Quaternary marine stratigraphy and geochronology in central West Greenland

Quaternary marine stratigraphy and geochronology in central West Greenland OLE BENNIKE, KAREN BILLE HANSEN, KAREN LUISE KNUDSEN, DAVID N. PENNEY AND KAARE LUND RASMUSSEN

Bennike, O., Hansen, K. B., Knudsen, K. L., Penney, D. N. & Rasmussen, K. L. 1994 (June): Quaternary marine stratigraphy and geochronology in central West Greenland. Boreas, Vol. 23, pp. 194-215. Oslo. ISSN

A new stratigraphic framework is proposed for the Quaternary of a portion of central West Greenland, based primarily on faunal and geochronologic studies of shallow shelf deposits. Twenty-four occurrences of pre- Holocene deposits were already known in West Greenland and data from 18 new sites are presented, together with new information on some of the previously described localities. Four pre-Holocene marine events are described. The interglacial Ivnaarssuit and Nordre Laksebugt marine events are considered to be Middle Pleistocene in age. The interstadial Laksebugt marine event is considered to be late Middle Pleistocene, whereas the Svartenhuk marine event is correlated with the last interglacial. For the last glacial period an extensive ice shelf is proposed west of Disko. The oldest postglacial deposits are dated at 10,470 Ole Bennike, Geological Survey of Denmark, Thoravej 8, DK-2400 Copenhagen NV, Denmark and Geological Museum, University of Copenhagen, 0ster Voldgade 5- 7, DK- I350 Copenhagen K, Denmark; Karen Bille Hansen, Zoological Museum, University of Copenhagen, Universitetsparken IS, DK-2100 Copenhagen 0, Denmar$; Karen Luise KnutiSen & David N. Penney, Department of Earth Sciences, University of Aarhus, DK-8000 Arhus C, Denmark; Kaare Lund Rasmussen, Carbon- 14 Dating Laboratory of the National Museum and Geological Survey of Denmark, Ny Vestergade 11, DK-1471 Copenhagen K and Department of Physics, University of” Odense, Campusvej 55, DK-5320 Odense M , Denmark; 11th January, 1993 (revised 20th September, 1993)

B o r n 0300-9483.

130 I4C-years BP.

The northern and central parts of West Greenland contain numerous deposits related to several interglacial/glacial cycles. Marine deposits in central West Greenland have been studied by Rink (1853), Steen- strup (1883, 1901), Laursen (1944), Donner (1978), Simonarson (1981), Funder & Simonarson (1984), Kelly (1985, 1986), Frich & Ingolfsson (1990) and Ingolfsson et al. (1990). Review articles on the Qua- ternary geology of Greenland include Weidick ( 1976) and Funder (1989).

The bedrock geology of the region is characterized by plateau basalts forming plateaux dissected by U- shaped valleys and cirques, as well as by steep-sided fjords, bays and straits. The topography contrasts strongly with the undulating gneissic terrains that occur both north and south of the region. Major parts are covered by local glaciers, whereas the western margin of the Inland Ice is situated 100-200 km inland. The mean July temperature is around 6°C and the mean annual temperature is around -4°C.

Today the region is strongly influenced by the north- ward flowing West Greenland Current that transports relatively warm Atlantic water to the region, and which supports a rich population of the common mussel Mytilus edulis in littoral waters of western Disko (Fig. 1). The species is less common on southwestern Svartenhuk Halva at present, possibly due to long-lasting sea ice cover (until mid-summer). Svartenhuk Halva is at the present northern limit for continuous populations. However, isolated populations occur in the Thule region further north (Funder & Simonarson 1984). Mytilus edulis and the more cold-tolerant sublit-

toral bivalve Chlamys islandica are here called subartic species (Dunbar, 1951). They have a present northern limit in the Thule area. The remaining zoogeographical terminology follows Feyling-Hanssen ( 1955).

The major objective of this paper is to describe marine deposits along a 250 km transect extending from the western shores of Disko northwards to Nu- ussuaq and Svartenhuk HalvA, West Greenland. Fieldwork was carried out by 0. Bennike in 1989. This work concentrated on locating the deposits and sampling for faunal and geochronologic analyses. Thus detailed lithostratigraphic and sedimentologic work remains to be done.

Modern distributions and taxonomy of Bryozoa follow Hansen (1962), Hayward ( 1979), Kluge ( 1962, 1975), Levinsen (1914, 1916), Maturo & Schopf (1968), Osburn (1936, 1950, 1952), Powell (1968) and Ridley ( 1881). Foraminifera and Ostracoda are housed in the Department of Earth Sciences, Arhus, whereas Bryozoa are housed in the Zoological Mu- seum, Copenhagen. The remaining fossils are housed in the Geological Museum, Copenhagen.

Spelling of Greenlandic place names follows the current orthography, which differs slightly from those on the topographical maps (the Patofik beds of former authors are spelt as the Pattorfik beds).

Dating methods Samples have been radiocarbon dated at the Carbon- 14 Dating Laboratory of the National Museum and

BOREAS 23 (1994) Marine sediments, W. Greenland 195

W 0 n z Z 4 -

9 HALV0 I_II 4 11 KU ssineq

I 20km J 550 5 4 0

'1 NUUSSUAQ

70"

Laksebugt

DISK0 BUGT

I 20km I 4 8 r . Kronprinsen Ejland %P 690

54"W %9

Fig. I . Locality map.

196 Ole Bennike et al. BOREAS 23 (1994)

Table 1. Macrofossils in pre-Holocene deposits from central West Greenland. For locations see Fig. 1.

Locality number Sample number GCI 74-

1 1 2 3 4 5 6 7 8 9 947 948 949 946 945 937 932 930 931 938

POLYCHAETA + + + - + + Caulostrepsis isp. - - - -

Spirorbis granulatus (Linnaeus, 1767) - - - - - - - - - - S. cf. spirorbis (Linnaeus, 1758) - - S. cf. uerruca (Fabricius, 1780) - - - -

S. vitreus (Fabricius, 1780) - - - _ - - - - -

GASTROPODA Scissurella crispata Fleming, 1832 - -

Puncturella noachina (Linnaeus, 1771) - - - _ - - - - - -

Acmaea rubella (Fabricius, 1780) - -

Moelleria costulata (Meller , 1842) - -

Alvania scrobiculata (Mraller, 1842) - - - _ - - - - - - Boreocingula castanea (Meller, 1842) ’ - - - - - - - - - - Trichotropis borealis (Broderip & G. B. Sowerby, 1829) - -

Natica sp./Lunatia sp. - -

Oichnus isp. - -

Trophon truncatus (Strom, 1767) - -

Colus gracilis (da Costa, 1778)2 - - - - _ - - - - - Buccinum sp. - -

Admete oiridula (Fabricius, 1780) ’ - - - - - - - - - -

Oenopota cf. exarata (Mdler, 1 842)2 - - _ _ _ _ - - - -

Cylichna alba (Brown, 1827) - - _ - _ - - - - -

Nucoloma belloti A. Adams, 1856 - - - - - - - -

Nuculana minuta (0. F. Miiller, 1777) - - - - _ - - - - -

Yoldia hyperborea Torell, 1859 - - - - _ - - - - - Portlandia arctica (Gray, 1824) ++ - Yoldiella fraterna Verrilli & Bush, 1898 - - - Yoldiella lenticula (Mraller, 1842) - - - - _ - - - -

Musculus sp. Actinula greenlandica (G. B. Sowerby, 1842) Chlamys islandica (0. F . Miiller, 1776) - - - - _ - - - - - Astarre borealis Schumacher, 181 7 + + + + + + + - ++ + + +++ - + + - A. elliptica (Brown, 1827) - -

A. montagui (Dillwyn, 1817) + A. montagui var. stria fa - - - A. montagui var. warhami - - - Cerastoderma elegantulum ( Mraller, 1842) - - _ Clinocardium ciliatum (Fabricius, 1780) - - Serripes groenlandicus (Bruguitre, 1789) - - - Macoma calcarea ( Gmelin, 1790) - - _ -

M. loueni (Jensen, 1905) - - - _ - - Cytodaria kurriana Dunker, 1862 - - - - - - Mya truncata Linnaeus, 1758 + + +++ + + + + + + + + ++ + + ++ Hiatella arctica (Linnaeus, 1767) + + +++ + + + + + + + + +++ + + + Pandora glacialis Leach, 18 19 - - - CIRRIPEDIA Balanus balanus (Linnaeus, 1758) - - - Balanus sp. BRACHIOPODA Hemithirrs psittachea (Gmelin, 1790) * - -

ECHINODERM ATA Ophiura sarsi Liitken, 18553 - - Strongylocentrotus droebachiensis (0. F. Miiller, 1776) - - -

Gadus ogac Richardson, 18364 - - - -

Gadus morhun Linnaeus, 1758/G. ogac - - - Alle alle (Linnaeus, 1758) - - -

- - - - - - - - - - + - + +

- - - - - - - -

- - - _ - - - - - - - - - - - -

- _ _ - - - - - - - - - - - + -

- _ _ - - - - - - - _ _ - - - -

+ - - _ _ - - -

BIVALVIA - ++

+ + - - +

+ +

- - _ - - _ - - - -

- - - - _ - - - - - - - - - - - _ - +

- - - - - - - + - - - - - + + + -

+ - _ _ - - - - _ - - - - + - - - - - - -

- + - - - - - - - - - - - - -

+ - - - + - - - - - - - - -

- - _ - - - -

- - - - - - _ - - - - - - - + - -

- _ - - - - - -

- - _ - - - - -

+ - - - + - + VERTEBRATA

- _ - - - -

- - - - _ _ - - - - - - - - -

+ /+ + / + + + : Frequency, ?: Identification uncertain. 1-5 identified by A. Wartn, Swedish Museum of Natural History, Stockholm, Sweden ( I), J.-A. Sneli, University of Trondheim, Norway (2), J. Kjennerud, Zoological Museum, Bergen, Norway (3), I. B. Enghoff (4) and K. Rosenlund (9, both at the Zoological Museum, Copenhagen, Denmark. * Often misspelled Hemithyris.


