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

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The Itilli Formation is also exposed in the eastern part of the Svartenhuk Halvø area (Fig. 73; J.G. Larsen & Pulvertaft 2000) where it was cored in the Umiivik-1 well (Dam et al. 1998b). On Nuussuaq, the lower part of the formation (Early Campanian and older) is only present west of the Kuugannguaq–Qunnilik Fault (Chalmers et al. 1999 fold-out 2) where it is exposed in the Itilli valley area. In this area, the formation was cored in the FP94-9-01 (Fig. 65; Madsen 2000) and GANT #1 wells (Fig. 74; Dam 1996a). Type section. The type section of the Itilli Formation is located in the southern part of the Itillli valley along the Pingunnguup Kuua river and its tributaries, Ukalersalik and Anariatorfik (Figs 65, 66, Plate 2). The type section was described briefly by J.M. Hansen (1976, 1980a) and in detail by Dam & Sønderholm (1994). Neither the base nor the top of the formation is exposed in the type section. The base of the type section is located at 70°36.35´N, 54°13.79´W. Reference sections. Reference sections showing the lower boundary with the Atane Formation are exposed at Kussinerujuk and Asuk on the north coast of Disko (Figs 55, 77) and in the Aaffarsuaq valley on central Nuussuaq (Fig. 83). The upper boundary towards the Kangilia Formation is located on the north coast of Nuussuaq around Kangilia (Figs 72, 74, 87; Birkelund 1965; Rosenkrantz 1970; Henderson et al. 1976). The upper boundary towards the Eqalulik Formation is exposed at Qilakitsoq on central Nuussuaq (Figs 82, 83). Well reference sections are available from the fully cored boreholes FP94-9-01 (Madsen 2000), Umiivik-1 (Dam 1997), and GANT#1 (Dam 1996a). The formation was drilled but not cored in the GRO#3 well (Fig. 67; Kristensen & Dam 1997). For details on these wells, see below under description of members. Thickness. The formation is more than 1400 m thick at the type locality where the base and top of the formation are not exposed (Plate 2). In the nearby GRO#3 well, the formation is more than 2000 m thick (Fig. 67). The formation thins dramatically eastwards across the m 800 750 700 650 600 550 500 Not exposed (dyke) Not exposed Fig. 66. Expanded sedimentological log showing a representative portion of the Itilli Formation in the type section along the Pingunnguup Kuua river; the entire section, at a smaller scale, is shown in Plate 2. For legend, see Plate 1; for location, see Fig. 65. From Dam & Sønderholm (1994). 470 mud sand pebbles 84
Kuugannguaq–Qunnilik Fault and is only 240 m thick along the northern slopes of the Aaffarsuaq valley between Qilakitsoq and Tunoqqu. At Kangilia, on the north coast of Nuussuaq, the formation is at least 250 m thick (Fig. 87), and the nearby GANT#1 well penetrated 645 m of the formation without reaching the base of the formation. On Svartenhuk Halvø, the drilled and cored part of the formation is 960 m thick (excluding twenty-two Paleocene dolerite intrusions with a total thickness of 240.2 m), but the base of the formation was not reached (Fig. 75). At Kussinerujuk on the north coast of Disko, the measured part of the formation is 42 m thick (Fig. 77; Pulvertaft & Chalmers 1990). Series Stage Strat. Paleocene Danian Vaigat Fm Eqalulik Fm Agatdal Fm m 100 200 300 400 500 600 700 GRO#3 0 GR 300 240 DTC 40 Submarine canyon Lithology. In the type section, the Itilli Formation comprises mudstones, thinly interbedded sandstones and mudstones, chaotic beds, amalgamated beds of coarsegrained to very coarse-grained sandstone, and giant-scale cross-bedded sandstones (Figs 66, 68, 69, 70, Plate 2; Dam & Sønderholm 1994). These lithological contrasts are reflected in the blocky pattern in the petrophysical logs of the GRO#3 well (Fig. 67; Kristensen & Dam 1997). In the Aaffarsuaq area, the Itilli Formation comprises mudstones, thinly interbedded sandstones and mudstones, and amalgamated sandstone and conglomerate units together with chaotic beds comparable to those in the Itilli valley (Dam et al. 2000). The main differences between the Itilli and Aaffarsuaq areas are that most of the channellised amalgamated sandstone and conglomerate units in Aaffarsuaq are separated from the underlying deposits by major erosional surfaces or minor angular unconformities and that they are generally coarsergrained than their Itilli counterparts. Furthermore, the chaotic beds in Aaffarsuaq occur at many levels in the section and are not restricted to a position immediately underlying a channellised sandstone unit, and the interbedded sandstone and mudstone units often show an overall thinning-upward trend. The amalgamated sandstone and conglomerate units of the Aaffarsuaq area consist of very coarse- to mediumgrained sandstone and conglomerate beds grading upward into thinly interbedded sandstones and mudstones. These coarse-grained units are up to 50 m thick, extend laterally beyond the extent of outcrop (several hundred metres) Upper Cretaceous No palynomorphs recorded due to thermal influence Campanian lower Maastricht. upper Maastricht. Con. Kangilia Fm Itilli Formation Anariartorfik Member 800 900 1000 1100 1200 1300 1400 1500 1600 1700 1800 1900 2000 2100 2200 2300 2400 2500 2600 2700 2800 Submarine canyon Slope 2900 Fig. 67. Lithological log of the GRO#3 well interpreted from petrophysical data. GR, Spectral gamma-ray log; DTC, Sonic log; Con., Coniacian; Maastricht., Maastrichtian; Strat., lithostratigraphy; T.D., total depth. Modified from Christiansen et al. (1999). For location, see Fig. 65. 3000 T.D.: 2996 m Hyaloclastite Intrusion Mudstone Sandstone 85
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GEOLOGICAL SURVEY OF DENMARK AND GR
Page 4 and 5:
Contents Abstract . . . . . . . . .
Page 7 and 8:
Preface The onshore Cretaceous-Pale
Page 9 and 10:
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
Page 17 and 18:
A lithostratigraphy for the marine
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to provide further funding for stud
Page 21 and 22:
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
Page 31 and 32:
Central Nuussuaq Agatdalen South co
Page 33 and 34: 3 10 4 6 5 Qorlortorssuaq Slibesten
Page 35 and 36: volcanic sediments are referred to
Page 37 and 38: Fig. 20. View from Uummannaq toward
Page 39 and 40: In the Kuuk area, the sediments ove
Page 41 and 42: 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: 782 Quaternary cover 54° 888 Malig
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 and 94: Umiivik-1 m Overburden ★ ★ No p
Page 95 and 96: 76). Heavily bioturbated interbedde
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
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Fig. 121. Well reference section of
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Pedersen 1978). The beds are usuall
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In detail, however, the boundary be
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Fig. 126. Composite type section of
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m m 240 340 m Pingu Member 230 230
Page 147 and 148:
Naujât Member Atane Formation, Kin
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The TOC [Total Organic Carbon] cont
Page 151 and 152:
Fig. 133. Correlation of the member
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Fig. 135. Type locality of the Ping
Page 155 and 156:
Fig. 137. Lower, sharp boundary of
Page 157 and 158:
m 130 125 110 t t invasive lava low
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Fig. 141. Upper part of the Assoq M
Page 161 and 162:
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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