Geological Survey of Denmark and Greenland Bulletin 19 ... - Geus

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310 610 m GANT#1 Overburden 350 50 650 400 100 700 Itilli Formation Umiivik Member 750 Itilli Formation Umiivik Member 450 500 Kangilia Formation Annertuneq Conglomerate Member 150 200 800 550 250 850 Itilli Formation Umiivik Member 600 300 900 clay si vf f mcvc f mc sand pebbles clay si vf f mcvc f mc sand pebbles clay si vf f mcvc f mc sand pebbles 94
76). Heavily bioturbated interbedded sandstones and mudstones, chaotic beds, and structureless, muddy sandstones also occur. Indistinct thickening- and coarseningupward cycles, 2–85 m thick, can be seen in the Umii - vik-1, FP94-11-02 and FP94-11-04 wells (Fig. 75; Dam & Nøhr-Hansen 1995). A cobble conglomerate composed of lithified sandstone clasts in a mudstone matrix is exposed in stream gullies on the south side of Uparu - aqqusuitsut on north-eastern Svartenhuk Halvø (Fig. 73; Christiansen et al. 2000). In the GANT#1 core, chaotic beds, muddy sandstones and sandy mudstones alternate with thick, sharpbased fining-upward successions (Fig. 76; Dam 1996a). The fining-upward successions consist of amalgamated sandstone beds grading upward into thinly interbedded sandstones and mudstones. Thin coarsening-upward successions also occur. The amalgamated sandstones consist of normally graded, medium- to coarse-grained sandstone beds with scattered basement pebbles and mudstone intraclasts. The sandstone beds are generally structureless, but parallel and cross-lamination occurs towards the top of some beds. A thin mudstone layer usually caps the sandstone beds. The thinly interbedded sandstones and mudstones consist of sharp-based, graded laminae and beds of finegrained to very coarse-grained sandstone alternating with black parallel-laminated mudstones. The sandstones are well-sorted and may show parallel and cross-lamination; small mudstone rip-up clasts frequently occur throughout the sandstone beds. Fossils. Ammonites from the Umiivik Member have been described from several localities on Svartenhuk Halvø and include Scaphites mariasensis umivikensis (Birkelund), Scaphites preventricosus svartenhukensis (Birke lund), Clioscaphites sp. aff. saxitonianus (McLearn), Scaphites cobbani (Birkelund), Scaphites rosenkrantzi (Birkelund), Scaphites cf. corvensis (Cobban), Clioscaphites saxitonianus septentrionalis (Birkelund), ammonites of the genus Haresiceras and inoceramids of the steenstrupi group (Birkelund 1965). Belemnites from Svartenhuk Halvø Facing page: Fig. 76. Sedimentological log of the Umiivik Member (Itilli Formation) and the Annertuneq Conglomerate Member (Kangilia Formation) in the GANT#1 well. For location, see Fig. 74; for legend, see Plate 1. Modified from Dam (1996a). include Actinocamax cf. primus (Arkhangelsky) and Actinocamax sp. (Birkelund 1956). Unidentified teleost fish remains have also been found in strata yielding Coniacian ammonites (Bendix-Almgreen 1969). Ammonites occur at several localities along the north coast of Nuussuaq in the Umiivik Member, including Pseudophyllites skoui (Birkelund), Scaphites (Hoploscaphites), S. (H.) greenlandicus (Donovan), S. (H.) ravni (Birkelund), and S. (H.) ikorfatensis (Birkelund). The belemnites Actinocamax groenlandicus (Birkelund) and Actinocamax aff. groenlandicus (Birkelund), and an indeterminate solitary corallum have also been collected (Birkelund 1956, 1965; Floris 1972). Dinocysts are abundant in the Umiivik Member (Dam & Nøhr-Hansen 1995; Nøhr-Hansen 1996, 1997a; Dam et al. 1998b). Depositional environment. The Umiivik Member records deposition from low-density and high-density turbidity currents, debris flows, slumping and fall-out from suspension. Deposition of the mudstones and intercalated mudstones and sandstones took place in a base-of-slope and basin-floor fan environment. The succession in the GANT#1 well, which is situated close to the Kuugan - guaq–Qunnilik Fault, reflects a fault-controlled base-ofslope environment with major and minor distributary feeder channels, small turbidite lobes and interdistributary channel areas. Boundaries. The Umiivik Member unconformably overlies the Atane Formation on the north coast of Nuussuaq in a small and poorly exposed section at high altitude immediately east of the Ikorfat Fault (Fig. 22; A.K. Pedersen et al. 2006b). West of the Ikorfat Fault, the lower boundary of the Umiivik Member is not exposed and has not been drilled. On northern Nuussuaq, the member is unconformably overlain by the Kangilia Formation (Figs 72, 74, 87). At most localities on Svartenhuk Halvø, it is unconformably overlain by Paleocene hyaloclastic rocks of the Vaigat Formation (Fig. 73). At Firefjeld, however, a thin Paleo - cene conglomeratic unit that may be correlated with either the Agatdal Formation or the Quikavsak Formation is present between the Umiivik Member and the volcanic succession. Geological age. The age of the Umiivik Member is based on dinocyst and ammonite data (Birkelund 1965; Nøhr- Hansen 1996, 1997a). The ammonites from Svartenhuk Halvø indicate a ?Late Turonian – Early Campanian age for the Umiivik Member in this area (Fig. 16). Dinocysts 95
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GEOLOGICAL SURVEY OF DENMARK AND GR
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Contents Abstract . . . . . . . . .
