Geological Survey of Denmark and Greenland Bulletin 37, 1-74 + Appendices GEOLOGICAL SURVEY OF DENMARK AND GREENLAND BULLETIN 37· 2016 Biostratigraphic correlation of the western and eastern margins of the Labrador–Baffin Seaway and implications for the regional geology Henrik Nøhr-Han sen, Graham L. Williams & Robert A. Fensome GEOLOGICAL SURVEY OF DENMARK AND GREENLAND MINISTRY OF ENERGY, UTILITIES AND CLIMATE Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 1 Geological Survey of Denmark and Greenland Bulletin 37 Keywords Baffin Margin, Labrador Margin, offshore West Greenland, Cretaceous, Cenozoic, biostratigraphy, palynology, dinocysts, palaeoenvironments Cover illustration The Canadian icebreaker Amundsen in Blanley Bay, southern Devon Island in the Canadian Arctic in the autumn of 2013. Immediately south-east of this locality, across Lancaster Sound, is Bylot Island where Cretaceous–Paleocene sediments are exposed. Photo: Kate Jarrett (GSC). Frontispiece: facing page Survey drilling team in Agatdalen, central Nuussuaq, West Greenland, recovering core from the lower–middle Campanian Aaffarsuaq Member (Itilli Formation); the mountain in the background is composed of Paleocene volcanic rocks of the Vaigat Formation. Such fully cored stratigraphic wells have been invaluable in documenting the detailed stratigraphy of the onshore area of the West Greenland Margin. Chief editor of this series: Adam A. Garde Editorial board of this series: John A. Korstgård, Department of Geoscience, Aarhus University; Minik Rosing, Geological Museum, University of Copenhagen; Finn Surlyk, Department of Geosciences and Natural Resource Management, University of Copenhagen Scientific editor of this volume: Jon R. Ineson Editorial secretary: Jane Holst Referees: Raquel Guerstein (Argentina) and Gregers Dam (Denmark) Illustrators: Jette Halskov (GEUS) and Bill MacMillan (GSCA) Digital photographic work: Benny M. Schark Graphic production: Annabeth Andersen Printers: Rosendahls · Schultz Grafisk · Denmark Manuscript received: 21 January 2015 Final version approved: 17 March 2016 Printed: 28 December 2016 ISSN (print) 1604-8156 ISSN (online) 1904-4666 ISBN (print) 978-87-7871-445-9 ISBN (online) 978-87-7871-447-3 Citation of the name of this series It is recommended that the name of this series is cited in full, viz. Geological Survey of Denmark and Greenland Bulletin. If abbreviation of this volume is necessary, the following form is suggested: Geol. Surv. Den. Green. Bulletin 37, 74 pp. Available from Geological Survey of Denmark and Greenland (GEUS) Øster Voldgade 10, DK-1350 Copenhagen K, Denmark Phone: +45 38 14 20 00, fax: +45 38 14 20 50, e-mail: geus@geus.dk or at www.geus.dk/publications/bull © De Nationale Geologiske Undersøgelser for Danmark og Grønland (GEUS), 2016 For the full text of the GEUS copyright clause, please refer to www.geus.dk/publications/bull Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 2 Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 3 4 Contents Abstract . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Introduction . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Tectonic setting . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Labrador Sea . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Davis Strait and Baffin Bay . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . General stratigraphy . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Offshore . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Labrador Margin . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . West Greenland Margin . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Baffin Margin . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Onshore . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . West Greenland . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . North-eastern Canada . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Methodology . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Previous palaeontological studies . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Biostratigraphic results . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Lower Cretaceous . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Aptian . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Albian . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Upper Cretaceous . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Cenomanian . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Turonian–Santonian. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Campanian . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Maastrichtian . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Palaeogene . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Danian–Selandian . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Thanetian . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Ypresian . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Lutetian . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Bartonian . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Priabonian . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Rupelian . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Chattian . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Neogene . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Miocene . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Pliocene–Pleistocene . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Discussion . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Cretaceous . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Palaeogene . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Neogene . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Palaeoenvironmental results . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . General considerations . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Palaeoenvironments and dinocysts: previous studies . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Previous palaeoenvironmental interpretations from the Labrador–Baffin Seaway . . . . . . . Results and interpretations . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Cretaceous . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Cenozoic . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 7 9 11 11 11 12 12 12 13 16 16 16 17 18 20 21 21 21 23 23 23 23 24 25 25 25 26 28 29 29 29 30 30 30 30 31 32 32 32 33 36 36 37 39 39 39 40 Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 4 Palaeogeography, palaeoclimatology and palaeoceanography . . . . . . . . . . . . . . . . . . . . . . Conclusions . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Acknowledgements . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . References . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Appendix 1 . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Appendix 2 . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Appendix 3 . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 5 44 48 49 50 60 67 74 Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 5 Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 6 7 Abstract Authors’ addresses H.N.