THE VEGA TRANSGRESSION
A hypsithermal event in Central East Greenland
CHRISTIAN HJORT
HJORT, C : The Vega Transgression - A hypsithermal event in Central
East Greenland. Bull. geol. Soc. Denmark, vol. 22, pp. 25-38. Copenhagen, January, 16th, 1973.
A stratigraphical sequence, studied in a cliff on the island Gåseø,
Vega Sund, Central East Greenland, has been interpreted as being
the product of a regression of sea-level, followed by a transgression and a renewed regression, leading down to (or psrhaps even below)
the present sea-level. The first regressional maxima has been found
to postdate 3970 B.C. and the transgression has been dated to
around 3690 B.C. This agrees well with Late Atlantic eustatic
movements, recorded elsewhere. A preliminary suggestion as to possible correlations with northern Europe is also put forward.
Christian Hjort, Department of Quaternary Geology, Sblvegatan 13,
223 62 Lund, Sweden. April 4th, 1972.
Although traces of Flandrian (West, 1968) marine transgressions from the
Hypsithermal interval (Deevey & Flint, 1957) have been found elsewhere
in the Arctic, as on Svalbard (Feyling-Hanssen, 1964a, 1964b; Hyvarinen,
1969; and Blake, 1970), none has so far been reported from Greenland.
One possible reason for this could of course be that isostatic recovery here
always outdid or equalled the eustatic rise of sea-level—information given
by Vogt (1933) and Jahn (1938) point towards pronounced stillstands of
sea-level in relation to land during this period. Another reason, more probable
according to the present author's opinion and also more in line with to-days
scientific knowledge of Greenland, might be that some of the most favourable areas for finding such traces, e.g. low flat outlying islands like Shannon
on the northeast coast, have rarely or never been visited by any geologist
working with these problems. In fact we know from several sources, among
them Bogvad (1940) and Saxov (1961), that at least during the end of the
last century and the first half of the present one subsidence of parts of the
east as well as the west coast took place. It seems very likely that the same
relationship, or at least about the same relative interaction between the isostatic and eustatic components could have existed in Greenland once or
several times earlier during Flandrian time.
26
HJORT: The Vega transgression
During field work in Central East Greenland in August 1971, among the
islands in the Scott Keltie Group of central Vega Sund, an area where to-day
coastal morphology seems to point towards a stagnant or transgressive sealevel, a stratigraphical sequence of some interest was encountered in the
western cliff of Gåseø island (72° 48'N Lat./22° 54'W Long.). It is described and discussed below.
The names used are those found on the Danish Geodetic Institute maps
72 0 1 and 72 02, in scale 1:250 000. Hydrographical information is found
on pilot chart no. 2730, Vega Sund E, Danish Hydrographic Office 1960.
An aerial view of all the westernmost islands in the Scott Keltie Group is
given on Geodetic Institute photo 669B-SV: 12450, and a vertical picture
of Gåseø on 672:3804—shown as fig. 2. Species of molluscs are named
according to Nordsieck (1969).
General'topography and geology
The Scott Keltie Islands are of a rather low relief. Only Kista 0, the largest
one, reaches an altitude around 150 m. Some, like Gåseø itself, for large
parts are flat tundra plains with. bogs and small shallow ponds. These
plains, usually lying between 3-5 m above sea-level, have been formed by
abrasion of the Quaternary deposits entirely forming some of the islands and
covering extensive parts of most of the others. Old beach-ridges are often
found. Bedrock is mainly Tertiary basalt, but a few outcrops of Cretaceous
rocks are also found (Koch & Haller, 1971).
Depth of water between the islands is generally shallow, in some cases
extremely shallow. To the west as well as to the east of the Scott Keltie
Group depths are much greater, soon reaching below 150 m. There are very
strong tidal currents between the islands. These turbulent conditions probably make the waters here comparatively nutritious—an unusually rich
bird-life is found. Probably for the same reason there is an uncommon
richness in sea-weed and shells along the shores, but this could, at least
partly, also be the result of deposition by the extremely strong currents.