9 10 10 1 1 12 12 13 14 15 16 17 21 26 27 36 39 42 42 939 940 941 942 950 951 859 857 856 851/3 928 873 922 926 901 904 892 893


the Geological Survey of Denmark, Copenhagen, Denmark (samples marked K); at RCD Radiocarbon Dating, Hanvell, England (samples marked RCD) ; at Teledyne Isotopes, Westwood, New Jersey, USA (samples marked I) and at The Svedberg Laboratory, Uppsala, Sweden (samples marked Ua, by accelerator mass spectrometry).

Shells dated in Copenhagen were etched in dilute hydrochloric acid until 10% of their weight was dis- solved in order to remove possible surface contamina- tion, but are otherwise untreated. Shell samples dated at Teledyne had 25% of their mass removed by acid treatment, whereas samples dated at RCD had 33% of their mass removed prior to dating. The gyttja sample dated in Copenhagen was treated with 3% hydrochloric acid followed by rinsing in deionized water. Stan- dard procedures have been used in calculating the ages (Mook & Waterbolk 1985). 6 13C was measured on all samples dated in Copenhagen, at Teledyne and at RCD, but not on samples dated in Uppsala.

The dates on marine shells from Copenhagen are corrected for isotopic fractionation according to measured values of 6I3C by normalizing to 613C= O.O%,PDB. The date of the gyttja sample dated in Copenhagen is corrected for isotopic fractionation by normalizing to 6 I3C = - 25%, PDB.

Shell and marine bone dates from RCD and Tele- dyne are supplied in a form where they are corrected for isotopic fractionation according to measured values of 6I3C by normalizing to 613C = -25% PDB. We have corrected these dates for isotopic fractionation by normalizing to 6 13C = O.O%, PDB (a correction of 400 years) and the dates are thus directly comparable. The reason for this is the (haphazard) coincidence that the reservoir effect in these waters correspond to this correction (Krog & Tauber 1973). Dates on marine and terrestrial samples given in this paper are thus directly comparable. No further reser- avoir effect is believed to be present.

The shell samples dated at the Tandem Accelerator Laboratory in Uppsala are assumed to have 6 13C = O.O%, PDB, while the bone samples are assumed to have 6I3C = -21% PDB, and terrestrial samples 6I3C = -25%, PDB. All samples are supplied in a form normalized to 6I3C = -25% PDB. In order to obtain comparable ages and to correct for the ocean reservoir effect as described above, the marine dates have been corrected to 6 I3C = 0.0% PDB by subtracting 400 years, while the date of the terrestrial sample has not been corrected further.

Thermoluminescence (TL) dates and optically stim- ulated luminescence (OSL) dates, which were made at the Nordic Laboratory for Luminescence Dating at Riser, Denmark, are corrected for the effect of shallow traps (Mejdahl et al. 1992).

Amino acid analyses were performed at Bergen Amino Acid Laboratory (BAL) in Norway, results of which are compared with previous results of Green-

landic material from the Amino Acid Geochronology Laboratory (AAL) at INSTAAR, Boulder, USA. The analyses from the two laboratories are directly comparable (Wehmiller 1984), but amino acid analyses performed in Boulder prior to 1982 are subject to laboratory fractionation (Miller et al. 1982) which renders comparisons difficult (Kelly 1986). All analyses were made on the marine bivalves Hiatella arctica and Mya truncata which have similar racemization rates (Miller & Mangerud 1985).

Results and discussion The pre-Holocene deposits are grouped into four marine events on the basis of radiocarbon, TL and OSL dates, amino acid ratios and faunal content.

Ivnaarssuit marine event

The sea cliff section with marine deposits near Iv- naarssuit, western Disko (loc. 36, Fig. l), was origi- nally described by Steenstrup (1883, as ‘Kasigisat’). The exposure reveals 2 m Tertiary basalt, overlain by 140cm sublittoral gravel with shells, followed by up to 80 cm red clay/slit with scattered stones and 8 m ‘breccia’ consisting of angular basalt blocks with little matrix and rare gneiss erratics. The cliff is overlain by 1-2m Holocene beach gravel. It appears that the ‘breccia’ was formed by frost-shattering of the basalt bedrock, and has been moved by slope processes.

The macrofauna from the sublittoral gravel is relatively poor with 9-1 1 taxa (Table l), but two of them, Chlamys islandica, which occurs with whole shells, and the snail Trophon truncatus, are indicative of coastal water temperatures like those of today or perhaps slightly colder (Thorson 1944; Funder & Simonarson 1984). The barnacle present in this deposit is Balanus balanus, not the boreal species Balanus hammeri (As- canius, 1767), as listed by Steenstrup (1883).

Seven species of encrusting bryozoans were recorded (Table 2), of which Escharella klugei is a subarctic, northern boreal species that is not recorded north of Disko. However, older records of E. ventri- cosa (Hassall) from the Thule area may represent this species, which was only established in 1979. The other species of Bryozoa are more widespread in arctic areas.

Two samples from the clay/silt unit at Ivnaarssuit were studied for their content of foraminifera. One sample was barren, but the other contained a diverse and specimen-rich assemblage (Fig. 2). Elphidium excavatum, Cassidulina reniforme, Islandiella helenae and Astrononion gallowayi dominate the fauna, and Buc- cella frigida calida, Haynesina orbiculare and Elphi- diella arctica are also relatively common. Some of the species recorded in this study are illustrated in Fig. 3. The composition of species indicates mainly arctic


Table 2. Bryozoa in Quaternary deposits from central West Greenland. For locations see Fig. 1.

Locality number 6 14 27 36 42 42 23 25 29 Sample number GCI 74- 932 857 926 901 892 893 923 920 912

Pre-Holocene - Holocene Age

CY CLOSTOMIDA Oncousoecia cf. diastoporides (Norman, 1869) 0. canadensis (Osburn, 1933) 0. polygonalis (Kluge, 191 5 ) Tubulipora sp. Idmidronea sp. Disporella cf. hispida (Fleming, 1828) CHEILOSTOMIDA, ANASCINA Electra arctica Borg, 1931 ?Caulorampus sp. Tegella sp. ?Tegella sp. Bidenkapia spitzbergensis (Bidenkap, 1897) Microporina articulata (Fabricius, 1824) Caberea ellisii (Fleming, 1814) CHEILOSTOMIDA, ASCOPHORINA Reginella spitzbergensis (Norman, 1903) Rhamphosromella radiatula (Hinks, 1877) Escharella connectens (Ridley, 1881) ’ E. indioisa Levinsen, 1916 E. klugei Hayward, 1979 ‘Escharella’ thompsoni (Kluge, 1955) Hincksipora spinulifera (Hincks, 1889) Lepralioides nordlandica (Nordaard, 1905) Smittina majuscula (Smitt, 1867) S. minuscula (Smitt, 1867) S. rigida (Lorenz, 1886) Smittoidea sp. Porella concinna (Busk, 1852) P. obesa Waters, 1900 Cystisella saccata (Busk, 1856) C. bicornis Obsurn, 1952 Schizoporella bispinosa Nordgaard, 1906 S. elmwoodiae Waters, 1900 S. pachystega Kluge 1929 Schizobrachiella stylifera (Levinsen, 1887) Stomachetosella cruenta (Busk, 1854) S. hincksi Powell, 1968 Pachyegis groenlandica (Norman, 1893) Myriapora subgracilis (d’orbigny, 1853) Myriozoella crustacea (Smith, 1867) M . plana (Dawson, 1859)2 Hippoporella hippopus (Smith, 1867) Celleporella hyalina (Linnaeus, 1767) Lepralliela contigua (Smitt, 1867) Celleporina surcularis (Packard, 1863) C. uentricosa (Lorenz, 1887)

+ + + + + + + - -

+ + + + + + + + + + + + + + + + + + + + + + + + + + + + + + + +

-

-

-

Contrary to Osburn (1936) Escharella connectens and E. indioisa are considered well-separated species. Myriozoella plana syn. Schizoporella costata Kluge, 1962.

ice-distal conditions, but there is a weak subarctic influence in the assemblage (see Gudina & Evzerov 1973; Feyling-Hanssen 1980).

The subarctic influence seen both in the molluscan, bryozoan and foraminiferal faunas, combined with the high foraminiferal diversity, suggests that the West Greenland Current entered the region during deposition and points to interglacial conditions.

