Regional Reconstructions of Former Ice Cover

The full publication of my work will, I hope, take place in the near future with the necessary illustrations, many of which were shown as slides accompanying the lecture. Space permits here only the reproduction of two series of block diagrams, constructed after the original maps, and showing the deglaciation of the Høvringen (western Rondane) and the Sjodal (eastern Jotunheim) areas.

Each stage is reconstructed from definite markings in the field, which I have correlated using all the material collected from the area in question. I would like to emphasize this, as of course one can always construct a map based upon probable general levels and gradients of the ice surface.

Something of an exception is Stage I in eastern Jotunheim, as a still active glacier leaves so few traces. This is largely an extrapolation from Stage II.

The deglaciation of the Hevringen area (Fig. 2, p. 749) is of the now classical dead ice type, and comes out very clearly in the map and block diagrams with explanations (Figs. 3, 4, 5, 6, pp. 750–51). The highest dead ice feature is that of a real marginal watercourse. The traces reach 1525 m., but probably the ice was inactive even when lying higher.

Fig. 2.

Part of the Hovringen map, reduced and simplified. (Altitudes in metres)

Fig. 3

Stage 1. Drainage towards north with the higher summits clear above the ice. Plateau ice on high-level flats. The ice is climatically dead

Fig. 4

Stage 2. Subglacial drainage towards south (see Fig. 1) to Gudbrandsdalen (foreground valley). Marginal lake. Plateau ice still lying on one high-level flat

Fig. 5

Stage 3. Western part of glacier surface slopes towards Gudbrandsdalen. High level free of ice. Marginal lakes in eastern part of area

Fig. 6

Stage 4. Ice only in the valley (Gudbrandsdalen)

In the Jotunheim there was active glacier cover at a fairly late stage, as is to be expected with such high mountains not very far from the sea. There is evidence of Stage I round Bessvatn, and Stage II is marked by one of the longest apparently strictly lateral lines that I have ever followed; it stretches uninterruptedly for some 8 km. to the north-west of the Sjodal (Figs. 7, 8, 9, pp. 752–53).

Fig.7

Stage 1. Active glaciers spreading from the Yotunheim glaciation centre. Local glaciers descend from Bessha (2258 m. left) and the Nautgardstind massif (up to 2257 m. centre) where there is also an isolated local glacier

Fig. 8

Stage II. The main ice climatically dead. Cirque glaciers in Bessvatn (lake), on Bessho and the Nautgardstind massif. Enormous marginal terraces and channels are being formed in Veogjelet (where the river at the right meets the ice)

Fig. 9

Stage III. The whole area is ice free except a small remnant of dead ice covered by gravel in the main valley (Sjodal). No cirque glaciers, in contrast to one to-day in Bessho and several in the Nautgardstind massif

Kongsvoll-Snøhetta-Fokstua is an important area. The down-melting was very regular from north-west towards south-east with no conspicuous traces of late active local glacierization even at the Snøhetta (2286 m.) (Fig. 10, p. 746), but the most interesting fact is that here a large part of the glacier surface could be reconstructed at the last “live” stage, being marked by lateral moraines with distal drainage channels. Below this surface the usual dead ice phenomena were met with in large numbers.

It is pleasant to imagine the interglacial plants of the “Dovre flora” following the retreating ice boundary from their refuges on or off the Møre coast to their present habitat near Kongsvoll.

Deductions

From work in the different areas marked on Fig. 1 it is possible to essay some generalizations of importance.

There can hardly be any doubt that during the whole of the last glaciation the Jotunheim mountains were an active centre, not overridden by the main Scandinavian ice. Not only do striae, etc., radiate from the Jotunheim area, but a complete transformation of landscape with large rocky hills transformed more or less to roches moutonnées, clearly indicate the long duration of a glaciation centre here. However, Jotunheimen is not the only centre of glaciation from which streams radiated onto the inland ice sheet.

Lateral moraines and drainage channels in Geiranger indicate that during deglaciation there must have been an ice surface there sloping to the north, forming part of an ice cap with its centre in the Jostedalsbre high plateau. Here as in Jotunheimen, sufficiently large areas are found at a sufficient altitude, and with a sufficient snowfall.

Other high parts of the land surface in western Norway have also formed glacierization centres for which there is positive evidence in many cases. Even for the maximum of the last ice cover the concept of a smoothly sloping ice shield must be superseded by a more varied picture.