Field work
A general feature to-day is the erosion by wave-action of the Quaternary
deposits in the area, an erosion being made more effective by an. obviously
stagnant or transgressive sea-level. As a result of this, eroded cliffs of some
meters height are commonly found. Fresh surfaces and not too much talus
makes the study of their stratigraphy easy.
The cliff visible in fig. 2 never reaches more than 5 m above high-water
level. As the lower parts of it is covered by talus it is not difficult to reach
Bulletin of the Geological Society of Denmark, vol. 22 [1973]
27
Fig. 1. Kong Oscars Fjord District, with inset map of Scott Kelties Islands. Based on
Geodetic Institute maps 720 1-2, and 730 1-2. Reproduced by permission of the
Geodetic Institute, Copenhagen (A. 220/72).
the uppermost layers from below. The complex part of the cliff stretches
from the small stream draining the lake and around 400 m northwards.
Further on in that direction soon only marine sand, corresponding to bed C
in the profile shown as fig. 3, is found. South of the stream the basalt lies
close to the surface, and the shore is a rather low sloping one, without any
cliffs.
Mapping of the actual profile was carried out by the simple method of
measuring the distances along the shore through repeated countings of steps,
and by measuring the heights above high-water level with a combination of
hand level and measuring tape. The profile has been drawn with the help
of these measurements and photographs taken.
Samples were taken for absolute dating as well as for soil analyses.
As time was unfortunately in demand for other work, the southeastern
parts of Gåseø could not be visited. Nor could any thorough search of Kista
0 , or the islands east thereof, be made. Those north and immediately east of
Gåseø had been visited earlier. On the northwesternmost one a cliff of some
HJORT: The Vega transgression
Fig. 2. Photo showing Gåseø (G), with section of cliff described in text marked by
white arrows. Lake, and small stream draining it, are clearly visible. Till sequence,
mentioned in connection with bed G, is found on the small island (S) to the west,
and is indicated by white arrow. Reproduced by permission of the Geodetic Institute,
Copenhagen (A. 220/72). Photograph 672:3804.
interest in connection with the Gåseø sequence was observed, and will be
briefly commented upon later.
Stratigraphy
Fig. 3 shows a profile along the cliff. Also shown is the simplified stratigraphical sequence, according to the authors interpretation. The abbreviation
(fc) means that only a field classification of the bed in question has been
made.
A: Sand with humic horizons, often very much disturbed by frost action.
Bulletin of the Geological Society of Denmark, vol. 22 [1973]
29
Cryoturbations are common. The border towards the underlying marine
sand is mostly indistinct or undefined, and the granulometric composition of the sandier part of that bed is very similar to that of bed A.
Marine shells of the same species as in C are often found lying on the
surface. Traces of eolian erosion and redeposition are common. Sometimes several sand-covered humic horizons are found above each other,
(fc)
B: Coarse stony gravel containing marine shells of the same species as in C.
Found only in the immediate vicinity of the small stream draining the
lake, (fc)
C: Marine sand, including fine sand and a small proportion of silt and with
thin strings of gravel. North of the central part of the profile shown,
these sediments lie almost horizontally. South of it they dip slightly
(around 5°) southwards. Marine shells, Mya truncata, Hiatella arctica
Fig. 3. Profile along the western cliff of Gåseø. It has been drawn with the help of
photos and vertical sections measured in the field. Consequently some slight generalisations have been necessary. Note also the different scales for length and height.
4
HJORT: The Vega transgression
30
D:
E:
Fi:
F2:
F3:
G:
and Mytilus edulis, are common. To a large extent both halves of the
shell are found together, as in life, (fc)
Shell-bearing sandy sediment. Several up to about 5 cm thick layers,
containing much allochtonous sea-weed and other coarse detritus, are
interbedded with sandier ones (fig. 4). Organic content in the central
part of the bed goes at most up to around 15% wt. The organic
layers contain leaves and small twigs of Salix, many shells of Mytilus
edulis, occasional ones of Tridonta borealis and (according to Dr. T. v.
