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Jökull - 01.12.1987, Qupperneq 69

Jökull - 01.12.1987, Qupperneq 69
Fig. 10. (A) The Melar diamicton at 1640 m. Its lower contact with facies Dms of the Ásbakkar diamicton is very sharp, and clasts are thrust or lodged into the substratum. The arrow points at a double facetted stone. The diam- icton is overlain by the glaciomarine facies of the Melabakkar silts and sands, (B) The Melar diamicton at 1550 m, where it rests on facies Dmu of the Ásbakkar diamicton. Notice the large number of angular boulders, (C) A lag concentration of boulders on top the Landhólmi sands delta deposit, (D) Large, striated boulder on the surface immediately above Látrar. 10. mynd. A og B: Jökulruðningur í bökkunum. C og D: Stórgrýtisdreif frá ruðningnum í sniði og á yfirborði. There are three major facies of sand in the sequence overlying the silt facies (logs F and G, Fig. 3), divided into a number of beds: Massive to crudely bedded, moderately sorted to silty sand (Su) stratified sand (Ss) and laminated silty sand (Sl). The sand units range in thickness from about 0.2 m to about 1.2 m, with conformable and loaded or erosional lower contacts, and stratification due to normal to reversed grading of the individual beds. Random intraformational lags of coarse sand to pebbly sand occur in most units. In facies Su, intralaminae of silt, resembling dish structures, were observed. Facies S1 is a succes- sion of thin, silt coated sandbeds. The Ás beds diamictons Description: Interbedded with the sand- and gravel facies in the sequence are discontinuous sheets or lenses of massive and stratified diam- ictons (Dmu, Dms, logs F and G, Fig. 3). Their matrix is sandy-silty, but they display considerable varibility in both tex- ture and clast content. Individual units range in thickness from a few centimetres to about one m, and, where occurring isolated, have sharp or erosive bases and a tendency towards convex upper contacts. On one occasion a 3 m thick diamicton succes- sion was observed (Log F). Facies Dms has intraformational bands of silt and thin sandbeds. Both facies Dms and Dmu show a tendency towards concentration of gravels at the base. The diamicton units appear to be randomly interbedded with the lithofácies of sand and gravel, suggesting penecontemporane- ous deposition1. Interpretation of the Ás beds The transition from the Ásbakkar diamicton to the gen- erally coarser overlying sequence indicates an increased energy input into the depositional basin. In the sub- polar glaciomarine environment, proximity to both the ice margin and to the source of meltwater plays a key role in determining the lithofacies distribution (e.g. Molnia 1983, Powell 1984). Powell (1983b) pointed out that supraglacial streams are absent and englacial streams rarely flow from tidewater glaciers, due to their highly crevassed nature. The meltwater discharge from such glaciers is almost entirely subglacial, and results in a proglacial submarine outwash deposit, composed of several lithofacies reflecting discharge, sediment load and the proximity of the deposit to the glacier margin. The lithologies and structures of the Ás beds are best explained as being a result of a combination of sedi- mentation from subaquatic ice-marginal outwash streams and glacigenic subaquatic debris flows. I suggest that the sand and gravel facies are ice-proximal melt- water fan sediments, where the gravel facies represent 67
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