-H., Geological Survey of Denmark and Greenland, Øster Voldgade 10, DK-1350 Copenhagen K, Denmark. E-mail: hnh@geus.dk G.L.W. & R.A.F., Geological Survey of Canada (Atlantic), Natural Resources Canada, PO Box 1006, 1 Challenger Drive, Dartmouth, Nova Scotia B2Y 4A2, Canada. New analyses of the palynological assemblages in 13 offshore wells on the Canadian margin and six on the West Greenland Margin, in conjunction with onshore data, have led to a new biostratigraphic framework for the Cretaceous–Cenozoic strata of the Labrador Sea – Davis Strait – Baffin Bay (Labrador–Baffin Seaway) region and the first broad biostratigraphic correlation of the Canadian and Greenland margins. This framework is based on 167 last occurrences and 18 local/regional peak/ common-occurrence events for dinocysts, miospores, fungal spores and Azolla. Detailed biostratigraph- ic evidence has confirmed the following hiatuses: pre-Aptian in the Hopedale Basin; pre-Albian in the Saglek Basin; Albian–Turonian in some wells of the Hopedale Basin; Turonian–Santonian/Campanian in some areas; pre-Campanian and late Campanian – Thanetian on the Greenland Margin; late Maastrichtian and Danian in some wells of the Hopedale Basin and in the Saglek Basin; Selandian in part of the Hopedale Basin, in all the Saglek Basin wells and in two wells on the West Greenland Margin; late Ypresian and/or Lutetian on both sides; Oligocene to middle Miocene of considerable vari- ability on both margins, with all of the Oligocene and the lower Miocene missing in all the West Greenland Margin wells; and middle to late Miocene on the western side. On the Canadian margin, the hiatuses can be partially matched with the five previously recognised regional unconformities; on the Greenland margin, however, the relationship to the five unconformities is more tenuous. Palyno - morph assemblages show that most Aptian to Albian sediments were deposited in generally non-marine to marginal marine settings, interrupted by a short-lived shallow marine episode in the Aptian. A marine transgression started in the Cenomanian–Turonian and led to the most open-marine, oceanic condi- tions in the Campanian–Lutetian; shallowing probably started in the late Lutetian and continued into the Rupelian, when inner neritic and marginal marine palaeoenvironments predominated. Throughout the rest of the Cenozoic, inner neritic palaeoenvironments alternated with marginal marine conditions on the margins of the Labrador–Baffin Seaway. These observations broadly reflect the tectonic evolu- tion of the seaway, with rift conditions prevailing from Aptian to Danian times, followed by drift through much of the Paleocene and Eocene, and post-drift from Oligocene to the present. Dinocysts indicate that climatic conditions in the Labrador–Baffin Seaway region were relatively temperate in the Cretaceous, but varied dramatically through the Cenozoic. The Danian was a time of increasingly warmer climate, a thermal maximum being reached around the Paleocene–Eocene boundary reflecting the global thermal event at this time. Warm to hot conditions prevailed throughout the Ypresian, but the climate began to cool in the Lutetian, a trend that accelerated through the Priabonian and Rupelian. Throughout the Neogene, temperatures generally declined, culminating in the Quaternary. Nøhr-Hansen, H., Williams, G.L. & Fensome, R.A. 2016: Biostratigraphic correlation of the western and eastern margins of the Labrador–Baffin Seaway and implications for the regional geology. Geological Survey of Denmark and Greenland Bulletin 37, 74 pp. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 7 8 r CanadaCanada Ellesmere Island 70°N 60°N 45°W55°W65°W Labrado r Nuussuaq Nuussuaq Basin Hareøen Disko Bylot Island Cape Dyer Scott Inlet Buchan Gulf Quqaluit/ Padloping islands Saglek B asin 646 112 113 645 Umiivik-1 Delta-1 T4-1 T8-1 Alpha-1/S1 Gamma-1 Hellefisk-1 AT7-1 AT2-1 LF7-1 Ikermiut-1 Nukik-2 Nukik-1 Qulleq-1 Gjoa G-37 Ralegh N-18 Hekja O-71 Rut H-11 Gilbert F-53 Karlsefni A-13 Skolp E-07 Pothurst P-19 Ogmund E-72 Snorri J-90 Bjarni O-82 Bjarni H-81 Herjolf M-92 North Bjarni F-06 Roberval K-92 North Leif I-05 Cartier D-70 Hare Bay E-21 Freydis B-87 South Labrador N-79 Kangâmiut-1 647 HopedaleBasin Cum berland Sound H om e Bay B af f in Is lan d Canada D a v is S t ra i t La b ra d o r S e a GRO#3 250 km Baffin Bay Greenland H udson Stra i t 75°W Shallow cored borehole Greenland–Canada border ODP or DSDP borehole Exploration well with gas shows Exploration well Exploration well with oil and gas shows 500 km Greenland Labrador Sea Baffin Bay D avis Strait Nar es St ra it B a ffin Isla n d 60°N 60°W 40°W 70°N 80°N Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 8 Canada and Greenland are separated, from south to north, by the Labrador Sea, the Davis Strait, Baffin Bay (referred to here collectively as the Labrador–Baffin Sea way), and the narrow Nares Strait (Fig. 1). As sum - marised in Monger et al. (2014) and Fensome et al. (2014), the Labrador–Baffin Seaway originated as a series of rift basins that developed successively from south to north during the Early Cretaceous, and which ultimately became connected to form a seaway in the Late Cretaceous. A drift phase in the seaway, causing the Greenland Plate to rotate away from North America, was heralded by an episode of volcanic activity between 62 and 56 million years ago, perhaps resulting from the passage of the Icelandic mantle plume (Dam et al. 1998a; Larsen et al. 2016). This episode involved vast outpourings of basalt in central West Greenland and south-eastern Baffin Island. As drift ensued, sea-floor spreading resulted in progressive widening of the La b - rador–Baffin Seaway until the Priabonian. This devel- opment meant that Greenland changed course, its northern end colliding with Arctic Canada, resulting in an episode of deformation known as the Eurekan Oro g - eny. The collision inhibited the rotation of Green land away from North America, and sea-floor spreading in the Labrador–Baffin Seaway ceased around the latest Eocene. From that time on, sea-floor spreading in the northern North Atlantic Ocean occurred only between Greenland and northwestern Europe, where a spread- ing axis had opened about 55 million years ago. Thus, until this time, Greenland was part of Laurasia, be - tween about 55 and 35 million years ago it constituted a separate plate, and after 35 million years ago it became part of the North American Plate. The Labrador–Baffin Seaway stretches from about 52°N to 75°N, a distance of roughly 2500 km (Fig. 1). Knowledge of the timing of the geological evolution of the Seaway is based primarily on biostratigraphic anal - yses on exploration wells drilled between 1971 and 2000 on the Labrador Margin, offshore West Green - land and in the Davis Strait, and from some shallow cored boreholes drilled in Baffin Bay in the 1970s and 1980s and in the Nuus suaq Basin in the 1990s (Fig. 1). Additional information comes from numerous Creta - ceous–Ceno zoic out crop sections in the Nuussuaq Basin in West Green land, a few onshore sections in Labrador and on Baffin and Bylot Islands, and from ODP Leg 105, hole 645 in Baffin Bay (Fig. 1). Although previous work on these wells and sections has provided a good stratigraphic foundation for the Cretaceous–Cenozoic of the region, renewed petroleum exploration interest in recent years has revealed gaps in our knowledge and a need to correlate the western and eastern margins of the seaway. Consequently, for the past decade the Geological Survey of Denmark and Greenland (GEUS) and the Geo logical Survey of Canada (Atlantic) (GSCA) have undertaken an exhaustive palynological study, with the goal of providing more detailed age control. This study is based on palynological analysis of more than 2000 well samples from the Labrador Margin, the Davis Strait and offshore West Greenland. Organic-walled dino flagellate cysts (dinocysts) are the primary palyno morph group eva l ua ted, but spores and pollen (mio spores), a fern micro spore massula (Azolla), algal and fungal microfos- sils and acritarchs have also been considered. The new age determinations presented here and docu- mented in detail in a companion publication (Fensome et al. 2016) are more precise than those of previous stud- ies because of advances made in refining the stratigraphic ranges of dinocysts (e.g. Williams et al. 2004). Moreover, the number of species for which detailed stratigraphic information is available has increased immeasurably since early studies in the region in the 1970s. Using the more detailed stratigraphic data, 187 bioevents are iden- tified for the Labrador–Baffin Seaway. Some events are coeval, so the 187 bio events define 106 bioevent hori- zons. Bioevent data are also incorporated from Piasecki (2003) for the Neo gene of offshore West Greenland and from Pedersen & Nøhr-Hansen (2014) for Albian to Paleocene strata of the Nuussaq Basin, West Greenland. In addition to biostratigraphic determinations, palaeoen- vironmental inferences are made from the data, using, for example, individual dinocyst species and dinocyst assem- blages. We have also endeavoured to decipher palaeo - oceanographic conditions and palaeoclimates, the results revealing similarities to high southern latitudes in the Late Cretaceous. 