Wachenfeldt, Lab. of Marine Botany, Lund) remnants of red algae,
Bangia sp., Polysiphonia sp., brown algae, Sphacelaria sp., and also of
some unidentified hydroides (Hydroida). The algae all belong to the
sublittoral zone, in the sense used by Lewis (1964), and are uncommon
below 10 m depth.
The boundaries of this bed, down towards bed E and up towards C
are mostly graded and indistinct.
Silty brownish clay, sometimes with small lenses of fine sand. Extremely
rich in marine shells, Mya truncata, Hiatella arctica, Tridonta borealis,
Nicania montagui, Mytilus edulis and Acmaea rubecula. The shells make
up about 7% of the total weight. They are to a large extent found
with both halves together. The clay is rich in travertine-like concretions,
in which shells are abundantly included.
Irregularly stratified, mainly coarse sediments. Sandy layers between
more stony gravelly ones. Sometimes lenses containing only sand and
silt occur, but their sideward extension is always limited. No shells, (fc)
Silty sand. Gravelly stony strings are found, but are of secondary importance. No shells, (fc)
LikeFi. (fc)
Hard packed, mainly coarse material (68% over 2 mm diameter).
Gravelly and stony, but also containing sand and a small amount of silt
and clay. Differs from other beds in the sequence in having a greyish
colour, and a marked till-like appearance. Its lateral contacts to Fi show
clear interdependence.
Discussion of stratigraphy
Structure and granulometric composition of beds Fi and F3 gives the impression of being the result of sedimentation under rather unsettled, somewhat turbulent conditions. Bed F2, on the other hand, bears witness of a
calmer environment.
Bed G is most likely explained as being of glacial origin—or as having
been deposited by a stranded ice-berg. The very flat surroundings speak
against the possibility of it being a product of solifluction, which of course
Bulletin of the Geological Society of Denmark, vol. 22 [1973]
31
would also have meant that sea-level before the deposition of bed E had
once stood at, or lower than around the present level 1 m above sea-level.
This is, according to the author's hitherto unpublished results from the area,
very unlikely; see also the shore-line displacement curves in Washburn &
Stuiver (1962) and Lasca (1969). In fact G bears a very strong resemblance
to the uppermost of two tills seen in a cliff along the southern shore of the
small round island (S in fig. 2) 2.5 km northwest of Gåseø. As certain
features, among them endmoraine-like structures on Geographical Society 0 ,
seem to indicate that the front of a glacier in Vega Sund once stood at the
western edge of the Scott Keltie threshold, it might be possible to regard G
as a rather washed variety of the beforementioned upper one of two tills.
Fi-3 might then be interpreted as being deposited in the close, or rather close
proximity of this postulated ice-front, F2 perhaps during a calmer period
between the deposition of the two tills. Everything taking place under submarine conditions—the upper marine limit west of the islands, in the
direction of ice-recession, lies on at least 65 m, probably higher. Work on
these problems is however far from finished.
During the Hypsithermal (see chapter on radiometric datings) deposition of
marine clay, bed E, took place. That is, according to the known facts about
ice-movements in the district, at least some thousand years after the deposition of any glacial sediments (ice-berg rafted excepted) in central Vega Sund.
And obviously also after some erosion of these layers had taken place.
The mollusc-fauna found in this clay is neither one of extremely shallow
waters, nor of extreme depths. That is about all which can be said with any
degree of accuracy. The living conditions however, must have been very
favourable, as can be seen from the immense numbers of shells. It should
also be noted that on the east coast to-day, Mytilus edulis is only found
living south of 67°N. In the areas north of that latitude, where it is found
in a sub-fossil state, it is generally regarded as an indicator of climatical
optimum conditions (Noe-Nygaard, 1932); see also Ockelmann (1958) for
information on occurring species.