Generally speaking, wherever there are important glaciers to-day, and even on some high plateaux now unglaciated, e.g. in Sogn, there seem to have been local centres during the last glaciation. A notable exception is the Hardangerjokul (Fig. 11, p. 746), to-day covering 95 km.² (Flåm-Ustaoset area).

Climatic Fluctuations

Climatic deviations must have tended to interrupt or reverse the course of down-wasting. Even within Rondane there are traces of some late climatic change, evidently but a slight one; but in two other places I have found evidence of a forward push from mountain massifs on to the surrounding vidde. In both cases a clear terminal moraine was found, with large boulders sticking out of the old moraine formed into roches moutonnées with striae.

There was evidently a kind of thin piedmont glacier involved, issuing in the one case from the Gjende-Bygdin massif on to Valdresfly, in the other from Heddersfjell (Gausta area).

Dead Ice Phenomena

These phenomena may be found everywhere above the marine limit, as there will always be some stagnant ice cut off, even when the glacierization was active to the last. But only in the Gudbrandsdal-Dovrefjell-Østerdal region are dead ice phenomena very evident. This is the area where there was least movement in the ice sheet and the thickest morainic cover, partly dating back to the penultimate glaciation. Here also was the last occurrence of a fairly thick shield, and a maximum supply of melt water. Thus the best conditions for magnificent glaciofluvial phenomena of erosion and deposition were present, and also plenty of ice to be buried.

The dead ice phenomena occur equally on both sides of the ice divide, and not only between the ice divide and the watershed. Indeed when approaching the watershed, for instance in the Grotlid area, the phenomena become very sparse and the uplands are covered with the ordinary thin bottom moraine found over most of the Norwegian highlands.

Dating of the Stages

Over the Gudbrandsdal-Rondane-Dovrefjell region the deglaciation process has been exclusively one of down-wasting of the Mannerfelt type.

It is the same all over the Gudbrandsdal-Østerdal areas surveyed by Gjessing and his collaborators, but they have found new and important phenomena at the stage when the dead ice remained in the valley bottoms, with water (the ice-dammed lakes of earlier authors) and glaciofluvial deposits from tributary streams upon and within it. Through future research these late stages may be connected with the melting-back from the coast.

It is not even permissible to fix a definite relative age upon any one stage at present, and comparatively sure datings will certainly be very difficult to obtain. It is easy enough to fmd out the general features of the story, especially from marginal phenomena, but a correlation in time even of very clear markings within a small area is not easy owing to the interrupted nature of all the features.

In the future, radiocarbon datings from the first organic lake deposits laid down in areas just left bare may fix the general chronology. Even so they cannot help much in a local analysis, as the down-melting has been so very rapid. To judge from distances between lateral drainage channels, vertical wastages of more than 10 m. yearly seem frequent, and compare well with present-day ablation during a warm summer. However, with the slight gradient of an ice surface in late stages this corresponds to large yearly regressions of the ice border. Some stages in the process must have been very rapid, and the corresponding enormous volumes of melt water have left their mark everywhere.

Indeed if only some 5 m. of yearly downward wastage is assumed, 1000 m. would be lost within 200 years! But of course stages with intense melting may have been interrupted by intervals of quiescence, and I am afraid we have as yet not even the framework of an absolute chronology.

Finally I may mention, mainly because of its accessibility, one glacier that has “died” recently, the Omnsbre. On a miniature scale it affords several parallelisms to conditions during the deglaciation period.

The Omnsbre is a kind of “sheet” glacier (Fig. 11, p. 746) with its southern snout only some 5 km. north of Finse on the Bergen–Oslo railway. The highest part of the glacier is at 1600 m., it descends to 1500 m. to the south, and to 1350 m. to the north. At the time of the topographical survey of 1923–29 (Map D. 33, Hardangerjokulen 1 : 100,000, stereophotogrammetric original 1 : 50,000) the glacier, as defined by the surveying party, covered some 10 km.².

The Omnsbre was thus an extremely flat glacier of considerable extent. Slight alterations in the firn line will work out much more sensationally than in an alpine glacier with perhaps 1000 m. attitudinal differences. Once the firn line rises above 1600 m., the Omnsbre is climatically dead.

Vertical wastage during the last few years has been very great. There are all kinds of marginal phenomena on a small scale, exactly like the dead inland ice in miniature. The ice is generally speaking very clean, and the melt water issuing from the glacier is now always quite clear. This is in enormous contrast to the melt water from the living glacier, which, when I worked on the lakes of the district in 1933, was frequently a real mud stream, blackish from the Ordovician shale below the glacier.