9 Introduction Facing page: Fig. 1. Map of the Labrador–Baffin Seaway showing the location of relevant wells, boreholes and onshore localities; wells and boreholes shown in red were used in this study. Inset map shows the regional context of the Labrador–Baffin Seaway between Canada and Greenland. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 9 10 rre s es S t ai t Island ■■ ■■ ■ ■ ■ ■ ■ ■ ■ ■ ■■ ■■ ■■ ■ ■ ■ ■ ■ ■ ■ ■ ■■ ■ ■ ■ ■ ■■ ■ ■ ■ ■ ■ ■ ■■ ■ ■ ■ ■ ■ ■ ■■ ■■ ■■ ■■ ■ ■ ■■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■■ ■ ■ ▲ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■■ ■■ ■ ■ ■ ■ ■ ■ ■ ■ ■■ ■■ ■ ■ ■ ■ ■■ ■■ ■ ■ ■ ■ ■■ ■ ■ ■ ■ ■■ ■■ ■■ ■ ■ ■ ■ ■ ■ ■■ ■■ ■ ■ ■■ ■■ ■■ ■ ■ ■ ■ ■ ■ ■ ■ ■■ ■■ ■ ■ ■ ■ ■ ■ ■ ■ ■■ ■■ ■■ ■ ■ ■ ■ ■■ ■ ■ ■ ■ ■■ ■■ ■■ ■ ■ ■■ ■■ ■■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■■ ■■ ■■ ■ ■ ■■ ■■ ■■ ■■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■ ■■ ■ ■ ■■ ■ ■■ ■ ■■ ■ ■ ■ ■ ■ ■ ■■ ■■ ■■ 646 112 113 645 Rut H-11 Gilbert F-53 Karlsefni A-13 Pothurst P-19 Skolp E-07 Ogmund E-72 Snorri J-90 Bjarni O-82 Roberval K-92 North Leif I-05 Freydis B-87 Cartier D-70 Herjolf M-92 North Bjarni F-06 250 km South Labrador N-79 647 Saglek Basin Hellefisk-1 Ikermiut-1 Nukik-2 Delta-1 T4-1 T8-1 Gamma-1 Alpha-1/S1 Nukik-1 Qulleq-1 LF7-1 AT2-1 AT7-1 Gjoa F-37 Ralegh N-18 Hekja O-71 Kangâmiut-1 Nuussuaq Svartenhuk Halvø Disko Cape Dyer Umiivik-1 GRO#3 45°W 35°W Sediments, large basins (400–0 Ma) Oceanic crust, Eocene Oceanic crust, age uncertain Basalts and intrusives (60–30 Ma) Basement locally covered by sediment Spreading axis Extensional fault Compressional fault thrust Transition fault ODP or DSDP borehole Oceanic crust, Paleocene Exploration well Exploration well with gas shows, Exploration well with oil and gas shows Shallow cored borehole Fault (undifferentiated) Paam iut B asin N u u k B as in K an gâ m iu t B as in Lady Franklin Basin Sisimiut Basin Disko Bugt Ik er m iu t B as in H o m e B ay B asin Lancaster Basin Eclipse Trough M elville Bay G raben Buchan G raben Scott G raben D av is S tr ai t H ig h Baffin Basin N u u ss u au q B as in Labrado r Labrador Sea Hudson Strait C um berland Sound M elville Bay K ivioq Basin Canada Greenland Bylot Island Baffin Island 65°W 55°W 45°W 60°N 70° 70°N 55°W65°W75°W H opedale Basin Hawke Basin West Greenland Volcanic Province Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 10 11 Labrador Sea Kerr (1967) and Grant (1980) considered the Labrador Sea to be floored by foundered continental crust. Umpleby (1979) explained the formation of this sea - way by using a modification of the Undation Theory of Van Bemmelen (1949, 1972), but still considered that there was no underlying oceanic crust. The seismic, mag netic and gravity data (Le Pichon et al. 1971; Srivastava 1978), however, strongly supported a plate- tectonic model of lithospheric extension and spreading, accompanied by generation of oceanic crust. Srivastava (1978) considered the oldest oceanic crust in the south- ern Labrador Sea to be assignable to Anomaly 34 (Coniacian–Santonian) and in the north to Anomaly 31 (Maastrichtian). He observed that a change in the direction of spreading occurred between Anomaly 25 (early Thanetian) and Anomaly 24 (late Thanetian to early Ypresian), and noted that Anomaly 13 (late Pria - bonian to earliest Rupelian) and subsequent anomalies were missing. Roest & Srivastava (1989) and Srivastava & Roest (1999) interpreted the oldest oceanic crust in the La b - rador Sea as Anomaly 33 (most of the Campanian; 73.6–79 Ma). However, biostratigraphic analyses of the Qulleq-1 well, offshore West Greenland, demonstrated that the well reached total depth (TD) in Santonian sedimentary rocks (Nøhr-Hansen et al. 2000; Christi - ansen et al. 2001; Henriksen et al. 2009), which would imply that the crust underlying Qulleq-1 is the oldest- known oceanic crust north of 56°N in the Atlantic (Henriksen et al. 2009). However, Chalmers (1991) and Chalmers & Laursen (1995) could not identify any anomalies in the Labrador Sea older than Chron 27n (latest Danian) and concluded that sea-floor spreading began between 63 and 61.7 Ma (latest Danian), and that a transition zone exists between continental and oceanic crust. The interpretations of Chalmers (1991) were later supported by those of Chalmers & Pulvertaft (2001) and Oakey & Chalmers (2012), and followed by Sønder holm et al. (2003a, b). Moreover, Funk et al. (2007, 2012) suggested that the crust underlying Qulleq-1 is of continental origin. Based in part on the understanding of magnetic ano - malies at the time and in part on biostratigraphy, Balk - will & MacMillan (1990) proposed three megasequences for the lithostratigraphic units encountered in offshore wells: synrift (Neocomian to Campanian), drift (Late Cre taceous to Eocene), and post-drift (Oligocene to Recent). Similarly, but based on updated knowledge of the timing of sea-floor spreading, Sønder holm et al. (2003b) recognised: an initial rifting phase (Phase 1) in the Early Cretaceous, a continued rifting phase (Phase 2) in the Late Cretaceous to Danian, and a subsequent drift and post-drift phase (Phase 3). Sønderholm et al. (2003b) speculated that Phase 1 may have started in the Jurassic based on tentative observations by Dalhoff et al. (2006) and Piasecki (2003), a notion supported by Larsen et al. (2009) who indicated that lithospheric stret ching between Canada and West Greenland prob- ably started in Jurassic time. On the western margin of the Labrador Sea from south to north is a series of roughly SE–NW-aligned basins separated by basement highs, or arches, oriented perpendicular to the basins (Fig. 2). Exploration wells have been drilled in two of the basins, the Hopedale and Saglek Basins. Davis Strait and Baffin Bay The Davis Strait High, where water depths can be as shallow as about 600 m, forms the northern periphery of the Labrador Sea and sits above a major transform margin that developed around the Paleocene–Eocene transition (Oakey & Chalmers 2012). Today, the Davis Strait connects the Labrador Sea with Baffin Bay. As was the case for the Labrador Sea, both non-plate-tec - tonic and plate-tectonic models have been proposed for Baffin Bay. Kerr (1967) and Grant (1975) considered Baffin Bay to be underlain by continental crust modi- fied by basalt intrusions. Keen et al. (1972) and Sriva - stava (1978), however, postulated that oceanic crust Tectonic setting Facing page: Fig. 2. Map of the basic geology of the Labrador–Baffin Seaway, showing the main structural features and relevant well/borehole locations; wells and boreholes shown in red were used in this study. Modified from Henriksen et al. (2009) and Oakey & Chalmers (2012). Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 11 12 General stratigraphy underlies Baffin Bay. Support for a plate-tectonic origin was provided by Jackson et al. (1979), who identified anomalies 21 (earliest Lutetian) to 13 (late Priabonian to earliest Rupelian). Oakey (2005) recognised two sets of linear magnetic anomalies trending NNW–SSE and NW–SE, which correspond respectively to the Paleo - cene and Eocene anomalies in the Labrador Sea. Har - rison et al. (2011) considered Baffin Bay to be under lain in part by oceanic crust, formed between Chron 27 and Chron 13 – i.e. late Danian to earliest Rupelian (Fig. 2). In the east of Baffin Bay, off West Greenland, is a series of roughly SE–NW- and S–N-aligned basins separated by basement highs or ridges oriented parallel or oblique to the basins (Fig. 2). Some of these basins along the south-western part of the West Greenland Margin were penetrated by wells drilled between 1976 and 2000: Qulleq-1 in the Paamiut Basin, Nukik-1 and Nukik-2 in the Nuuk Basin, Kangâmiut-1 in the Kan - gâ miut Basin and Ikermiut-1 in the Sisimiut Basin. Another well, Hellefisk-1, was drilled in the same peri- od within the West Greenland Volcanic Province (Figs 1, 2). The oil company Cairn drilled eight exploration wells in 2010 and 2011: one in the Lady Franklin Basin (LF7-1), two in the Nuuk Basin (AT2-1, AT7-1), and five in the West Greenland Volcanic Province (Delta-1, T4-1, T8-1, Alpha-1/S1, Gamma-1; Fig. 2); none of the samples or data from these wells are yet released. Offshore Labrador Margin A formal Cretaceous–Cenozoic lithostratigraphic scheme was proposed for Labrador Margin wells by Umpleby (1979) and modified by McWhae et al. (1980); the ver - sion adopted here (Fig. 3) is that with the timescale cali- brated by Sørensen (2006, fig. 2) and modified by Dickie et al. (2011). The oldest rocks in some wells in the Hopedale and Saglek Basins are igneous or metamorphic and of Pre - cambrian age. In other wells in the two basins, the oldest rocks are Ordovician or Carboniferous. Separa ting these basement rocks from overlying Cretaceous and Cenozoic strata is an unconformity, termed the Labrador Uncon - formity by McWhae et al. (1980) and McWhae (1981; Fig. 3). McWhae (1981) gave an age of 130 to 120 Ma for the Labrador Unconformity though the timescale on which this was based is not clear. The oldest Cretaceous unit is the Alexis For mation, which consists of basalts with subordinate claystone, siltstone and sandstone (Fig. 3). Corgnet & McWhae (1973) determined radiometric ages of 139 ± 7 Ma and 122 ± 6 Ma for two basaltic cores from the type section of the Alexis For mation in Bjarni H-81, viz. Valanginian to early Aptian on the timescale of Gradstein et al. (2012). Sørensen (2006, fig. 2) gave an age of Barremian to Al - bian for the Bjarni Formation, which overlies the Alexis Formation. The Bjarni Formation is a predominantly sand stone unit and the main hydrocarbon reservoir in the Hopedale Basin (Figs 2, 3). According to McWhae (1981), the Bjarni Formation is separated from the over- lying Markland Formation by the Avalon Unconformity, which McWhae considered to range from 100 to 85 Ma (timescale not specified). The Markland Formation con - sists mainly of a distal mudstone facies and its proximal sandstone equivalent, the Freydis Member. Sønderholm et al. (2003b) determined an age of Cenomanian to earli- est Paleocene for the Markland Formation. A sandstone unit at the top of the Markland Formation, the informal lower Gudrid member, straddles the Cretaceous–Palaeo - gene boundary (Sørensen 2006). Overlying the Markland Formation is the Cart wright Formation, which is predominantly a mudstone unit of Paleocene age (Sørensen 2006). In the Saglek Basin, the Cartwright Formation has lower and upper proximal sandstone facies, informally termed the mid dle and up - per Gudrid members respectively (Balkwill & McMillan 1990). Separating the middle and upper Gudrid members is the Bylot Unconformity; the duration of the hiatus was dated by McWhae (1981) as being Danian, 60–63 Ma (timescale not specified) and which Dickie et al. (2011) placed at the Danian–Selan dian boundary. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 12 13 A major volcanic episode occurred in the northern Labrador Sea, the Davis Strait and southern Baffin Bay (Figs 2, 3) during the Paleocene to early Eocene. In the Rut H-11 well in the Saglek Basin, supposed tuff beds from this volcanic episode are reported to underlie the Upper Cretaceous – Danian Markland Formation, yet have been dated as 59 Ma (Klose et al. 1982). A thick sequence of basalts in Gjoa G-37 appears to be coeval with the tuff beds in Rut H-11, with two basalt samples dated at 59.5 ± 1.0 Ma and 59.2 ± 1.8 Ma (Williamson et al. 2001). In Gjoa G-37, however, the basalts occur above the Markland Formation; the implication is that the volcanic rocks in Rut H-11 are of intrusive origin. Also of closely similar age are the Cape Dyer volcanics, dated at 58 ± 2 Ma (Clarke & Upton 1971). William - son et al. (2001) gave ages of 62.9 ± 2.5 Ma and 55.1 ± 2.3 for two basalt cores recovered off Cape Dyer. These volcanics may be related to the transform margin that was developing in the northern Saglek area through the Davis Strait, or to the onset of sea-floor spreading in southern Baffin Bay. On the Labrador Margin, the top of the informal upper Gudrid member, and thus of the Cartwright For mation, roughly corresponds to the Paleocene–Eocene boundary. Successively above these rocks are the Ken amu (Eocene), Mokami (Oligocene to Miocene) and Sag lek (middle Miocene to Pleistocene) Formations. Each of these units consists broadly of a mudstone se quence that becomes sandier and even conglomeratic upwards. McWhae et al. (1980) recognised a regional unconformity, the Baffin Bay Unconformity, between the Kenamu and Mokami For mations. These authors also named the regional un - con formity between the Mo kami and Saglek Formations as the Beaufort Uncon formity. McWhae (1981) consid- ered the hiatus at the Baffin Bay Unconformity to be with- in the early Oligo cene, 38–34 Ma; he placed the Beaufort Unconformity in the early to middle Miocene, between 20 and 15 Ma (timescale not specified). West Greenland Margin Rolle (1985) formally defined seven formations from well sections released at that time in offshore West Greenland (Fig. 3). He assigned the oldest rocks, a sequence of interbedded mudstones and sandstones, to the Narssarmiut Formation and considered this to be equivalent to the Freydis Member of the Markland Formation to the west, and thus of Campanian age. Based on this study, the Narssarmiut Formation is now considered to be of Selandian age (Fig. 3). According to Rolle (1985), the Narssarmiut For - mation is unconformably overlain by the Ikermiut For - mation, which comprises carbonaceous mudstone with some siltstone and sandstone. Rolle (1985) considered the Ikermiut Formation to be of Campanian to middle Eocene age and correlated it with the Markland and Cartwright Formations of the Labrador Margin. If these correlations are correct, then the Ikermiut For - mation would straddle the Bylot Unconformity. In - deed, Sønderholm et al. (2003b) illustrated the pre sence of a major hiatus within the Ikermiut Formation, possi- bly spanning the late Campanian to earliest Paleocene and thus equivalent to the Bylot Unconformity. The Hellefisk Formation occurs only in the Hellefisk-1 well. Rolle (1985) dated it as Thanetian to Eocene and consid- ered that it may interfinger laterally with the Ikermiut Formation; we consider it to be a correlative of the upper part of the Ikermiut Formation (Fig. 3). Palaeogene formations of the West Greenland Mar - gin are all siliciclastic, with mudstones dominant. The Ataneq Formation is mudstone-dominated; sandstone- dominated units are the Nukik, Kangâmiut and Manît - soq Formations. Current age determinations of all these formations in individual wells are shown in Fig. 3, based on work by Dalhoff et al. (2003), Nøhr-Hansen (2003), Rasmussen et al. (2003), Rasmussen & Sheldon (2003), Sheldon (2003) and the results of this study. Neogene sediments are generally upward-coarsening sequences of marine mudstones interbedded with well- sorted fine-grained sandstones. Although the lithostratigraphy of the West Green - land Margin confirmed in well sections extends back only to the Santonian, older Mesozoic strata are evident from seismic data. Three seismic sequences have been recognised within the Cretaceous succession (Fig. 3). From oldest to youngest, these are the Kitsissut (which probably includes volcanics), Appat and Kangeq se quences (Chalmers et al. 1993, 1995; Chalmers & Pul vertaft 2001). The Kitsissut sequence may be coeval with the lower part of the Bjarni Formation, with the inferred volcanics equivalent to the Alexis Formation. The Kangeq sequence has been partly drilled in the Ikermiut-1 and Qulleq-1 wells, where the succession en countered is of early Cam - panian (Sønderholm et al. 2003b) and San to nian–Cam - panian (Christiansen et al. 2001) age, re spec tively. The mudstone-dominated Kang eq sequence is the lithologi- cal equivalent of the Markland Formation of the Lab - rador Margin. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 13 14 Upper Cretaceous Paleocene Eocene Oligocene Miocene Pliocene Quaternary Lower Cretaceous 0 Ma 5 10 15 20 25 30 35 40 45 50 55 60 65 70 75 80 85 90 95 100 105 110 115 120 125 130 135 140 145 Aptian Barremian Hauterivian Valanginian Berriasian Albian Cenomanian Turonian Coniacian Santonian Campanian Maastrichtian Danian Selandian Thanetian Ypresian Lutetian Bartonian Priabonian Rupelian Chattian Aquitanian Burdigalian Langhian Serravallian Tortonian Messinian Zanclean Piacenzian C28 C29 C30 C31 C32 C33 C34n C34n C34n C34n M"-3"r M"-2"r M"-1"r C27 C26 C25 C24 C22 C21 C20 C19 C18 C17 C23 C16 C15 C13 Magnetostrat. (Polarity, Chron) Chronostratigraphy Uncon- formitiesShelf Basin Labrador MarginSW NE Labrador Trough erosion Leif Mb upper Freydis Mb lower Freydis Mb upper and middle Gudrid mb lower Gudrid mb Sa gle k F m Mokami Fm lower Kenamu Fm Cartwright Fm lower lower upper upper upper Bjarni Fm Alexis Fm Markland Fm (Labrador U nc.) (Avalon Unc.) (Bylot Unc.) Bylot Avalon Labrador Baffin Bay Beaufort (Baffin Bay Unc.) (B eaufort U n c. ) Fig. 3. Stratigraphic framework of the Mesozoic–Cenozoic rocks of the Labrador and West Green - land margins and adjacent on - shore sections; modified from Gregersen et al. (2013). The La - brador Margin stratigraphy is from Dickie et al. (2011), with unconformities from McWhae (1981). The West Greenland Mar gin stratigraphy is based on well stratigraphic studies by Rolle (1985), Nøhr-Hansen (2003) and Sønderholm et al. (2003); the deeper sub-well section is based on Chalmers et al. (1993), Chal - mers & Pulvertaft (2001) and Sørensen (2006). The Nuussuaq Basin stratigraphy is from Storey et al. (1998), Dam et al. (2009), Pedersen & Nøhr-Hansen (2014) and Larsen et al. (2015); these pa - pers and this study are the source of the inferred ages. The south- east Baffin Island stratigraphy is from Burden & Langille (1990) and Pedersen et al. (2002), the Home Bay and Scott Inlet seabed samples from MacLean et al. (2014) and the north Baffin Is - land stratigraphy is based on Jack - son et al. (1978) and McWhae (1981). The Bylot Island strati - graphy is from Miall (1986), Waterfield (1989), and Harrison et al. (1999). The timescale (Ma) and magnetostratigraphy are from Gradstein et al. (2012). Fm: For - mation (formal). fm: formation (informal). Mb: Member (for - mal). mb: member (informal). Unc.: unconformity. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 14 15 H el le fis k- 1 G R O # 3 U m iiv ik -1 Ik er m iu t- 1 K an gâ m iu t- 1 N u ki k- 2 N u ki k- 1 Q u lle q -1 West Greenland Margin Kangilia Fm Nuussuaq Basin SE Baffin IslandNWSES N Bylot Island Itilli Fm Atane Fm ? Itilli Fm (Ikermiut Fm) Kangeq sequence Ikermiut Fm Ikermiut Fm Narssarmiut Fm Kangâmiut Fm Kangâmiut Fm Kangâmiut Fm Kangâmiut Fm Hellefisk FmNukik Fm Nukik Fm ? ? ? ? ? ? ? ? ? ? ? Ataneq Fm Ataneq Fm Manîtsoq Fm Manîtsoq Fm Manîtsoq Fm Fylla sand Erqua Fm Naqerlog Fm Hareøen Fm (Hareøen) Youngest volcanics Quqaluit Fm Cape Searle Fm N u u ss u aq G ro u p (Home Bay – Scott Inlet) Cape Dyer Basalt Maligât Fm Svartenhuk Fm Vaigat Fm Atanikerluk Fm Eqalulik Fm Quikavsak Fm Kome Fm Basalts? Sills/dykes Appat sequence Kitsissut sequence ? ? Upernivik Næs Fm Slibestens- fjeldet Fm Hassel Fm (Labrador Unc.) Sermilik fm Kanguk Fm Aktineq fm Pond Inlet fm Navy Board fm Bylot Island fm Agatdal Fm Ikermiut Fm Mainly marine mudstones, locally sandy/silty Mainly marine or deltaic sandy/silty deposits, locally mudstones Potential and known source rocks Volcanics TD in basement Unconformity Mainly continental deposits Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 15 16 Baffin Margin Offshore rocks of western Baffin Bay are known only from shallow cored boreholes drilled on the Baffin Shelf. According to MacLean et al. (2014), Cretaceous rocks of Aptian–Albian to Cenomanian age occur on the south-eastern Baffin Shelf, and of Coniacian to Campanian age on the north-eastern Baffin Shelf. The former equate to the Bjarni Formation, the latter to the Markland Formation. However, according to MacLean et al. (2014), Danian to Selandian rocks, of similar age and lithology to the Eureka Sound Group (a unit gener- ally used for strata farther north and west, see below) have been recovered from cores off Cumberland Sound (MacLean & Williams 1983; MacLean et al. 1986). Onshore West Greenland Mesozoic–Cenozoic rocks in West Greenland occur in the Nussuaq Basin, adjacent to Baffin Bay, where rocks of the Nuussuaq Group outcrop on several peninsulas and islands. Dam et al. (2009) provided a synthesis of this group, in which they formalised the lithological units proposed by previous researchers, especially Hen - derson et al. (1976), and proposed some new units. Stra tigraphic control in Dam et al. (2009) was based on palynological studies, including those of Koppelhus & Pedersen (1993), Nøhr-Hansen (1993b, 1996), Nøhr- Hansen & Dam (1997), Dam et al. (1998b, c), Lans - torp (1999), Kennedy et al. (1999), Nøhr-Hansen & Heilmann-Clausen (2000), Nøhr-Hansen et al. (2002), Sønderholm et al. (2003a, b). Additional data were presented by Pedersen et al. (2013) and Pedersen & Nøhr-Hansen (2014). In the Nuussuaq Basin, the oldest known rift to early post-rift sediments are Aptian? to Albian in age and consist of fan-delta, fluvio-deltaic and shallow marine deposits of the Kome Formation, which onlap Pre cam - brian basement on Disko and Nuussuaq (Hen derson et al. 1976; Dam et al. 2009; Pedersen & Nøhr-Hansen 2014). The succeeding Slibestensfjeldet For mation com - prises lacustrine or lagoonal deposits, with palynofloras dominated by non-marine miospores and rare, brack- ish-water dinocysts of Albian, possibly mid dle Albian, age (Pedersen & Nøhr-Hansen 2014). Both the Sli be - stensfjeldet and the Kome Formations are un con form - ably overlain by Albian to upper Santonian post-rift, fluvial and wave-dominated deltaic to fully marine deposits of the Atane Formation (Pedersen & Pulver - taft 1992; Nøhr-Hansen et al. 2002; Dam et al. 2009; Pedersen & Nøhr-Hansen 2014). To the west of a major fault, sediments of the Atane Formation are replaced by deep-water submarine-fan deposits as - signed to the Itilli Formation. Turonian – lower Maa - strichtian slope deposits are also described from Svartenhuk Halvø (Dam et al. 1998b). Lithological and age similarities suggest that the Kome, Slibestensfjeldet and Bjarni Formations are coeval, the unconformity beneath the Atane Formation being equivalent to the Avalon Unconformity. A major angular unconformity separates the deltaic deposits of the Qilakitsoq Member (the upper part of the Atane Formation) from the marine gravity-flow deposits of the lower–middle Cam - panian Aaffarsuaq Member of the Itilli Formation in Nuussuaq (Dam et al. 2000, 2009). Rifting continued through the