The formation and age of the travertine-like concretions is the scope of
a special study, and so should not be further discussed here. Conclusions
concerning their origin are not likely to have any immediate importance
for the stratigraphical discussion in this paper.
Bed D with its mainly allochtonous remnants, of Salix and of Mytilus
edulis and other detritus from (or even from slightly above) the upper parts
of the sublittoral zone, is regarded as a sediment of the kind found accumulated along the shore, or in very shallow water close to the shore. An interpretation, this should be stressed, of vital importance for the whole discussion.
The change from clay-sedimentation to accumulation of this intertidal or
4*
32
HJORT: The Vega transgression
Fig. 4. Showing transition from bed E to D, and on to C, at the approximate distance
210m in fig. 3. Note the darker, more organic sublayers in bed D.
extreme shallow-water deposit must obviously be the result of a negative
fluctuation of sea-level. This (high-water level) is not likely to have come
further down than to around 2.0 m above the present level, as at about
1.0 m (tidal range around 1 m) an undisturbed successive grading from one
bed to the other can be seen, and that is unlikely to occur above low-water
level. The relatively short span of time (see chapter on radiometric datings)
between deposition of the clay and of the marine sand (bed C), of a deeper
origin than the underlying bed D, also makes any great amplitude for this
lowest part of the regressional phase unlikely; see e.g. Fairbridge (1961) and
Berglund (1971) for opinions on amplitudes of sea-level fluctuations in
other areas during Hypsithermal time.
Whether the fact that the successively higher layers of bed D reach successively further in over the underlaying clay has to be attributed directly to a
transgression, or is merely an effect of gradual filling up around the slight
elevation covered by the clay, is an open question. That bed D does not
entirely cover the top thereof can easily be explained by its exposed position;
under any conditions. And what erosion might have done, we do not know.
For faunal and sedimentological reasons it seems reasonably clear that the
Bulletin of the Geological Society of Denmark, vol. 22 [1973]
33
marine sand (C) must be of a somewhat deeper origin than the underlying
bed D, being more or less connected with low-water level. A transgressional
phase has followed the regressional one; and rather successively too, as can
be seen from the grading upwards from one bed to the other.
Exactly how far above present sea-level this transgression terminated can
not yet be determined. But occurrence of the marine sand around the 6 m
level on the plains of central Gåseø (abraded and with beach-ridges from the
later regression), gives an absolute minimum value for it. As, however, a
sand with this fauna hardly can have been deposited at less than one or a
few meters below low-water level, a minimum for the upper limit of the
transgression, at around 8 m above present high-water level must be concluded.
Bed B, found only along the small stream, entirely resting on bed C and
also having exactly the same fauna, is regarded as a strongly washed remnant of this marine sand. The stream has washed almost all the finer fractions away, as it successively, during the regression of sea-level down to its
present level, eroded the sediments. At an early stage of this regression, what
is now the lake probably was a shallow lagoon or bay.
Bed A, with its frost disturbed humic horizons and clear traces of eolian
activity, is regarded as being mainly formed of redeposited material from
bed C. The occurrence of bed A is not at all a general feature on Gåseø, as
is also indicated in fig. 3. Often the marine sand of bed C is the deposit
found on the surface.
Radiometric dating
Radiocarbon dated samples
Age Ti/ 2 : 5568
Sample
B. P.
B.C.
<5C13
%«
Bed C (Lu-585)
Marine shells
6190 ± 70
4240
+ 1.7
BedD(Lu-584)
5100 ± 75
3150
H-17.9
Algae
Bed E (Lu-586)
Marine shells
6470 ± 70
4520
+ 1.7
All samples have been collected in the middle parts of their respective beds.
The CI 4 age is based on the half-life 5568 ± 30, and all values have been
corrected for deviations from the "normal value" of CI 3 in terrestrial plants
(<5 C13:-25.0 %o in P.D.B.scale).