Radiocarbon dating of shells yielded an age of >39,110 years BP (Table 3), and amino acid analyses

yielded mean aIle/Ile ratios of 0.117 0.013 and 0.345 f 0.019 in the HYD and FREE fractions, respectively (n =4 , Table 4, Fig. 4). By comparisons with mean aIle/Ile ratios of 0.54 and 0.97 in the HYD and FREE fractions, respectively, from the Early Pleistocene Pattofik beds (Funder & Simonarson 1984; Funder 1989; Knudsen unpublished) and mean ratios of 0.031 and 0.21 in the HYD and FREE fractions from the last interglacial Kaffehavn marine event (Kelly 1986), the Ivnaarssuit marine event is

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Fig. 3. Light microscope. photographs of foraminifera. 1-3 Elphidium excuuutum; specimens from Ivnaarssuit, sample 74902 x 90. 4-6 Cussidulinu reniforrne; specimens from Ivnaarssuit, sample 74902, x 90. 7-9 Huynesinu niueu; specimens from Arfertuarssuk, sample 74936, x 90. 10 Nonionellu uuriculu; specimen from Arfertuarssuk, sample 74935, x 90. 11 - 12 Islundiellu helenue; specimens from Ivnaarssuit, sample 74902, x 90. 13- 14 Astrononiongullowuyi; 13 specimens from Ivnaarssuit sample 74902, x 90; 14 specimen from Arfertuarssuk, sample 74935, x 90. 15 Huynesinu orbiculure; specimen from Arfertuarssuk, sample 74936, x 90. 16-19 Buccellu frigidu; two specimens from Arfertuarssuk, sample 74935, x 90. 20 Elphidium rnugellunicurn; specimen from Ivnaarssuit, sample 74902, x 90. 21 -22 Cibicides lobutulus; specimen from Ivnaarssuit, sample 74902, x 55. 23 Stuinforthiu loeblichi; specimen from Ivnaarssuit, sample 74902, x 90. 24 TrifarinuJluens; specimen from Arfertuarssuk, sample 74935, x 90. 25 Elphidium incertum; specimen from Arfertuarssuk, sample 74935, x 90. 26 Elphidiellu urcticu; specimen from Ivnaarssuit, sample 74902, x 90. 27 Elphidium usklundi; specimen from Arfertuarssuk, sample 74935, x 90. 28-29 Nonionellinu lubmdoricu; specimen from Arfertuarssuk, sample 74936, x 90. 30-3 1 Elphidium burtletii; specimens from Arfertuarssuk, 30 from sample 74935, x 55; 31 from sample 74934, x 90. The specimens are kept at the Institute of Geology, University of Aarhus.


a: LL

0 3 -

Table 3. Radiocarbon dates from central West Greenland obtained during this study. For locations see Fig. 1.

LOC N W Sample Lab. Elevation Age, I4C 6 '3C no lat. long. no GCI- no Material (m) yrs BP %,

Svartenhuk Halva

Nuussuaq

+Hammer Dal

+ lvnaarssuit

A Nordre Laksebugt

17 48 45 35 33 38 31 34 38 38

43 49 30

24 20 23 19 27

I

4 2

14 11 10 42

36 13 8

70"43' 69"04 69"27' 69"57' 69%' 69"52' 70"04' 69"57' 69"52' 69"52'

69"37' 68"59' 70"03'

70"14 70"28' 7Ool6' 70"23' 70"08'

71"38'

71 "23' 71"38' 70"43' 71 "27' 71"27' 69"39'

69"lS' 70"44 71"3O

54"36 53"32' 53"4O 54"50' 54"12' 54"46' 54"W 54"49' 54"46' 54"46'

54"45' 53"19 54"45'

54"47' 54"06' 54"37' 54"57' 54"49'

55"35'

55"02' 55"31' 54"33' 55"02' 55"OO 54"63'

54"52' 54"32' 55" 13'

74929 74918 74960 74914 74958 74906 749 10 74917 74907 74905

74900 74871 74909

7492 1 74863 74923 74925 74926

74947

74945 74949 74857 74942 7494 1 74893

74901 74859 7493 1

1-16414 Ua- 1787 K-5776 1-16358 Ua-1785 RCD-24 1-16357 I- 16366 I- 16356 K-5509

K-5969 RCD-21 K-5510

I- 16390 Ua-1788

Ua- 1789 Ua- 1786

Ua-1790

1-16393

K-55 13 K-5514 K-5505 K-5512 K-5511 K-5506

K-5508 RCD-23 RCD-22

Bone of large whale Basal peat Basal gyttja Shells of Mytilus edulis Bone of ?Balaena mysticetus Shells of M . edulis Shells of M . edulis Rib of ?B. mysticetus Bone of ?B. mysticetus Shells of Mya truncata, Hiatella arctica, Macoma calcarea Lower jaw of large whale Shells of H. arctica, M . truncata Shells of M . calcarea, Portlandia arctica Shells of M . truncata, H. arctica Shells of P . arctica Shells of H. arctica, M . truncata Shells of M . truncata Shells of P. arctica

Shells of P. arctica

Shells of M . truncata, H. arctica Shells of M . truncata, H. arctica Shells of H. arctica, M . truncata Shells of Astarte borealis Shells of H. arctica, M . truncata Shells of H. arctica, Balanus balunus, Serripes groenlandicus, Hemithiris psit tacea Shells of Chlamys islandica Shells of H. arctica, M . truncata Shells of H. arcticu, M . truncata

5 5.2 13 4.5 ? 22 3.8 6.5 22 15-20

36 62 38-44

4 10-15 25 30-35 24-25

0-2

14 8-10 48 35 7 3

4 42 22

380 f 80 1610 f 100 4730f 115 5920 f 120 6510 f 80 6870 f 80 6940 f 120 7190 f 150 7350 f 120 7810 f 90

8400 f 90 8690 f 90 9350 f 100

9200 f 150 9300 f 150 9920 150

10470 f 130 28530 f 680

37570 f yii: > 30400 > 32530 > 33540 >34710 > 36600 > 38050

> 391 10 > 40000 > 40000

-18.1

-23.5 -1.2

0.0 -2.0

-21.6 - 19.6 -0.8

- 15.8 +1.0 -3.8

-1.9

-3.7

+ 0.9 + 1.4 + 1.7 +0.2 -0.3 +2.0

0.0 +1.3 +0.1

+ A

+

0'02 0'04 0'06 0'08 610 0'12 HYD

Fig. 4. Mean AIle/Ile ratios in the FREE and HYD (Total) fractions on in situ shells from different localities.

referred to a Middle Pleistocene, interglacial stage (Fig. 5).

The deposit has amino acid values correlative with the Mudderbugt aminozone with mean ratios of 0.10

and 0.31 in the HYD and FREE fractions, respectively (Funder & Simonarson 1984) and with the Meteorbugt marine event with mean ratios of 0.088 and 0.415 at one site (Kelly 1986). The Mudderbugt aminozone is defined by ratios from shells in moraines, the fauna of which includes Chlamys islandica. The Meteorbugt marine event is defined by ratios from shells that may also be reworked; the faunas do not include subarctic elements.

Nordre Laksebugt marine event

This event is defined by sediments from a c. 10 m high and c. 1 km long coastal cliff, west of Nordre Lakse- bugt (loc. 42, Fig. 1). The sequence can be divided into three units: Unit 1 is a basal diamicton that is missing to the southwest. Unit 2 is a c. 8 m thick unit consisting of basal, shell-rich sand grading upwards into red and grey silt and clay with scattered shells. The silt layers are interbedded with thin diamictons - presumably deposited by debris flows. Unit 3 consists of 2 m Holocene beach gravel (Fig. 6) .

The macrofauna which comes from the bottom of unit 2 (Table 1) is unusually diverse, and among the


Table 4. AIle/Ile ratios in the total hydrolysate (HYD) and free (FREE) fractions in shells of Hiatella arctica (Ha) and Mya truncata (Mt) from central West Greenland. For locations see Fig. I .