Maastrichtian and into the Danian in the Nuussuaq Basin, with at least three tectonic phases associated with valley and sub - marine canyon incision (Dam et al. 1998a; Dam et al. 2009). The fill of the incised valleys represents three formations that are overlain by deep-water marine mudstones and volcanic tuffs (Dam et al. 2009). Al - though occurrences of Neogene rocks in West Green - land are sparse, a thin succession of Neogene sediments overlies the Eocene Hareøen Formation (Fig. 3; Hald 1976; Christiansen et al. 1999). An insightful study of the rocks from onshore West Greenland was undertaken by Larsen (2006) and Lar - sen et al. (2009), who mapped and dated the dyke swarms in that region. These authors recognised the following phases of intrusion, which can be related to significant stages in the development of the Labrador Sea and the Davis Strait: early extension (220–150 Ma, Late Triassic to Late Jurassic) increased extension (around 150 Ma, Kimmerid gian) regional rifting and dyke intrusion (140–133 Ma, Berriasian to Valanginian/Hauterivian) subsidence and sedimentation (130–120 Ma, Barre - mian and Aptian) faulting, sedimentation and magmatism (around 120– 100 Ma, Aptian–Albian) Late Cretaceous subsidence, sedimentation and fault- ing (100–65 Ma) Palaeogene rifting and magmatism (about 62 Ma). The last phase gave rise to the West Greenland Palaeogene Volcanic Province (Fig. 2), with a volcanic • • • • • • • Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 16 17 succession up to 3 km thick (Storey et al. 1998; Larsen et al. 2016), occurring mainly onshore but extending offshore. Onshore, volcanism associated with this pro - vince commenced around 61–62 Ma (Chron 27n; latest Danian to early Selandian; Nøhr-Hansen et al. 2002), with most of the basalts being extruded in less than a million years (Storey et al. 1998; Larsen et al. 2009, 2016), followed by younger Paleo cene volcanism in the Nuussuaq Basin. Other volcanic basalts are con - sidered to be of Ypresian, late middle Eocene and middle Oli gocene age. According to Larsen et al. (2009), the youngest volcanic rocks in West Greenland are 28 Ma (around the Rupelian–Chattian boundary; Fig. 3). Rol - le (1985) noted that the Jurassic and Lower Cretaceous alkaline intrusions in southern Greenland are similar pe trographically to the intrusives of north-western New - foundland, which he believed were associated with the formation of the Labrador Margin basins. North-eastern Canada The oldest onshore Cretaceous rocks on the Canadian margin adjacent to the Labrador–Baffin Seaway are the Ford Bight volcanics, which crop out along the La b - rador coast. These rocks were described by King & McMillan (1975) and dated by Balkwill et al. (1990) as 129 ± 6 Ma (Valanginian – earliest Aptian on the Gradstein et al. 2012 timescale) and 145 ± 6 Ma (Ti - thonian – earliest Valanginian). These ages are broadly compatible with those given for the Alexis Formation (122 and 139 Ma). There are no known rocks onshore Labrador that equate with the Bjarni Formation, but such rocks do occur in eastern and north-eastern Baffin Island and on Bylot Island. From the Cape Dyer area of Baffin Island, Burden & Langille (1990) described sandstones, silt- stones and coal beds that contain palynomorphs indica- tive of an Aptian to early Cenomanian age. Outcrops of Cretaceous and lower Cenozoic rocks occur in the Eclipse Trough on Bylot Island and north- eastern Baffin Island. These deposits, which show simi- larities with rocks on the Labrador Margin (Figs 2, 3), were described by Miall et al. (1980), McWhae (1981) and Miall (1986), who used lithostratigraphic unit names with type sections in the Arctic Islands to the north-west. The units are, from oldest to youngest, the Hassel For mation (equivalent to the Bjarni Formation), the Kanguk Formation (equivalent in part to the Markland Formation) and the Eureka Sound Group (Fig. 3). The Eureka Sound Group was named by Troelsen (1950), reduced to formation status by Tozer (1963), and raised back up to group status indepen- dently by Miall (1986) and Ricketts (1986). Rather than using the Eureka Sound Formation/Group, Sparkes (1989) and Water field (1989) proposed an informal lithostratigraphic breakdown for equivalent rocks on Bylot Island. Accor ding to these authors, the Kanguk Formation is unconformably overlain by the informal Sermilik and Bylot Island formations, which are in part coeval. The top of the Bylot Island formation is unconformably overlain by the Pond Inlet formation, above which are the informal Navy Board and Aktineq formations (Fig. 3). This scheme was followed by Harrison et al. (1999) and Har rison et al. (2011). McWhae (1981) considered the unconformity sepa- rating the Hassel Formation from the overlying Kanguk Formation to be the Avalon Unconformity and he named the hiatus between the Kanguk and Eureka Sound Group (as Eureka Sound Formation) as the Bylot Unconformity. Although not using the name Bylot Unconformity, Miall (1986) also recognised an unnamed unconformity between the Kanguk For - mation and the Eureka Sound Group. Both of these authors indicated an early Paleocene age for this uncon- formity. However, Sparkes (1989) and Waterfield (1989) dated the Bylot Unconformity as Maastrichtian. Similarly, Harrison et al. (2011) gave a Maastrichtian to Danian age to the section extending from the Sermilliq Formation to the Aqtineq Formation (i.e. the former Eureka Sound Formation/Group), with an unconfor- mity beneath these. As discussed further below, the number of unconfor- mities and/or hiatuses is probably greater than the five specified by McWhae et al. (1980). For example, our data seem to indicate two hiatuses associated with the Maastrichtian–Paleocene interval, one at the base of the Cenozoic and one in the Selandian. On Baffin Island, Andrews et al. (1972) recorded marginal marine to lacustrine Palaeogene sediments from the north-central region, and Clarke & Upton (1971) found terrestrial sediments north of Cape Dyer. Burden & Langille (1990) described fluvial and debris- flow deposits of Danian age on the Quqaluit and Pad - loping islands (Figs 1, 2). Presumably these rocks and the overlying Cape Dyer Basalt represent the late rifting phase immediately before the opening of Baffin Bay. Pedersen et al. (2002) considered the Cape Dyer Basalt most likely to be time equivivalent to the lower part of the Vaigat Formation in the Nuussuaq Basin (Fig. 3). Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 17 18 The results presented in this bulletin reflect data from analyses of offshore wells from both margins of the La b - rador–Baffin Seaway; detailed taxonomic data are pre - sented in the companion bulletin (Fensome et al. 2016). The Labrador Margin wells are from both the Hopedale Basin (Bjarni O-82, North Leif I-05, Ogmund E-72, Roberval K-92, Snorri J-90 and South Labrador N-79) and the Saglek Basin (Gilbert F-53, Gjoa G-37, Hekja O-71, Karlsefni A-13, Ralegh N-18, Rut H-11 and Skolp E-07). The wells on the West Greenland Margin are: Hellefisk-1, Ikermiut-1, Kangâmiut-1, Nukik-1, Nu - kik-2 and Qulleq-1. Also incorporated are some results from onshore West Greenland cored boreholes and sur - face sections, and from some shallow cored boreholes from western Baffin Bay. An event-stratigraphic approach is adopted as we consider this to provide greater detail and precision than an approach based on zonations. An event-strati- graphic approach also better facilitates incorporation of events from multiple disciplines; the events used here are exclusively derived from palynology. Events can be originations of species, called first occurrences (FOs), extinctions, called last occurrences (LOs), or occasion- ally peak occurrences, or acmes, of species. Although some stratigraphic control was obtained from analysis of conventional