34
HJORT: The Vega transgression
Discussion of radiometric dating
It is a well known fact (Olsson & Blake, 1962; Mangerud, 1970) that
datings of marine shells often do not give the correct age. It has been found
that a "sea-correction" must sometimes be applied to the original value, in
order to eliminate the effect of a proportion of C 14 in sea-water often different from that in the atmosphere.
In East Greenland a correction of -550 years was once used by Washburn
& Stuiver (1962). This value was based on one single sample of live
specimens, collected at Mestersvig in Kong Oscars Fjord, about 70 km SSW
of Gåseø. A later dating of another recent sample from the same locality
gave the age 200 years, the lower value thought by Stuiver (1969) as being
possibly due to nuclear contamination. Whether any of these two samples
had been corrected for the original isotope fractionation (CI 3) was however
nowhere mentioned.
In order to study the problem samples of shells collected as live specimens
by Swedish expeditions to East Greenland around the turn of the century
were dated at the Lund Radiocarbon Laboratory. The results (Hjort, in
press) gave a mean value of 570 years (CI 3 corrected) for three different
dated samples. Considering the small number of samples and the standard
deviation, a preliminary "sea-correction" for East Greenland, rounded off to
-550 years, will be. suggested. This correction, at least seemingly well in
accordance with the one used by Washburn & Stuiver (1962), is used in the
present paper.
As to the rather surprising value for the organic material from bed D the
following can be said. First: The stratigraphical position of this bed, between
E and C, is indisputable. Second: Great care has been taken to avoid getting
any remnants of terrestrial plants (Salix) og shells (Mytilus edulis, Tridonta
borealis), otherwise found in the bed but of which not enough material for
a dating could be obtained, into the sample dated. Consequently this has in
all probability been done on more or less pure algae, only perhaps with
a small content of hydroides. Third: No contamination of bed D with humus
of younger age seems possible. The dated sample was taken in a part of the
bed (to the right in fig. 3) overlain only by sand of bed C. Lateral transport
from the rather thin, and low-grade humic horizons in bed A, even though
perhaps facilitated by the southward-dipping gravelly strings in bed C,
seems unlikely.
Although the source of error thus cannot presently be traced, it is the
author's firm belief that it has to be sought in the dating of bed D. This bed,
with its originally rather mixed content, should be more problematic to date
correctly than marine shells. It should also be noted that more than 20%
of the outer parts of the dated shells have been removed through treatment
Bulletin of the Geological Society of Denmark, vol. 22 [1973]
35
with acid before dating, and that the chronological positions of beds E and
C, according to the respective ages arrived at, agrees with their stratigraphical position.
The following are the corrected dates:
Bed C
5640±70 B. P.
Bed E
5920±70 B. P.
3690 B. C.
3970 B. C.
Conclusions
According to the interpretation of beds Fi-s and G as glacial or glaciodependent, no traces of any sedimentation from the time between glacial
withdrawal from the area and the middle part of the Hypsithermal interval
can be found in the profile studied. Though as the mentioned beds obviously
have been somewhat eroded, it can not be excluded that such sediments
once could have covered them.
In Hypsithermal time deposition of marine clay took place. This sedimentation was halted some time after 5920 ± 70 B.P. (3970 B.C.), through a
regression of sea-level, which could of course have been in progress well
before it began affecting bottom-conditions, making clay sedimentation impossible and also changing the f aunal assemblage.
During the time around, and perhaps even for some time after the maximum of this regression the littoral or extreme shallow-water sediment, bed D,
with its mainly allochtonous content of terrestrial and sublittoral origin, was
deposited. As an undisturbed graded contact between bed E and the overlying D is found at around 1 m above present high-water level (to the right
in fig. 3), it is concluded that this point probably always remained below
low-water level. With a tidal range of around 1 m this gives a high-water
level at the maximum of regression standing not below 2 m above the present
one. Though probably it stood even a little higher than so.