~ ~

LOC. Sample Lab. No. HYD FREE no. no. GCI- BAL- Species HYD mean FREE mean

1

2

3

4

8

9

9

10

74947

74949

74946

74945

7493 1

74938

74939

7494 1

2385A

3285B

2386A 2386B 2384A

2384B

2383A

2383B

2379A

2379B

2380A

2380B

2381A

2381B

2382A

2382B

Mean for the Svartenhuk Marine Event 13 74859 2377A

2377B

14 74857 2376A

2376B

16 74853 2375A

2375B

Mean for deposits on Nuussuaq 17* 74928 2013A

2013B

2013C

21* 74873 20 1 OA

20 1 OB

20 1 oc

Mt

Mt

Mt Mt Mt

Mt

Mt

Mt

Ha

Ha

Ha

Ha

Ha

Ha

Mt

Mt

Ha

Ha

Ha

Ha

Mt

Mt

Ha

Ha

Ha

Ha

Ha

Ha

0.028 0.028 0.028 0.026 0.032 0.031 0.030 0.028 0.027 0.027 0.033 0.034 0.040 0.038 0.035 0.035 0.025 0.028 0.021 0.032 0.034 0.035 0.034 0.036 0.036 0.042 0.038 0.039 0.040 0.031 0.036 0.024 0.034

0.041 0.042 0.050 0.052 0.058 0.058 0.053 0.056 0.047 0.051 0.048 0.048

0.041 0.035 0.042 0.040 0.038 0.041

0.284 0.290 0.065 0.066 0.155 0.148

0.028 f 0.193

0.032 f 0.001

0.028 f 0.001

0.036 f 0.003

0.029 k 0.006

0.034 f 0.001

0.039 f 0.002

0.031 f 0.005

0.032 0.005

0.046 k 0.006

0.056 f 0.002

0.049 f 0.002

0.050 f 0.006

0.040 f 0.003

0.287 f 0.004

0.066 f 0.001

0.152 k 0.005

0.214 0.193 0.202 0.126 0.176 0.203 0.180 0.178 0.177 0.214 0.230 0.136 0.152 0.160 0.121

ND

0.174

0.125

0.209

0.185 0.178 0.189 0.110 0.222 0.108

0.151 0.167 0.184 0.143 0.166 0.142 0.205 0.213 0.131 0.122 0.188 0.173

0.158

0.275 0.267 ND

0.81 1 0.862 0.328 0.302 0.324 0.332

0.184 f 0.039

0.190 k 0.019

0.187 f 0.018

0.170 k 0.041

0.121

0.150 k 0.035

0.191 0.016

0. I57 f 0.057

0.173 k 0.036

0.161 kO.018

0.182 k 0.033

0.154 f 0.032

0.165 0.029

0.233 f 0.065

0.837 k 0.036

0.315 f 0.018

0.328 f 0.006


Tab/e 4. (Continued)

LOC. Sample Lab. No. HYD FREE no. no. GCI- BAL- Species HYD mean FREE mean

26* 74922 20 12A

20 12B

20 12c

27 74926 2520A

2520B

36 7490 1 2378A

2378B

Mean for the lvnaarssuit Marine Event

39* 74904 201 1

2014

42 74893 2519A

25 19B

Mean for the N. Laksebugt Marine Event

Mt

Mt

Mt

Ha

Ha

Ha

Ha

Mt

Mt

Ha

Ha

0.041 0.041 0.046 0.045 0.058 0.054 0.047 0.048 0.060 0.060 0.106 0.106 0.124 0.131

0. I06 0.097 0.092 0.093 0.070 0.070 0.052 0.050

0.160 0.193 0.169 0.156 0.158 0.224 0.249 0.263

0.054 k 0.007 0.267 0.254 _+ 0.014 0.237 0.354 0.352

0.1 17 * 0.013 0.377 0.354 0.019 0.331

0.177 k 0.027 0.048 0.007

0.1 17 * 0.013 0.354 * 0.019 0.295 0.271

0.097 * 0.006 0.243 0.260 0.028 0.232 0.223 0.220

0.061 0.01 1 0.245 0.229 k 0.01 1

0.228 0.061 0.01 1 0.229 * 0.01 1

* Reworked material. ND: Not detectable

This work

Postglacial

Ice shelf?

Svartenhuk ME

Laksebugt ME

Nordre Laksebugt ME

lvnaarssuit ME

Correlations

Mudderbugt AU Meteorbugt AZ

Fig. 5. Stratigraphic summary and correlations with areas in West Greenland outside the study region (Kelly 1986; Funder 1990). ME, marine event; AZ, aminozone. Ages of Pleistocene subdivision boundaries are according to Martinson et a/. ( 1987).

Middle or Late Pleistocene faunas from Greenland its number of molluscs is only surpassed by that from the Langelandselv fauna in central East Greenland, which is correlated with the last interglacial (Petersen 1982). The large number of epifaunal elements is noteworthy, and the shells of many of these animals were found sitting directly on top of the underlying diamicton. The unusually large contingent of epifaunal animals may in part explain the large diversity of the fauna. Most of the species are widely distributed in the Arctic, but several are usually considered high-arctic, and one of these, the bivalve Pandora glacialis, is new to the fossil fauna of West Greenland (Fig. 7). Pan- dora glacialis is also unknown from West Greenland at present, but in the Langelandselv fauna it occurs together with Mytilus edulis (Petersen 1982), and along the Pacific coast of North America it lives as far south as Juan de Fuca Strait at c. 48"N (Dall 1921). Thus, its palaeoclimatic significance is uncertain. Two other mollusc species are also new to the fossil fauna of West Greenland, Trichotropis borealis and Colus gracilis. T. borealis is rather common in West Green- land at present (Posselt & Jensen 1898), but there are no previous fossil records from this region, whereas there are many from Holocene deposits in North and Northeast Greenland. Colus gracilis is mainly a south-


Arfertuarssu k

Nordre Laksebugt loc 42

Laksebugt loc. 46

I Legend

I Diamicton

I

- 100"

Ti, . .. - - . [I.=! - . - I Silt

- . : a

. . . - . . .

74936 74935174932 74934 . . . -

_ ,

* , . - , . .

Planar cross-bedding Massive

b Mollusc shells

74934 Sample

Fig. 6. The sequences at Nordre Laksebugt (loc. 42), Laksebugt (loc. 46) and at the head of Arfertuarssuk (loc. 6) .

ern species, but it lives around the Faroe Islands (Sparck & Thorson 1933) and Iceland (Oskarsson 1982), and possibly along the southwest coast of Nor- way (Hnisaeter 1986). There is a fossil record of 'Fus- cus gracilis Da Costa aff.' from West Greenland that could refer to this species (Rink 1853).

Most of the other species from unit 2 are widely distributed along the coasts of West and East Green- land. Exceptions are Trophon truncatus and Cerasto- derma elegantulum, which are subarctic species confined in East Greenland to the southernmost part (Thorson 1944; Ockelmann 1958), and C. elegantulum with a northern range limit in West Greenland in the

Thule area (Clarke 1974). Several other species are often referred to as high-arctic species including Port- landia arctica, Actinula greenlandica, Macoma loveni and Cyrtodaria kurriana. The last two taxa, however, are widely distributed in West Greenland where they live together with subarctic molluscs. Actinula greenlandica has a southern range limit in West Greenland in the Uummannak region today, and the species is considered an indicator of high-arctic conditions by Peacock (1989), but it is not infrequently found together with subarctic or, even boreal species in fossil assemblages (e.g. Simonarson 198 1). Portlandia arctica is at present only known from the Thule district in


Fig. 7. Selected macrofossils. A. Spirorbis granulatus (Annelida: Polychaeta) shell from sample 74893. B. Spirorbis violaceus shell, 74871. C. Spirorbis vitreus shell, 74893. D. Acmaea rubella (Gastropoda: Prosobranchia) shell, 74871. E. Moelleria costulata (Gastropoda: Prosobranchia) shell, 74892. F. Puncturella noachina (Gastropoda: Prosobranchia) shell, 7487 1. G. Retusa obtusa (Gastropoda: Opisto- branchia) shell, 74871. H. Yoldiella lenricula (Bivalvia) shell, 74892. I. Yoldiella fraterna (Bivalvia) shell, 74938. J. Cerastoderma elegantulum (Bivalvia) shell, 74893. K. Macoma loveni (Bivalvia) shell, 74893. L. Pandora glacialis (Bivalvia) shell, 74893. M. Caulostrepsis isp. (trace fossil), two U-shaped borings in Balunus balanus (Crustacea: Cirripedia) plate, 74910. N. Strongylocentrotus droebachiensis (Echinoderma: Echinoidea) plate, 74893. 0. Turtonia minuta (Bivalvia) shell, 74956. P. Oichnus isp. (trace fossil), round hole in Hiatella arctica (Bivalvia) shell, 74956. J-M are light photographs (specimens coated with ammonium chloride), the others are scanning electron microscope photographs (specimens coated with gold). The specimens are kept in the type collection of the Geological Museum, Copenhagen (MGUH 22232-22247). The scale bars are one millimeter long.

West Greenland. When it dominates fossil assemblages, it is considered an indicator of proximal glaciomarine conditions (Peacock 1989), but the high diversity in the two assemblages from Nordre Lakse- bugt strongly contradicts this interpretation. The record of little auk (Alle alle) is the first Pleistocene record of a bird from Greenland, but the species has been reported from a Pleistocene deposit on Ellesmere Island (Blake 1980).

Some of the shells and many small stones from this deposit form a substratum for a rich bryozoan fauna of encrusting species (34 taxa, Table 2). By far the most common species is Escharella klugei, which occurs on 75% of the stones. Second in abundance is Hincksipora spinulifera, which is more dominating due to its broader and thicker crusts. In addition, detached fragments or small colonies of seven erect branching taxa were found. The small colonies belong to the


genus Celleporina. Up to eight bryzoan species were found on a single small stone, covering most of its surface. The high percentage of membraniporiform (encrusting) species is indicative of a low depositional rate (Lagaaij & Gautier 1965). Most of the species are known to live at present around Disko or in areas to the north and south hereof, with purely arctic, arctic/ subarctic or arctic/northern boreal ranges. However, two species appear to have a subarctic range (Escharella klugei and ‘Escharella ’ thompsoni). The latter species is recorded from the Disko area, from Labrador and other parts of the subarctic in the North Atlantic (Hansen, unpublished). Oncousoeciapolygonalis has mainly a subarctic distribution; it is unknown from the Disko area or further north at present but lives in the Arctic Ocean, according to Denisenko (1990). One of the species, the erect-growing Cystisella bicornis, has not before been recorded from Greenland. It is recorded from northern Alaska (as Porella saccata var. beringia Kluge), the Chukchi Sea, Bering Sea and the Sea of Okhotsk.

