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Jökull - 01.12.1987, Qupperneq 73

Jökull - 01.12.1987, Qupperneq 73
angular, and serveral striated and facetted clasts with double stoss-lee sides, characteristic for lodgement till (Kriiger 1984) were recognized. Some of the elongated clasts show an apparent imbricated fabric in the exposure, with a dip towards north. The diamicton is lithified and very difficult to sample or check for preferred orientation fabric. Where the diamicton sheet climbs the cliffs, clasts can be seen thrust or lodged into the substratum (Fig. 10A) and silt clasts from the substratum are incorporated into the diamicton. Neither joints nor folds were observed with- in the diamicton, but both occur in its substratum (see later). At some places the upper contact is coated by a thin (1-5 cm) sheared siltband. Concentrations of large boulders on top of the strata between 1700 m and 2500 m and large, striated erratics on the lowland surface above Látrar (Fig. 10D), could be lagdepos- its from the Melar diamicton. Interpretation of the Melar diamicton The Melar diamicton has many of the properties com- monly used for recognizing lodgement tills (for reviews see Boulton 1976, Dreimanis and Schluter 1985): It is a non sorted, massive sediment, containing large, striated and facetted clasts. Elongated clasts show imbricated fabric. Its lower contact is erosional and it has a sheet- like depositional geometry. Its surface is sheared at places, and glaciotectonic deformations occur in its sub- stratum. On this basis I interpret the Melar diamicton as lodgement till. Apparent fabric and direction of the glaciotectonical deformations in its substratum (see lat- er) indicate a deposition beneath a glacier coming from a northerly direction, out of the Borgarfjördur main val- ley. The Asgil gravels: an ice-marginal outwash facies association Description: A deposit of coarse gravels, trending NE-SW, is buried in the sediments south of the Ásgil ravine, between 2725 m and 2875 m (Fig. 2, Fig. 3, log E). It has a ridge-like morphology: It is about 150 m wide and 5-12 m high, and can be followed in exposures some 300 m inland from the coast. The deposit is composed of four major gravel facies (Gu, Gp, Gs, Ggn) and three major sand facies (Ss, St, Sp). Most conspicuous are the facies of massive to weakly stratified gravel (Gu, Fig. 11A), often with well developed imbricate fabrics, arranged together with facies Gs in poorly defined multistorey sets (Fig. 11B). Set thicknesses are 1-2 m, set contacts are erosional or gradiational, and individ- ual sets can be traced laterally for up to 45 m. Boulders are abundant in the gravels, and the largest one encountered had a diameter of 60 cm. The gravel and boulder clasts are sub- rounded to well rounded. Some of the clasts derive from the Ásbakkar diamicton and contain subfossil molluscs. Facies Gs (sample 16, Fig. 4) is sandy, planar stratified, with imbricated gravel trains and minor intrabeds of gravelly sand. The graded facies (Ggn) grades upwards from clast supported gravel to sandy, matrix-supported pebble gravel. The Gp facies consists of large-scale isolated sets of planar cross-stratified gravels, occurring within and below the multisto- rey sequence of Gu and Gs facies. Set thicknessesobserved were around 1 m, with foreset thicknesses of 20-30 cm, dipping around 20° towards SE. The foresets are angular based to slight- lyconcave. Facies Ss is a roughly planar parallel stratified poorly sorted sand, with occasional pebbles (Fig. 11C). It occurs both as about 1 m thick single units, and as thin and discontinuous lenses within the multistorey sequence. The stratification is due to normal grading from pebbly to poorly sorted sand within the individual 4-10 cm thick sandbeds. Facies St is gravelly sand (Fig 4, sample 17) in grouped trough sets, with coset thickness of about 1.5 m. Set thicknesses are 20-30 cm and set widths about 1 m. Planar cross stratified sand (Sp) occurs in large scale isolated sets at the base of the sequence (Fig 11D). Set thicknesses are up to 1.5 m, with foreset dip angles up to 26° towards SE and foreset thicknesses of 10-20 cm. The foresets are angular based and consist of alternating layers of coarse, pebbly sand and some- what better sorted sand. Interpretation of the Ásgil gravels I interpret the Ásgil gravels to be ice-marginal glacioflu- vial outwash deposits. Their sedimentology fits descrip- tions of proximal glaciofluvial deposits by e.g. Booth- royd and Ashley (1975), Frazer (1982) and Miall (1983). Large boulders in glaciofluvial deposits have been used by e.g. Thomas (1984a) to infer ice-contact depositional environment, as the stream capacity to carry large boul- ders downstream is limited. Haraldsson (1981), who studied the recent Markarfljótssandur in S-Iceland, rarely found boulders with diameters larger than 40 cm outside its very proximal part. The deposit is buried under glaciomarine sediments (Fig. 2) belonging to the Melabakkar silts and sands described below. Paleocurrent measurements from im- bricated fabrics and foreset dips (Fig. 2) indicate a de- positing stream direction from NW. The glaciofluvial deposits interfinger as gravel trains with the Melabakkar silts and sands glaciomarine facies. That, along with the lack of faults or other tectonic features supports the assumption that the broad ridge form is the syndeposi- tional geometry of the deposits. I suggest that the Ásgil gravels were deposited as an ice-marginal transverse ridge where fast flowing subglacial streams entered the marine environment. The waterdepth during the ridge deposition was more than 25 m. THE MELABAKKAR SILTS AND SANDS: A GLACIOMARINE FACIES ASSOCI- ATION AND SUBLITTORAL FACIES A third major sequence of silty-sandy sediments, with a 71
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