Between the end of clay deposition, after 5920 ± 70 B.P. (3970 B.C.),
and before 5640 ± 70 B.P. (3690 B.C.), transgression set in. At the latter
date it had already been in full progress for some time. When it finally
terminated is not known, but it has been found that the maximum level
reached in all probability was at least around 8 m above present high-water
level.
This leads to a preliminary conclusion about a transgression in relation
to land (that is with no compensation given for the so far insufficiently
known isostatic movement in the area during the time) of somewhere between or slightly above 5-6 m. A figure which however must be regarded
as rather unsafe. Though it will have to stand until further and more
detailed research of the locality and surrounding areas can be carried out.
Bed B has been interpreted as consisting of washed material from bed C,
36
HJORT: The Vega transgression
and bed A as consisting mainly of material from the same bed—redeposited by eolian action.
Correlation with other areas
The described transgression, here for geographical reasons called The Vega
Transgression, according to the age of bed C (5640 ± 70 B.P. 3690 B.C.)
falls within Late Atlantic time. That is, during a period of climatical optimum
conditions, and also of generally high eustatic niveaus.
The Vega Transgression also falls within the period 6000-4600 B.P.
covered by The Older Peron Submergence (Fairbridge, 1961), the earliest
one of two phases of Flandrian eustatic maxima, recorded in isostatically
stable areas of the world.
Any final correlation with results obtained in northern Europe will have
to wait until further research has been done, and more complete datings
have been made. It should however, most preliminarily, be pointed out that
general agreement seems to be rather good. See Marthinussen (1962) for
northern Norway, Tapes 111:5700-5500 B.P.; Morner (1969) for Swedish
west coast, PTM-4B:3700-3550 B.C.; Berglund (1971) for Blekinge,
southeastern Sweden, Siretorp III-IV: 3900-3300 B.C.; Binns (1972)
for the British Isles, F3:5492 B.P.
As to the transgressions on Svalbard, the one recorded at Trullvatnet
(Hyvarinen, 1969) has been dated to between 5550-4745 B.P. An age,
like the one of F3 mentioned above, slightly younger than the one date given
for The Vega Transgression. But as that date clearly does not mark the end
of this transgression, those events are not necessarily different ones.
The other dates from Svalbard, from Skansbukta and Talavera (FeylingHanssen, 1964a and 1964b), seem to be rather unsafe (see Olsson & Kilicci, 1964), but however to fall within the same general period of Hypsithermal transgressions (dates given range from about 6000 B.P. to 3000
B.P.).
Acknowledgements. The manuscript has been read, and improvements suggested by
Prof. B. E. Berglund, Mr. Leif Bjelm (who also took part in the field work), Mr. Sven
Funder, Mr. Soren Håkansson (who dated the samples), Mr. Erik Lagerlund and Dr.
Anker Weidick. Dr. T. v. Wachenfeldt identified specimens of algae, and commented
upon their origin. Analyses have been made by Miss C. Ullman and Mrs. C. Liljegren,
the latter of which has, together with Mrs. Siri Bergstrom, also drawn the figures.
Finally Mrs. M. Palmgren gave my english a needed brush-up. To them all my
sincere thanks. The work was carried out as part of a larger project, financed with
grants from the Swedish Society for Antrophology and Geography, The Royal Physiographic Society, Lund University and The Malmo Student Corporation.
Bulletin of the Geological Society of Denmark, vol. 22 [1973]
37
Dansk sammendrag
En postglacial lagfølge fra Gåseø i Vega Sund, centrale Østgrønland, tolkes som resultatet af et regressions/transgressions/regressions forløb, hvorved havoverfladen
endte ved det nuværende niveau, eller lavere. En C14 datering viser, at den første
regression kom efter 3970 år f. Kr., og tilsvarende er transgressionen dateret til omkring 3690 år f. Kr. Det svarer udmærket til de sen-atlantiske eustatiske bevægelser
kendt fra andre steder. Endelig forsøges en korrelation med Nordeuropa.
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