Foraminifera were studied in four samples from the lower part of unit 2 (Figs. 2 and 6). Few specimens were found and they were poorly preserved and etched on the surfaces. These are considered to represent residuals of richer faunas which were exposed to chemical etching after deposition. Consequently, the foraminifera do not provide an indication of the environmental conditions.

To conclude, the faunas indicate coastal water temperatures similar to those of today or slightly warmer. Notweworthy, however, is the absence of Mytilus edulis and Chlamys islandica.

A shell sample from unit 2 yielded a radiocarbon date of > 38,050 years BP (Table 3). Mean amino acid ratios are 0.061 f 0.01 1 and 0.229 f 0.01 1 in the HYD and FREE fractions (n = 4, Table 4, Fig. 4). The unique fauna makes a correlation with other sites in West Greenland difficult and the amino acid values cannot be correlated with other sites in West Greenland. However, the amino acid values indicate that the deposit is of Middle Pleistocene age, older than the Kaffehavn marine event, which is attributed to the last interglacial stage (Kelly 1986, Fig. 5).

Laksebugt marine event

Deposits at Laksebugt. - The Laksebugt marine event, described and named by Funder & Simonarson

(1984), is based on deposits exposed along a stream north of Laksebugt on southwest Disko (loc. 46, Fig. 1). A revised sedimentological log for the site shows a coarsening upward sequence from silt to sand to diamicton, capped by Holocene beach gravel (Fig. 6). The silt and sand layers are exposed from 51 to c. 61 m above the present sea level, which is higher than any of the other in situ pre-Holocene fossiliferous occurrences of the region. This suggests that the deposits were laid down during a period of extensive glacier loading. The gradual transition to diamicton indicates that a glacier subsequently approached and possibly overrode the site. The diamicton layers show parallel lamination and are likely to represent glaciomarine deposits.

The lower part of the sequence contains common shells of Portlandi arctica and, in addition, rare shells of the small bivalve Axinopsida orbiculata. Molluscan assemblages completely dominated by Portlandia arc- tics are indicative of nearby calving glaciers, and A. orbiculata can also live in proximal glaciomarine environments (Peacock 1989).

Foraminifera were examined in eight samples (Figs. 2 and 6). The lowermost four samples yielded sparse, well-preserved foraminifera dominated by Elphidium excavatum. Comparable assemblages are found at present in proximal glaciomarine environments (Elverh~i et al. 1980; Osterman & Andrews 1983). The few specimens in the top sample may represent reworked specimens.

The sediments at Laksebugt have been dated by means of thermoluminescence (TL) and optically stim- ulated luminescence (OSL) dating (Table 5). The two TL dates differ widely, whereas the three OSL dates are more consistent indicating an age of c. 160 ka. This corresponds with isotope stage 6; traditionally considered a period of heavy glaciation in West Greenland (Kelly 1985; Funder 1989), compatible with a heavy isostatic downwarping. Amino acid ratios have not been determined on in situ shells because Portlandia arctica racemizes at a different rate from that of Hiatella arctica and Mya truncata used in this study. This lack of amino acid ratios hampers correlation with the other marine events discussed.

On the surface of the described section a more diverse mollusc fauna occurs including one specimen of Mytilus edulis (Funder & Simonarson 1984). This fauna is not compatible with proximal glaciomarine

Table 5. TL and OSL dates (ka) from Laksebugt, central West Greenland (loc. 46, Fig. 1).

Sample no. TL age TL age OSL age OSL age (GCI-) Lab. no. uncorrected corrected uncorrected corrected

74887 R-9 1420 1 146’ 74888 R-9142022 - 74889 R-914203 114

- 117 110

161 f 15 115 -

164 & 15 156 k 15 162 f 15

I Too old to be corrected. * Sample too small for TL dating


Table 6, Ostracods in some pre-Holocene (localities 6, 16) and Holocene (45) deposits from central West Greenland. For locations see Fig. 1.

Locality number Sample number GCI 74-

6 6 16 45 935 936 853 960

Acanthocythereis dunelmensis (Norman, 1865) Cytheretta teshekpukensis Swain, 1963 Cytheropteron nodosoalatum Neale & Howe, 1973 Finmarchinella barentzouoensis (Mandelstam, 1957) Hemicythere emarginata (G. 0. Sars, 1866) Robertsonites tuberculatus (G. 0. Sars, 1866) Sarsicytheridea bradii (Norman, 1865) Sarsicytheridea macrolaminata (Elofson, 1939) Sarsicytheridea punctillata (Brady, 1865) Xestoleberis depressa (G. 0. Sam, 1866) Total no. of valves

1 1

~

- ~

194

1 128

325

-

- - - ~ 2 7 6

conditions. The source of these shells was not located and they may derive from the diamicton. This fauna, which is possibly reworked, was correlated by Funder & Simonarson (1984) with the oxygen isotope stage 5/6 transition on the basis of amino acid analyses and the altitude of the deposit.

Deposits on Nuussuaq. - An extensive deposit of sand and gravel occurs on the tip of Nuussuaq (locs. 13- 16, Fig. 1) exposed in coastal cliffs and along small streams. The lower part of the deposit is dominated by sand, in some places containing abundant mollusc shells, whereas the upper part consists of gravel, in places exhibiting giant scale cross-bedding. In situ shells occur up to 48 m a.s.l., and the marine limit is about 60 m a.s.1. The deposit is interpreted as a raised delta/alluvial fan complex. From its position at the tip of the Nuussuaq peninsula, it must have formed when the Vaigat sound to the south and Uummannaq Fjord to the north were filled by outlet glaciers (Fig. 1). No till cover or glaciotectonic disturbances were observed in the sections, but diamictons occur in the area and the local bedrock is striated.

The macrofauna (Table l), which is dominated by Hiatella arctica and Myu truncata, comprises eight taxa, most of which are widespread in the Arctic, although Astarte montaqui var. striata is mostly confined to the mid-Arctic (Peacock 1989). Only a single worn bryozoan specimen was found. One fine- grained sediment sample contained low numbers of ostracods belonging to two species: Robertsonites tu- berculutus and Sarsicytheridea bradii (Table 6). Both are common, shallow marine, infaunal, cold-temperate to arctic species, and their occurrence suggests a quiet shelf environment during deposition of the fine- grained sediment. Two samples were examined for foraminifera (Fig. 2), but both were barren. There is no indication of North Atlantic water entering the region at the time these sediments were laid down.

Two shell samples yielded non-finite radiocarbon dates (locs. 13 and 14, Table 3). Three samples

yielded mean aIle/Ile ratios of 0.050+0.006 and 0.165 f 0.029 in the HYD and FREE fractions (n = 12, locs. 13, 14 and 16, Table 4). These ratios suggest that the deposit is older than the widespread deposits on Svartenhuk Halvs (see below).

Deposits at Hammer Dal. - At locality 27, at the mouth of Hammer Dal on northwest Disko, Port- landia arctica, collected from marine silt interpreted as pro-deltaic, yielded a radiocarbon age of 28,530 f 680 I4C-years BP (Table 3). The amino acid data show that this is a minimum age, and the aIle/Ile ratios in the HYD fraction correspond to those obtained on shells from the deposits at the tip of Nuussuaq (Table 4). The most common bivalve from the Hammer Dal deposit is Portlandia arctica. This species, as well as Clinocardium ciliatum were not found on Nuussuaq.

We provisionally refer the deposits at Laksebugt, on Nuussuaq and at Hammer Dal to the Laksebugt marine event. All have low diversity faunas without subarctic faunal elements. The deposits on Nuussuaq and at Laksebugt are associated with high relative sea level, and we consider the amino acid ratios from Nuussuaq and Hammer Dal to be correlative.

Svartenhuk marine event

Deposits at Kugssineq, Svartenhuk Halvca (loc. 10, Fig. 1) belonging to the Svartenhuk marine event were studied by Steenstrup (1883) and Laursen (1944), and a non-finite radiocarbon date was published by Weidick (1974). In addition, deposits at a locality at the head of the small fjord Arfertuarssuk (loc. 8, Fig. 1) were studied by Kelly (1986) who named this event. During the present study raised marine deposits were found to be widespread in the southwestern part of Svartenhuk Halvs. Twelve shell-bearing localities were visited, of which three were previously known (locs. 1-12, Fig. 1).

Lithologically, the sites consist of littoral gravel and sublittoral mud. Diamictons were only observed at the


site (loc. 8) described by Kelly (1986). It is possible that these diamictons are glaciomarine sediments, but they may also represent solifluctuation deposits, because the terrain rises rather steeply from the coastal cliff. In view of the fact that none of the other sites on Svartenhuk Halva, seem to be covered by diamictons, and that glaciotectonic deformations have not been observed, we believe that the sites reflect the last deglaciation of this coastline. The sites represent raised spits, cuspate forelands and deltas/alluvial cones. Shelly deposits reach altitudes up to 35 m a.s.l., which is close to the marine limit of the area.