Page 7 and 8:
Preface The onshore Cretaceous-Pale
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Introduction The Nuussuaq Basin bel
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chemistry of the Nuussuaq Basin hav
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Fig. 5. Plant fossils from the Atan
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Peak 2010 m Peak 1900 m Peak 1760 m
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A lithostratigraphy for the marine
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to provide further funding for stud
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DGR Geological setting As a result
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TSS 8 Agatdal Fm Eqalulik Fm Kangil
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A Svartenhuk Halvø 50 km B Hinterl
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Nuussuaq Group new group History. T
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ley (Figs 2, 40, 65). The section a
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Central Nuussuaq Agatdalen South co
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3 10 4 6 5 Qorlortorssuaq Slibesten
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volcanic sediments are referred to
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Fig. 20. View from Uummannaq toward
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In the Kuuk area, the sediments ove
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m m 15 14 14 13 12 11 10 9 8 7 6 5
Page 43 and 44: Kome Formation m 40 30 20 D tial re
Page 45 and 46: Fig. 28. Reference locality of the
Page 47 and 48: Vaigat Fm Vesterfjeld Slibestensfje
Page 49 and 50: Gilbert delta in the Ikorfat area (
Page 51 and 52: 150 300 450 100 250 400 m 550 50 20
Page 53 and 54: Fig. 36. Outcrop of the Upernivik N
Page 55 and 56: Correlation. The Upernivik Næs flo
Page 57 and 58: 12’ 09’ 15’ 06’ 03’ Saqqa
Page 59 and 60: m 0 GGU 247801 200 400 247815 ★
Page 61 and 62: wave-rippled sand streaked mudstone
Page 63 and 64: the formation in the marine mudston
Page 65 and 66: d d Fig. 47. Type locality of the S
Page 67 and 68: Fig. 49. Cross-bedded medium- to co
Page 69 and 70: and Qaarsut (Fig. 22). Its wider di
Page 71 and 72: Fig. 52. Two closely spaced section
Page 73 and 74: Type section. The type section of t
Page 75 and 76: Fig. 56. Delta front succession of
Page 77 and 78: Fig. 59. The Kingittoq Member at Ki
Page 79 and 80: sh L sh ch delta front Vaigat Forma
Page 81 and 82: Fig. 63. Type locality of the Itivn
Page 83 and 84: 782 Quaternary cover 54° 888 Malig
Page 85 and 86: Kuugannguaq-Qunnilik Fault and is o
Page 87 and 88: and include clasts of intraformatio
Page 89 and 90: deposited in a base-of-slope and ba
Page 91 and 92: VK 53°30’ 53°15’ Niaqornat Tu
Page 93: Umiivik-1 m Overburden ★ ★ No p
Page 97 and 98: Fig. 78. Type locality of the Kussi
Page 99 and 100: A B Itilli Formation Kussinerujuk M
Page 101 and 102: 160 140 120 100 Vaigat Formation Eq
Page 103 and 104: Fig. 85. Mudstones and conglomerati
Page 105 and 106: Fig. 87. Type section of the Kangil
Page 107 and 108: m 150 140 130 120 110 100 90 Kangil
Page 109 and 110: channellised, high-density currents
Page 111 and 112: Thickness. The Annertuneq Conglomer
Page 113 and 114: Fig. 96. A: Type locality of the Oy
Page 115 and 116: On Svartenhuk Halvø, on the east s
Page 117 and 118: Fig. 100. Reference locality of the
Page 119 and 120: Tupaasat Member Atane Formation Fig
Page 121 and 122: ever, have a fluvio-lacustrine orig
Page 123 and 124: etween Tupaasat and Nuuk Qiterleq a
Page 125 and 126: Vaigat Formation sill Quikavsak For
Page 127 and 128: Fig. 112. The sharp boundary betwee
Page 129 and 130: Agatdal Formation Eqalulik Formatio
Page 131 and 132: Fig. 116. Basal conglomerate unit o
Page 133 and 134: heterolithic deposits of the Kangil
Page 135 and 136: GANE#1 Vaigat Fm Anaanaa Mb m Hyalo
Page 137 and 138: Fig. 121. Well reference section of
Page 139 and 140: Pedersen 1978). The beds are usuall
Page 141 and 142: In detail, however, the boundary be
Page 143 and 144: Fig. 126. Composite type section of
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m m 240 340 m Pingu Member 230 230
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Naujât Member Atane Formation, Kin
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The TOC [Total Organic Carbon] cont
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Fig. 133. Correlation of the member
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Fig. 135. Type locality of the Ping
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Fig. 137. Lower, sharp boundary of
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m 130 125 110 t t invasive lava low
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Fig. 141. Upper part of the Assoq M
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Brown, R. 1875: Geological notes on
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a rosetted spreite trace fossil: Da
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ing bark from the Nûgssuaq peninsu
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1998: The syn-volcanic Naajaat lake
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Appendix: Place names and localitie
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Place name Place name P Paatuut sou
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Geological Survey of Denmark and Greenland Bulletin 19 ... - Geus

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