeetive. This supports the view that at least some parts of eentral Spitsbergen wereiee-free at this time and that the uplift tendeney began earli er than the last iee relief.LAVRUSHIN (1967) interpreted OLSSON & BLAKE's (1962) HC dates of 35 to 40000years b. p. for beaeh terraces on Nordaustlandet as an indieation of a mostly iee-freeinterstadial.

The presenee of end-moraines (see, for example, the striking examples in the Bellsundarea near Collinderodden on Van Mijenfjord) also suggests regionally varying, repeatediee reliefs and, as a result of glaeial re-advanees, new and eonsiderable iee burdens.During such stages the elevated shorelines sank again. Regionally pronouneed stageswere distinguished for the Billefjord ("Billefjord stage") and for Bellsund ("Bellsundstage") on the basis of Pleistoeene sediments (SEMEVSKIJ, 1967a). So the glaeigenouspart of the land uplift should not be regarded as just the result of the deglaeiation of alarge Barents Sea iee-sheet (a hypothesis last put forward by HUGHES et al. (1977)).Younger glaeier oseillations, as BUDEL (1960) dedueed from observations in the Freeman­sund area, have also led to regional shoreline variations. This .is supportedby thestudies earried out in northern Spitsbergen by BOULTON & RHODES (1974), who pointedto the effeets of lateglacial oseillations there.

Cliff formations on the west eoast and in SE Svalbard - e. g. on the eoast ofAxelöyain Bellsund or on the west eoast of Edgeöya (cf. WIRTHMANN, 1964; GLASER, 1968: 18)

show that land-uplift does not take plaee today. It is eoneeivable that the presentland subsidenee is a last lagging reaetion of the powerful glacial re-advanee in the19th eentury. Most of the individual glaciers show no older moraines apart fromthe terminal moraines from this most reeent advanee. The present-day glaciers havethus reaehed their Holoeene maximum stage (STABLEIN, 1969). In many plaees, thesere cent glacier advanees passed over postglacial beaeh terraces whieh had been depositedin an iee-free are a: In eomparison, the glaeier burden must have been eonsiderablyless during the postglaeial warm period than today.

4. ICE-SCOUR LIMIT AND MAXIMUM ICE THICKNESS

It is diffieult to establish by direet means the extent of former iee burden in the Free­mansund area, beeause the eompletely seoured form of the just under 500 m lowplateaux shows that the ice eap must onee have been very mueh thieker (Fig. 5),

In the Spitsbergen fjords in the W, the mountains (sometimes higher than 1200 m)clearly show an iee-seour limit, the extent of earlier erosion by the iee masses flowingwestward through the fjords (Fig, 4). In southern Nordenskjöld-Land the top ice lirrerises from 400 m at the entranee to Bellsund to 550 m at Ingeborgfjellet and 780 m atLitledalsfjellet, reaehing 800 m at Liljevalchfjellet. In aeeordanee with the glacier snoutform, familiar to us from re cent glaciers, we must assurne that Pleistoeene lee ean haveextended only a few kilometres beyond the west eoast of Spitsbergen (Fig. 3). This wasproved in the last years by the existenee of submarine moraines on the flat shelf offSpitsbergen (LIEST0L, 1972).

5. THE MECHANISM OF LAND-UPLIFT MOVEMENT

Contrary to this established inerease in iee hurden from W to E, land uplift in the W,particularly in the area of Bellsund and its hinterland, does not vary, Here, the marine

178

terraees run predominantly horizontally, parallel to the eurrent sea-Icvc! along thefjord eoasts whieh noteh 70 km inland. It is only beyond the big N-S striking, strueturerletermining faults and the Storfjord qr oo ve further E that the uplift of the eomparablelevels is greater and inereases ees t s ards, eorresponding to the inereased iee burden.

This suggests the eonclusion that uplift did not oeeur as a regionally differentiatedeontinuous proeess that ean be reprodueed aeeurately by interpolated isobases, as inthe ease of the postglacial domal uplift of the Fennoseandie shield. Whilst W ofSvalbard Spitsbergen with its Caledonian-eonsolidates basement reaeted bloekwise tothe ice-burden, the geologieally more eontinuous southeast was buekled aeeording tothe varying pressure.

6. CONCLUSIONS

To return to our original question of how great a share should be attributed to thevarious eauses of the regionally differentiated shoreline displacements:

Observations to date indieate that uplift in Svalbard was not just a glacio-isostatieproeess but also the elastoplastie endogenous re action of the earth's erust to exogeniestress through Quaternary ice burden and iee reli ef, whieh modifies an older epirogenieuplift tendeney and is due to the neotectonic plate development in the area (cf.SEMEVSKIJ, 1976). - This thesis is supported by a eomparison with Greenland, whe rewe earried out similar research on land uplift (STABLEIN, 1975). In Greenland, theextent of postglaeial eoastal development whieh is doeumented by marine evidenee issimilar, although the Greenland iee sheet still exists today and postglaeial iee relief ispresumably on the whole less than in Svalbard, where the iee-age Barents Sea iee­sheet as such has disappeared. The eauses of longterm uplifts must be older than theiee age and are to be found in postorogenie shield developmen t. Regional differentiationindieates that upper Quaternary land-uplift was only temporarily more or less redueedby probably several phases of iee retreat and advance with regionally varyingglaciation.

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BI a k e, VV. (1961): Radi ocarb on dating of raised beaches in Nordaustlandet, Spitsbergen. - In: G. O.Re as ch , ed .• Geology of the Arctic 1: 133-145, Toronto.

B 0 u I ton, G. S. & M. Rho des (1974): Isostatic uplift end glacial history in northern Spitsbergen.- Geol. Mag. 111: 481-500.

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and Chemistry of the Eer th 4: 99-185, New York.Fe y I i n g - H ans sen, R. W. (1955): Stratigraphy of th e marine le te Pleistocene of Billefjorden,

Vestspitsbergen. - Norsk Polarinst. Skr. 107: 1-186.

Fe y I i TI 9 - H ans sen, R. W. (1965a): A marine seetion from the Holocene of Talavera on Barentsöyain Spitsbergen. - Erqebn. Stauferland-Expedition 1959/60, 3 (Vorträge des Pv-Nanscn-Gcd ächtnis­Symposiums über Spitzbergen 1961 in Würzburg) : 30-58, Wiesbaden.

Fe y 1 in g - H ans sen, R. W. (1965b): Sh or el i ne dtspl acement in central Spitsbergen. - Ergebn.St aufer lan d-Exp ed i tion 1959/60, 3 (Vorträge des F.·Nansen·Gedächtnis-Symposiums über Spitzbergen1961 in Würzburg) : 24-28, Wiesbaden.

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GI ase r , U. (1968): Junge Landhebung im Umkreis des Storfjord (SO-Spitzbergen). - Würzburger Geogr.Arb. 22 (II): 1-22, Würzburg.

H u 9 h es, T., Den ton, G. H. & H. G. G r 0 s s wal d (1977): Was there a late - Würm Arelielee Sheet? - Nature 266: S96-602.

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