In this context, it is important to note that Holocene marine deposits have not been found despite the fact that many sites were radiocarbon dated. The glacial limit on southwestern Svartenhuk Halva, appears also to lie at a low altitude - the uppermost glacial erratic southwest of Arfertuarssuk was observed at only 60 m a.s.1. Possibly, the Holocene uplift did not exceed the eustatic sea-level rise due to minor glacial loading.

Sixteen shell samples (locs. 1-12, Fig. 1) are as- cribed to the Svartenhuk marine event. Twenty-three macrofaunal taxa are present (locs. 1-12, Table l), but most samples are dominated by Hiatella arctica and Mya truncata. In addition, Kelly (1986) reported on two further species. Two small shell fragments of Chlamys islandica were found in one sample. This is the only indication of a subarctic mollusc species. On the other hand, several of the assemblages comprise Portlundia and Yoldiella species: P. arctica, Y. fraterna and Y. lenticulu (Fig. 7). The last two species occur off West Greenland at present, but the only previous fossil record of Yoldiella fraterna from West Green- land comes from the Early Pleistocene Pattofik beds (Simonarson 198 1). Yoldiella intermedia, which was reported by Kelly (1986) from the Svartenhuk marine event and thought to typify deposits belonging to it, was not found. Two assemblages comprise the bivalve Actinula greenlandica whose palaeoclimatical significance is uncertain. Astarte montagui var. warhami, present in one sample, is mostly a high-arctic taxon (Peacock 1989). All identifiable sea urchin remains from the region appear to belong to Strongylocentro- tus droebachiensis rather than the closely related species S. pallidus, which replaces the former towards the north. S. pallidus constitutes nearly 90% of the echi- noids in shallow waters in the Thule area today, while at Solitax Bugt in East Greenland (c. 73"N) it is the only regular echinoid present in shallow waters (Jensen 1974). Thus it was rather surprising that only S. droebachiensis was found in the fossil material. One sample contained a fragment of the free-growing, branched bryozoan Cystisella saccata, which is widely distributed in arctic waters. Overall the macrofaunas resemble Holocene faunas from North Greenland, but they include several species not found in North Green- land (Bennike et al. 1986; Kelly & Bennike 1992). This

suggests that conditions were less harsh during the Svartenhuk marine event than those of North Green- land during the Holocene.

Formaminifera were studied in three samples from the head of Arfertuarssuk (loc. 6, Figs. 2 and 6). Moderately high frequency assemblages were present in two of the samples (210) and 245 specimens in 100 g sediment), while the lowermost sample contained only 30 specimens. All samples, however, were characterized by high species diversities. Even though very few foraminifera occurred at the base of the sequence, it is clear that the species compositions are similar in the two lower samples. Elphidium excaua- tum, Cassidulina reniforme, Buccella frigida and As - trononion gallowayi are dominant, the latter species indicating glacier-distal conditions (Mudie et al. 1984). The subarctic indicators Buccella frigida calida, Elphidium incertum, Elphidium ulbiumbilicatum and Nonionella auricula are also relatively common. This subarctic influence is manifested more strongly in the top sample where Nonionella auricula is one of the dominant species (Gudina & Evzerov 1973; Feyling- Hanssen 1980). New elements with high frequencies in this assemblage are the shallow water species Hay- nesina orbiculare and Haynesina nivea. The latter species has not been reported from the high arctic and its distribution in the subarctic is poorly known, but it has been registered in recent shallow water assemblages along the coast of Disko and further south in Southwest Greenland (Penney, unpublished).

Two of the samples from this locality also contained Ostracoda (Table 6). Robertsonites tuberculatus and Sarsicytherideu punctillata, which dominate the faunas, were represented by valves of adult males and females and juvenile stages as small as A-VI (six moults pre-adult), with all intermediate stages present. The presence of adults of both sexes and of many small valved instars clearly indicates that the microfauna represents an in sifu life assemblage. Both are infaunal species that live on fine sand and sandy mud substrates in shallow marine settings where the salinity remains above 25%, (e.g. Elofson 1941). R. tuberculatus, Sarsicytheridea macrolaminata and S. punctillata are all species that can survive bottom temperatures of between -2" and +9"C (Cronin & Dowsett 1990; Cronin et al. 1991). Today, these temperature limits and salinities of c. 32.5%, reflect conditions in the upper c. 20m of the water column off Godhavn and in Disko Fjord (Andersen 1981). The Arfertuarssuk ostracod fauna, thus, indicates quiet, shallow marine conditions below wave base at some distance from the coast and far from any meltwater sources. The low species diversity represented in sample 74936 is probably a function of local bottom conditions.

To conclude, there is some discrepancy between the mollusc data and the microfossil data. The former indicate coastal water temperatures somewhat lower than those of today, while the latter imply full inter-


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glacial conditions with temperatures at least as warm as at present. However, as noted in the introduction, Mytilus edulis seems to be rare along this coast today, and it is possible that long-lasting sea ice (until mid- summer) may have controlled the former distribution of subarctic molluscs in shallow water.

Six samples were radiocarbon dated during this study, five of them gave non-finite dates up to >40,000 years BP, and the sixth date is also considered a minimum age (37,970 f ::;: years BP) (Table 3). Amino acid ratios from eight shell samples are relatively uniform. The mean aIle/Ile ratios are 0.032 f0.005 and 0.173 f0.036 in the HYD and FREE fractions (n = 33, Table 4, Fig. 4). The ratios for the HYD fraction are higher than those reported by Kelly (1986) for the Svartenhuk aminozone: 0.020-0.025 (range of mean values). Although no analyses from the same deposit were performed, we believe that the deposits correlate and represent a high sea-level event of last interglacial sensu luto age (Fig. 5). The absence of Mytilus edulis and the very rare occurrence of Chlumys islundicu may indicate that the event does not represent the last interglacial climatic maximum. The Svartenhuk marine event is also correlated with the Thule aminozone (Funder 1990).

Reworked faunas

Reworked shells or shell fragments were noted at four sites. At Asuk (loc. 21, Fig. 1) on northeast Disko, Laursen (1944) found shells at 150 m a.s.1. and reported that they were in situ indicating a former high sea level. We consider that the shell fragments occur in till and their amino acid ratios (Table 4) are widely scattered. One of them could represent and Early Quaternary marine event.

Shell fragments found in till in a moraine ridge that crosses the mouth of Vesterdalen, c. 8 km southwest of Ivnnaarssuit (loc. 39, Fig. l), may come from the same marine event as the shells at Ivnaarssuit. The shell fragments gave uniform ratios of 0.097 0.006 and 0.260 f 0.028 in the HYD and FREE fractions (n = 4, Table 4). The Middle Pleistocene value gives a maximum age for the moraine.

Amino acid ratios of three shell fragments from a diamicton at 190 m above sea level at locality 17 (Fig. 1) yielded uniform ratios of 0.040 f 0.003 and 0.233 f 0.065 in the HYD and FREE fractions. These shells may be of the same age as the nearby in situ deposits on the tip of Nuussuaq, or slightly younger. We sugget that these shells were transported from near sea level to their present location by an ice shelf of which there is evidence on Disko to the south (see below).

Finally, at locality 26 (Fig. 1) on northwest Disko small shell fragments found at 60-65 m a.s.1. in gravel forming what is probably a small kame feature yielded mean amino acid ratios of 0.048 & 0.007 and

0. I77 i 0.027 in the HYD and FREE fractions. These ratios could correlate with either Laksebugt or the Svartenhuk marine events.

Lute Weichselian ice shelf?

Some morphological evidence exists for an extensive ice shelf west of Disko Island prior to the last deglaciation. In Rink Dal, (loc. 32, Fig. 1) unfossiliferous, rhythmically bedded silt and clay, interpreted to be glaciolacustrine, were apparently deposited when the mouth of the valley was blocked presumably by a glacier. Near the mouth of the main valley at Nordre Laksebugt (loc. 43), at Kugssineq to the west (loc. 41) and at the mouth of Vesterdalen (loc. 37), kame deposits and kame features were probably formed along the eastern margin of an ice shelf because some of them have surfaces that decline to the east. Near the coast south of the mouth of Hammer Dal (loc. 28) two parallel, low hummocky ridges are interpreted as moraines with their proximal sides to the west. The deposits and features are provisionally correlated with the Late Weichselian Godhavn stade on Ingolfsson et ul. (1990), mainly based on the degree of weathering.

The Postgluciul

The oldest Postglacial deposits, found on Harer?en (loc. 19, Fig. 1) were dated to 10,470 f 130 14C-years BP (Table 3), which is calibrated to 10,440 (10,600- 10,200) years BC (Stuiver & Reimer 1993). The elevation of the marine limit on Disko was treated by Ingdfsson et ul. (1990) who reported a decline from 90 m in the south to 60 m in the north. The observa- tions from this study are similar. Holocene marine deposits have not been found on the tip of Nuussuaq or on southwestern Svartenhuk Halvr?. Shell-bearing marine deposits were located on Harenen, between Disko and Nuussuaq (loc. 19, Fig. I) where they reach an altitude of about 40 m a.s.1. In addition, Holocene fossiliferous marine deposits extend to 36 m a.s.1. at the mouth of Auvfarssuaq on Nuussuaq (loc. 20, Fig. 1).

From the distribution of the I4C dates (Table 3) the age of the marine limit decreases from 10.5 ka on Harer?en in the north to 9.1 ka on Kronprinsen Ejland in the south. This, together with the regional gradient of the marine limit, suggests that the southern part of the studied region were more heavily glaciated in the Late Weichselian - during the Godhavn stade of Ingolfsson et ul. (1990) - than the northern part, and that a major outlet glacier from the Inland Ice lin- gered on in Disko Bugt.

Since the marine limit along the outer coast varies from 110 m in Disko Bugt to c. 40 m on Hare~en, it is difficult to construct emergence curves in spite of the many radiocarbon dates available from the region.

BOREAS 23 (1994) Marine sediments, W. Greenland 21 3

Ingolfsson et al. (1990) presented two emergence curves for the Disko Bugt area. They suggested that the Early Holocene was a period of transgression soon followed by rapid regression. However, this initial rise in sea level cannot be proven by the present data set. If the sea inundated the area following deglaciation, it is possible that the relative sea level began to fall just after it reached the marine limit, as depicted on other emergence curves from West Greenland (Kelly 1985; Funder 1989). The new data cannot confirm any transgression but they support the regression provided by Ingolfsson et al. ( 1990).

The macrofaunas of Holocene samples are set out in Table 7. The faunas can be divided into two groups, an older group between 7.8 and 10.5 ka, and a younger group between 5.9 and 6.9 ka. The older group is characterized by Hiatella arcitca, Mya truncata and Portlandia arctica. The last species is now extinct in the region; it probably reflects proximal glaciomarine conditions where common. Most of these Early Holocene faunas are of low diversity, but the assemblage from Kronprinsen Ejland (loc. 49, Fig. 1) is a notable exception with 19-20 taxa of which at least one species, Trophon truncatus, is a subarctic element.

The younger group is completely dominated by Mytilus edulis. This is by far the most common bivalve species in littoral waters and on the beaches of western Disko today. Substantial numbers of modern Mytilus shells from the beaches of the western part of the island were bored, presumably by the spionid polychaete worm Polydora, either the east Atlantic species P . ciliata or the closely related west Atlantic species P. websteri (Blake & Evans 1974). Similar borings as- signed to the trace fossil Caulostrepsis isp. (ichnospe- cies) were found in many fossil shells. The oldest date for Mytilus edulis found on Disko is 6940 I4C-years BP. Further south, in Southwest Greenland, Mytilus is dated back to 8735 f 140 I4C-years BP (1-9954, Kelly, pers. comm., 1993), but the species was already present in the Thule area to the north by 9150 I4C- years BP (Funder 1990). Apparently, the species had difficulties in colonizing central West Greenland, and this feature may also explain why the species was not found in any pre-Holocene faunas of this region.

Another polychaete worm, Spirorbis violaceus is new to the fossil fauna of Greenland, but all Spirorbis species identified in this wrok belong to the extant fauna of West Greenland (Wesenberg-Lund 1950). The identifications of Spirorbis tubes are somewhat tentative because the modem taxonomy is primarily based on the soft parts of the animals and because many fossil tubes were worn and poorly preserved.

Three Holocene samples contained a total of 13 bryozoan taxa (Table 2). All are widespread arctic or subarctic species, and only two of them, a small unidentifiable Tegella species and Myriapora subgracilis, are not present in the pre-Holocene faunas.

One site (loc. 45, Fig. 1) is represented in lake cores which contain c. 60cm of marine sediments below 338 cm of gyttja, the basal part of which was dated at 4730 k 115 I4C-years BP (Table 3). The marine sediments contain a rather diverse macrofauna, including an abundance of well-preserved fish bones of capelins, sculpins and pricklebacks (Table 7) and a few ostracods (Table 6). The phytal, shallow marine species Xestoleberis depressa was present in two samples in the same core, while Hemicythere emarginata occurred in one sample. Penney (1989 & unpublished) has noted that both species are common in recent inter- tidal to shallow subtidal algal communities in West Greenland, including Disko Fjord. Their occurrence imparts a brackish, shallow water, eurythermal aspect to the sediments. The threshold of this lake is 16.5 m a.s.l., which corresponds to the relative emergence since the mid-Holocene.

In addition to the fossil content shown in Table 7, marine macroalgae from one site have been described by Pedersen & Bennike (1993) and a few whale remains were also found, of which four were radiocarbon dated (Table 3). Two of them could only be identified as ‘large whale’, while two of them probably represent Greenland whale (Balaena mysticetus Lin- naeus, 1758), the bones of which are very difficult to distinguish morphologically from those of the closely related Biscayan whale (Balaena glacialis (0. F . Muller, 1758) (Mshl, pers. comm. 1991).

Acknowledgements. - The fieldwork was carried out in 1989-1990 by 0. Bennike while serving as scientific director of the Arctic Station (University of Copenhagen) in Godhavn. The board of directors of the Arctic Station and the staff of the station are thanked for their support. Funding was provided by the Danish Natural Research Council, the Commission for Scientific Research in Greenland and Dronning Margrethe’s and Prins Henrik’s Foun- dation. Radiocarbon dates marked K were obtained by courtesy of the Geological Survey of Denmark. Thanks are extended to 0. B. Berthelsen, S. Meldgaard Christiansen, J. Fuglsang, J. Gissel Nielsen and J. Aagaard for technical help, and to M. Kelly, H. P. Serjup and Boreas referees W. Blake, Jr. and J. England for their reviews of the manuscript.

References Andersen, 0. G. N. 1981: The annual cycle of phytoplankton

primary production and hydrography in the Disko Bugt area, West Greenland. Meddelelser om Grmland, Bioscience 6, 65 pp.

Bennike, O., Funder, S . & Hjort, C. 1986: Notes on the Holocene marine fauna of eastern North Greenland. Bulletin of the Geolog- ical Society of Denmark 35, 71 -74.

Blake, J. A. & Evans, J. W. 1974: Polydora and related genera as borers in mollusk shells and other calcareous substrates. The Veliger 15, 235-249.

Blake, W., Jr. 1980: Mid-Wisconsinan interstadial deposits beneath Holocene beaches, Cape Storm, Ellesmere Island, Arctic Canada. American Quaternary Association, 6th Biennial meeting (Orono, Maine, Aug. 18-20, 1980), Abstracts, 26-27.

Clarke, A. H. 1974: Molluscs from Braffin Bay and the Northern North Atlantic Ocean. National Museums of Canada, Publications in Biological Oceanography 7, 23 pp.


Cronin, T. M. & Dowsett, H. J. 1990: A quantitative micropaleon- tologic method for shallow marine paleoclimatology: application to Pliocene deposits of the Western North Atlantic Ocean. Marine Micropaleontology 16, 117- 147.

Cronin, T. M., Briggs, W. M., Jr., Brouwers, E. M., Whatley, R. C. Wood, A. & Cotton, M. A. 1991: Modem Arctic Podocopid Ostracode Database. United States Geological Survey, Open-File Report 91-385, 51 pp.

Dall, W. H. 1921: Summary of the marine shell bearing molluscs of the northwest coast of America, from San Diego, California, to the Polar Sea, mostly contained in the collection of the United States National Museum, with illustrations of hitherto unfigured species. United States Naiional Museum, Bulletin 112, 217 pp.

Denisenko, N. V. 1990: Raspredelenie i Ekologiya Mshanok Barentseva Morya. Akademiya Nauk SSSR 1990, 157 pp.

Donner, J. 1978: Holocene history of the west coast of Disko, Central West Greenland. Geografiska Annaler (60A), 63-72.

Dunbar, M. J. 1951: Eastern Arctic Waters. Fisheries Research Board of Canada, Bulletin 18, 131 pp.

Elofson, 0. 1941: Zur Kenntnis der marinen Ostracoden Schwe- dens, mit besonderer Beriicksichtigung des Skagerraks. Zoolo- giska Bidrag frdn Uppsala 19, 215-534.

Elverhei, A., Liestel, 0. & Nagy, J. 1980: Glacial erosion, sedimentation and microfauna in the inner part of Kongsfjorden, Spits- bergen. Norsk Polarinstitutt Skrfter 172, 33-61.

Feyling-Hanssen, R. W. 1955: Stratigraphy of the marine Late- Pleistocene of Billefjorden, Vestspitsbergen. Norsk Polarinstitutt Skriyter 107, 186 pp.

Feyling-Hanssen, R. W. 1980: Microbiostratigraphy of young Cenozoic deposits of the Qivituq Peninsula, Baffin Island. Marine Micropaleontology 5, 153- 183.

Frich, P. & Ingolfsson, 0.1990: Det holoczne sedimentationsmiljo ved Igpik samt en model for den relative landhaevning Disko Bugt omrbdet, Vestgreland. Danrk Geologisk Forening, Arsskriyt for 1987-89, 1- 10.

Funder, S. (co-ordinator) 1989: Quaternary geology of the ice-free areas and adjacent shelves of Greenland. In Fulton, R. J. (ed.): Quaternary Geology of Canada and Greenland, 743-792. Geologi- cal Survey of Canada, Geology of Canada 1 (also Geological Society of America, the Geology of North America K-1).

Funder, S. (editor) 1990: Late Quaternary stratigraphy and glaciol- ogy in the Thule area, Northwest Greenland. Meddelelser om Grmland, Geoscience 22, 63 pp.

Funder, S. & Simonarson, L. A. 1984: Bio- and aminostratigraphy of some Quaternary marine deposits in West Greenland. Cana- dian Journal of Earth Sciences 21, 843-852.

Gudina, V. I. & Evzerov, V. Ya. 1973: Stratigrafiya i Foraminifery verkhnego Pleystotsena Kol’skogo Poluostrova. Akademia Nauk SSSR, Siberian Department, Institute of Geology and Geophysics 175, 148 pp.

Hansen, K. B. 1962: Bryozoa. The Godthaab Expedition 1928. Meddelelser om Grmland 81 (6). 74 pp.

Hayward, P. J. 1979: Systematic notes on some British Ascophora (Bryozoa, Cheilostomata). Zoological Journal of the Linnean So- ciety 66, 73-90.

Hoisaeter, T. 1986: An annotated check-list of marine molluscs of the Norwegian coast and adjacent waters. Sarsia 71, 73-145.

Ingolfsson, O., Frich, P., Funder, S. & Humlum, 0. 1990: Paleocli- matic implications of an early Holocene glacier advance on Disko Island, West Greenland. Boreas 19, 297-3 1 I.

Jensen, M. 1974 The Strongylocentrotidae (Echinoidea), a mor- phologic and systematic study. Sarsia 57, 1 13- 148.

Kelly, M. 1985: A review of the Quaternary geology of western Greenland. In Andrews, J. T. (ed.): Quaternary Environments: eastern Canadian Arctic, Bafm Bay, and western Greenland, 461 - 501. Allen & Unwin, Boston.

Kelly, M. 1986: Quaternary, pre-Holocene, marine events of western Greenland. Rapport GrmlandF Geologiske Undersflgelse 131,

Kelly, M. & Bennike, 0. 1992: Quaternary geology of western and 23 PP.

central North Greenland. Rapport Grmlands Geologiske Un - ders0gelse 153, 34 pp.

Kluge, G. A. 1962: Mshanki Severnykh Morei SSSR. Opred. Faune SSSR 76, 584 pp.

Kluge, G. A. 1975: Bryozoa of the northern seas of the U.S.S.R., 71 1 pp. Amerind Publishing Co., New Delhi.

Krog, H. & Tauber, H. 1973: I4C chronology of Late- and Post- glacial marine deposits in North Jutland. Danmarks Geologiske Unders0gelse, Arbog 1973, 93- 105.

Lagaaij, R. & Gautier, Y. V. 1965: Bryozoan assemblages from marine sediments of the Rhane delta, France. Micropaleontology 11, 39-58.

Laursen, D. 1944: Contributions to the Quaternary geology of northern West Greenland especially the raised marine deposits. Meddelelser om Grmland 135(8), 125 pp.

Levinsen, G. M. R. 1914: Bryozoa, Endoprocta, Pterobranchia og Enteropneusta. Conspectus Faunae Groenlandicae. Meddelelser om Grmland 23, 545-634.

Levinsen, G. M. R. 1916: Bryozoa. Danmark-Ekspeditionen ti1 Grmlands Nordestkyst 1906-08. Meddelelser om Grmland 43, 43 1-472.

Martinson, D. G., Pisias, N. G., Hays, J. D., Imbrie, J., Moore, T. C. & Shackleton, N. J. 1987: Age dating and the orbital theory of the ice ages: development of a high-resolution 0 to 300,000-year chronostratigraphy. Quaternay Research 27, 1-29.

Maturo, F. J. S. & Schopf, T. J. M. 1968: Ectoproct and Entroproct Type Material. Postilla 120, 1-95.

Mejdahl, V., Shlukov, A. I., Shakhovets, S. A., Voskovskaya, L. T. & Lyashenko, H. G. 1992: The effect of shallow traps: a possible source of error in TL dating of sediments. Ancient TL 10, 22-25.

Miller, G. H. & Mangemd, J. 1985: Aminostratigraphy of Eu- ropean marine interglacial deposits. Quaternary Science Reviews 4, 215-278.

Miller, G. H., Bingham, J. & Clark, P. 1982: Alteration of the total aIle/Ile ratio by different methods of sample preparation. Annual Report Amino Acid Geochronology Laboratory, Uniuersity of Boulder. Colorado 1981/1982, 9-20.

Mook, W. G. & Waterbolk, H. T. 1985: Handbook for Archaeolo- gists, No. 3, Radiocarbon dating. 65 pp. European Science Foun- dation, Strasbourg.

Mudie, P.J., Keen, C. E., Hardy, 1. A. & Vilks, G. 1984: Multivari- ate analysis and quantitative paleocology of benthic foraminifera in surface and Late Quaternary shelf sediments, northern Canada. Marine Micropaleontology 8, 283-313.

Ockelmann, W. K. 1958: Marine Lamellibranchiata. The Zoology of East Greenland. Meddelelser om Grmland 122(4), 256 pp.

Osburn, R. C. 1936: Bryozoa collected in the American Arctic by Captain R. A. Bartlett. Journal of the Washington Academy of Science 26, 538-543.

Osburn, R. C. 1950: Bryozoa of the Pacific Coast of America, Part I. Cheilostomata-Anasca. Allan Hancock Pacific Expeditions 14, 1-269.

Osburn, R. C. 1952: Bryozoa of the Pacific Coast of America, Part 11. Cheilostomata-Asclophora. Allan Hancock Pacific Expeditions 14, 271-611.

Oskarsson. I. 1982: Skeldvrafana Islands. 351 DD. Prentsmidian = * Leiftur, Reykjavik.

Osterman, L. E. & Andrews. J. T. 1983: Changes in Glacial-Marine sedimentation in core HU77-159, Frobisher Bay, Baffin Island, N.W.T: A record of proximal, distal, and ice-rafting glacial- marine environments, 451 -493. In Molnia, B. F. (ed.): Glacial- Marine Sedimentation. Plenum Publishing Corporation, New York.

Peacock, J. D. 1989 Marine molluscs and Late Quaternary environmental studies with particular reference to the late-glacial period in Northwest Europe: a review. Quaternary Science Reviews 8, 179- 192.

Pedersen, P. M. & Bennike, 0. 1993: Quaternary marine macroalgae from Greenland. Nordic Journal of Botany 13, 221 -225.

Penney, D. N. 1989: Recent shallow marine Ostracoda of the Ikerssuak (Bredefjord) District, Southwest Greenland. Journal of Micropalaeontology 8, 55-75.

BOREAS 23 (1994) Marine sediments. W. Greenland 21 5

Petersen, K. S. 1982: Attack by predatory gastropods recognized in an interglacial marine molluscan fauna from Jameson Land, East Greenland. Malacologia 22, 721 -726.

Posselt, H. J. & Jensen, A. S. 1898: Grsnlands Brachiopoder og Bleddyr. Meddelelser om Grmland 23(1), 299 pp.

Powell, N. A. 1968: Bryozoa (Polyzoa) of Arctic Canada. Journal of the Fisheries Research Board of Canada 25, 2269-2320.

Ridley, S. 0. 1881: Polyzoa of Franz-Josef Land. Annals and Magazine of Natural History Ser. 5, 7, 442-457.

Rink, H. 1853: Udsigt over Nordgronlands Geognosie. Kongelige danske Videnskabernes Selskabs Skrifter 5, 3, 71 -98.

Simonarson, L. A. 1981: Upper Pleistocene and Holocene marine deposits and faunas on the north coast of Niigssuag, West Greenland. Bulletin Grmlands Geologiske Unders0gelse 140, 107 pp.

Sparck, R. & Thorson, G. 1933: Marine Gastropoda Prosobranchi- ata. The Zoology of the Faroes 3, I , 9-54.

Steenstrup, K. J. V. 1883: Bidrag ti1 Kjendskab ti1 de geognostiske og geographiske Forhold i en Del af Nord-Grsnland. Meddelelser om Grnnland 4, 173-242.

Steenstrup, K. J. V. 1901: Beretning om en Underssgelsesrejse ti1 @en Disko i sommeren 1898. Meddelelser om Grmland 24, 249- 306.

Stuiver, M. & Reimer, P.J. 1993: Extended I4C data base and revised CALIB 3.0 I4C age calibration program. Radiocarbon 35, 21 5-230.

Thorson, G. 1944: Marine Gastropoda Prosobranchiata. The zoology of East Greenland. Meddelelser om Grmland 121(13),

Wehmiller, J. F. 1984: Interlaboratory comparisons of amino acid enantiomeric ratios in fossil Pleistocene molluscs. Quaternary Research 22, 109- 120.

Weidick, A. 1974 CI4 dating of survey material performed in 1973. Rapport Grmlanh Geologiske Underst~gelse 66, 42-45.

Weidick, A. 1976: Glaciation and the Quaternary. In Esher, A. & Watt, W. S . (eds.): Geology of Greenland, 431-458. The Geolog- ical Survey of Greenland, Copenhagen.

Wesenberg-Lund, E. 1950: The Polychzta of West Greenland with special reference to the fauna of Nordre Stremfjord, Kvane- and Bredefjord. Meddelelser om Grmland 151(2), 171 pp.

181 pp.

Quaternary marine stratigraphy and geochronology in central West Greenland

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