cores from several La b - rador Margin wells and from some side-wall cores, the availability of and recovery from such samples were limited. It has been necessary therefore to rely mostly on ditch-cuttings samples, and hence on LOs for most of the events, as such samples usually contain down- section contamination (cavings). Reworked specimens also occur in many samples, being most frequent in what we consider to be Pliocene–Pleistocene sections. Piasecki (2003) noted that reworked species outnum- bered in-situ species in his late Pliocene interval in the Qulleq-1 well. Contamination from drilling mud was also a minor concern; for example, the presence of the dinocyst Ovoidinium verrucosum in most of the ditch- cuttings samples in Hellefisk-1 and Nukik-2 is inter- preted to have resulted from contamination from Cen o manian bentonite added during drilling. Samples processed at GSCA (Bjarni O-82, Gilbert F-53, Karlsefni A-13, Roberval K-92, Rut H-11, Snorri J-90, South Labrador N-79) followed the procedure outlined in Barss & Williams (1973) and carried out from 1971 to 2007 (Fig. 4). The first step after crushing the sample, if necessary, was the addition of 10% hydrocholoric acid to remove carbonates. After decant- ing the acid, the residue was washed and placed in hydrofluoric acid to remove the silicates. When the sample appeared to be broken down, the hydrofluoric acid was decanted and the sample washed several times. To remove any remaining fluorides, the sample was placed in concentrated hydrochloric acid, followed by washing. The fraction remaining was further concen- trated using a heavy liquid such as zinc bromide. This was followed by oxidation in concentrated nitric acid or Schulze solution, followed by careful washing to re - move the oxidising agents, and treatment with ammo- nium hydroxide. The final phase before making the slides was sieving, a technique that concentrates the dinocysts and larger miospores. All the slides were mounted in elvacite. Most residues were stained with Safranin red or Bismarck brown. Although oxidation, if done at all, was always carefully controlled, most samples were processed at a time when the detrimental Methodology Mudstone, sandstone, limestone Pre-acid preparation 10% HCl Decant Wash 3 times Concentrated HF Decant Wash 3 times Concentrated HCl Decant Wash 3 times Centrifuge Wash 3 times HN4OH Wash until clear Remove remaining minerals Stain Screen 20, 30, 38, 180 µm Stain/make slides Coal, peat ZnBr2 1.4 specific gravity Differential centrifuge/ screen Store cut for carbonisation studies Store residue Oxidise (HNO3 or Schulze solution) ZnBr2 2.0 specific gravity Remove coarse material Fig. 4. Flow chart showing the palynological processing method used at the Geological Survey of Canada (Atlantic). Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 18 19 selective effect of oxidation procedures on peridinioids, and especially protoperidinioids, was not fully appreci- ated. Hence the general scarcity of protoperidiniod cysts in our assemblages may be due to over-oxidation, although most samples stratigraphically predate times when protoperidinioids became common. Samples from Hellefisk-1, Ikermiut-1, Kangâmiut- 1, Nukik-1, Nukik-2, Qulleq-1, North Leif I-05, Og - mund E-72, Skolp E-07, Hekja O-71, Ralegh N-18 and Gjoa G-37 were processed at the Geological Survey of Greenland (GGU, now GEUS). Palynomorphs were extracted from 10–20 g of sediment from each sample by modified standard preparation techniques that in - cluded treatment with hydrochloric (HCl) and hydro- fluoric (HF) acids, sieving using a 20 μm nylon mesh and oxidation (3–10 minutes) with concentrated nitric acid (HNO3), often followed by washing with a weak potassium hydroxide solution (KOH). Finally, paly- nomorphs were separated from coal particles and woody material in most samples using the separation method described by Hansen & Gudmundsson (1978) or by swirling. After each of the steps mentioned above, the organic residues were mounted in a solid medium (Eukitt®) or in glycerine gel. The palynological slides were studied with transmitted light using a Leitz Dialux 22 microscope (no. 512 742/057691). Dinocysts, acri - tarchs and selected stratigraphically important spore and pollen (miospores) species were recorded from the sieved, oxidised or gravity-separated slides. Approxi - mately 100 specimens were counted whenever possible. Using transmitted light microscopy, qualitative and quantitative analyses were undertaken of the palyno - morphs present in each well (see appendices 2, 3); the stratigraphically important events are plotted on sum - mary charts (Figs 5, 6, in pocket). The LOs of species plotted in Figs 5 and 6 were generally based on occur- rences in several wells, thus allowing correlation be - tween well sections. However, few of the taxa recorded on the events plot are present in all the wells, due in part to the variable duration of the hiatuses in the individual wells. A detailed chart has been generated for each well showing LOs and other key events, such as peak occur- rencies and acmes (Appendix 3). Although broad con - sistency has been sought, the information included in these charts is variable to some degree, dependent on the source of the data. Those done by HN-H (Helle - fisk-1, Ikermiut-1, Kangâmiut-1, Nukik-1, Nukik-2, Qulleq-1, North Leif I-05, Ogmund E-72, Skolp E-07, Hekja O-71, Ralegh N-18 and Gjoa G-37) present a zonation and events (predominantly LOs) that were published in Sønderholm et al. (2003b), Nøhr-Hansen et al. (2000) and Nøhr-Hansen (2003, 2004a, b) for the Aptian‒Albian to Priabonian of the West Greenland and Labrador Margins of the Labrador Sea. Some of HN-H’s plots in the present paper also show dinocyst species richness and Azolla abundances. Plots generated by GLW and RAF (Bjarni O-82, Gilbert F-53, Karl - sefni A-13, Roberval K-92, Rut H-11, Snorri J-90 and South Labrador N-79) show events and ages only; a zonation was not developed. In total, 187 bioevents are identified for the Labra - dor–Baffin Seaway; 169 of these represent the youngest or last occurrence (LO) of a taxon, the others represent peak occurrences or abundances. Some events are coe - val, so the 187 bioevents define 106 bioevent horizons. Collectively, the bioevents are based on 177 taxa. Also incorporated are 22 events (13 event horizons) estab- lished by Piasecki (2003) for the Neogene of off shore West Greenland and 50 events (44 event horizons) established by Pedersen & Nøhr-Hansen (2014) for Albian to Paleocene strata of the Nuussuaq Basin, West Greenland (Figs 5, 6 in pocket). Most of the species are dinocysts but several are pollen and spores, and we also include a fungal spore peak and two Azolla peaks. To promote understanding, communication and future consistent recognition of taxa encountered in this study, a companion bulletin presents the systematic taxonomy (Fensome et al. 2016), describing and illustrating most of the species referenced in Figs 5 and 6 and specifying location and repository information for the material used in this study. The timescale of Gradstein et al. (2012) is adopted. Detailed analyses and palaeoenvironmental curves for wells analysed in this study are presented in Appendices 2 and 3; those dinocyst taxa whose occurrences are considered to have significance as palaeoenvironmental indicators are listed under the appropriate palaeoenvi- ronment in Table 1 (see p. 37). Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 19 20 Palaeontological evidence used to interpret the evolu- tion of the Labrador–Baffin Seaway region has been derived primarily from the study of Cretaceous–Neo - gene microfossil (including palynological) assemblages recovered from offshore wells on the Labrador Margin and on the West Greenland Margin. Papers, reports and two theses on the palynomorphs from Labrador Margin and Davis Strait wells, all drilled in the 1970s and 1980s, have been produced by Williams (1975), Gradstein & Williams (1976), Barss et al. (1979), Ioakim (1979), Gradstein & Williams (1981), Wil liams (1986), Bujak Davies Group (1987), Bell (1989), Wil - liams et al. (1990), Nøhr-Hansen (2004a, b), Nøhr-Han - sen (in Sønderholm et al. 2003b), Williams (2007a–f), Ainsworth et al. (2014) and Fensome (2015). Fora - miniferal studies were undertaken by Grad stein & Wil - liams (1976), Gradstein & Srivastava (1980), Grad stein & Agterberg (1982), Gradstein et al. (1994) and Ains - worth et al. (2014). Williams (1986) is the only author to have presented a zonation for Labrador–Baffin Seaway wells based on Cenozoic spores and pollen. She analysed six wells: Kangâmiut-1, Hekja O-71, Karlsefni A-13, Herjolf M- 92, Roberval K-92 and Cartier D-70. Based on these analyses, she recognised eight provisional spore and pollen zones of the following ages: early to middle Paleo - cene, middle to late Paleocene, early to middle Eocene, middle to late Eocene, latest Eocene/earliest Oligocene, early Oligocene, early to middle Miocene, and middle to late Miocene. The middle and upper Oligocene was inferred to be absent in the wells. Ioakim (1979) analysed the dinocysts from two Hopedale Basin wells, Bjarni H-81 and Freydis B-87. She erected 11 zones and three subzones, which collec- tively spanned the Maastrichtian–Priabonian. Most of the zones were named after peridiniaceans, especially wetzelielloideans. Ainsworth et al. (2014) undertook a detailed litho - stratigraphic and biostratigraphic study of six Labrador Margin wells: Herjolf M-92, North Bjarni F-06, Og - mund E-72, Pothurst P-19, Roberval K-92 and Snorri J-90, plus Hare Bay E-21 from offshore north-eastern Newfoundland. They based their biostratigraphy on fora minifera and palynomorphs, with the latter being primarily dinocysts, and their palaeoenvironmental in - terpretations exclusively on fluctuations in the for - aminiferal assemblages. Among their suggestions was a division of the Markland Formation into a lower mem - ber of Coniacian–Maastrichtian age and an upper mem - ber of Selandian age, with the boundary between the two units equivalent to a base-Cenozoic unconformity. According to Ainsworth et al. (2014), the upper part of the Markland Formation was deposited in a predom- inately deep-water setting – a very different interpreta- tion from that of Balkwill & McMillan (1990), who postulated a marginal marine to middle shelf environ- ment. The re-interpretation by Ainsworth et al. (2014) was based on present-day knowledge of deep-water agglutinated foraminifera. Ainsworth et al. (2014) in - cluded the Gudrid member as part of the Cartwright Formation (instead of being parts of the Markland, Cartwright and Kenamu For mations as used here), and considered it to be Thane tian in age and deposited in a bathyal environment. Based on their interpretation of the Saglek Basin’s Pothurst P-19 well, Ainsworth et al. (2014) regarded much of the ‘lower’ Mokami For ma - tion (Chattian to Miocene) and all of the ‘upper’ Mio - cene to be absent. This is at variance with other studies, which indicate that Miocene sediments occur in this well. The interpretation of Ainsworth et al. (2014) sup - ports the observations of Knutsen et al. (2012), how - ever, who noted that off West Greenland during the Miocene there was uplift and erosion, which they relat- ed to hot-spot migration. A recent study of Pothurst P- 19 (G.L. Wil liams, unpublished data) demonstrated that most of the lower and all of the middle Miocene are missing, but some upper Miocene is present. Palaeogene nannofossil biostratigraphy was de - scribed for the Gilbert F-53 and Skolp E-07 wells by Crux & Gard (2004). In Gilbert F-53, they recorded a thick Palaeogene sequence succeeded by an indetermi- nate Cenozoic succession. Skolp E-07 contained a sec - tion with mixed nannofossils of Cretaceous and Ceno zoic age overlain by Cenozoic strata. Crux & Gard (2004) interpreted the lower section to be probably Cenozoic with reworked Cretaceous nannofossils. Nan no fossil re - covery was generally disappointing. On the West Greenland Margin, Rolle (1985) published the stratigraphy of the five wells drilled in 1976 and 1977 (Hellefisk-1, Ikermiut-1, Kangâmiut-1, Nukik-1, Nukik-2; Figs 1, 2), with age control based on palynology. Renewed interest in exploration of the West Greenland Margin in recent years has motivated new and detailed studies of the Cretaceous to Neogene Previous palaeontological studies Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 20 21 palynology (e.g. Nøhr-Hansen 1996, 1997a–c, 2003; Nøhr-Hansen & Dam 1997; Dam et al. 1998b, 2009; Nøhr-Hansen et al. 2000, 2002; Sønderholm et al. 2003b; Piasecki 2003; Pedersen & Nøhr-Hansen 2014). Other microfossil groups utilised include nannofossils (Nøhr-Hansen et al. 2000; Sheldon 2003) in the Palaeo - gene–Neogene and foraminifera (Nøhr-Hansen et al. 2000; Rasmussen et al. 2003; Rasmussen & Sheldon 2003), plus ostracods, radiolarians and diatoms (Ras - mussen et al. 2003). Further information comes from numerous Creta - ceous–Cenozoic outcrop sections from the Nuussuaq Basin in West Greenland, a few onshore sections in Labrador and on Baffin and Bylot Islands, and from ODP Leg 105, hole 645 from offshore Baffin Island (Fig. 2; Kaminski et al. 1989a, b). Invariably, the bio - stratigraphy is based on microfossils including paly- nomorphs. Results from analyses of the cuttings provided the basis for the plots of LOs of taxa (Figs 5, 6, in pocket). Peak occurrences or abundances are also included in the Palaeogene. As noted previously, results are based on three areas: the Hopedale Basin on the Labrador Mar - gin (Bjarni O-82, North Leif I-05, Ogmund E-72, Ro - berval K-92, Snorri J-90 and South Labrador N-79), and the Saglek Basin, partly on the Labrador Margin (Gilbert F-53, Karlsefni A-13, Rut H-11 and Skolp E- 07) and partly off south-eastern Baffin Island (Gjoa G- 37, Hekja O-71, Ralegh N-18). On the West Green land Margin, the wells are: Hellefisk-1, Ikermiut- 1, Kangâ miut-1, Nukik-1, Nukik-2, and Qulleq-1. Figures 5 and 6 represent composite compilations that involve the merging of data from both the Canadian and Green land margins. One unexpected difficulty has been the identification of taxa common to both mar - gins of the seaway. This may be because some taxa are endemic to one margin or even one area, and perhaps also because of the different latitudes of the overall loca- tion of wells on the two sides, the Greenland wells being farther north. However, there was enough over- lap to provide a detailed event-stratigraphic framework (Figs 5, 6, in pocket), especially with the incorporation of information on known stratigraphic ranges of taxa in European sections (Powell 1992; Bujak 1994; Williams et al. 1999, 2004) and from other wells and cored bore- holes from offshore eastern Canada and West Green - land (Williams 1975; Williams & Brideaux 1975; Williams & Bujak 1977; Barss et al. 1979; Williams et al. 1990; Sønderholm et al. 2003b; Nøhr-Hansen 2004a, b; Fen some & Williams 2005; Fensome et al. 2008, 2009). Lower Cretaceous The oldest Mesozoic rocks identified here in the La - brador–Baffin Seaway are Aptian (see below), and these are restricted to the Labrador Margin. However, H. Nøhr- Hansen has also observed reworked Late Jurassic – Early Cretaceous taxa such as Lithodinia sp., Nelchinopsis kostro - miensis, Sirmiodinium grossii, and forms similar to Gony - aulacysta pectinigera/fastigiata from seabed samples col- lected by GEUS (Dalhoff et al. 2006). Piasecki (2003) also reported Late Jurassic dinocysts in dredge samples from the West Greenland Margin. Aptian Gradstein & Williams (1976), in their biostratigraphic study of Labrador Margin wells, defined a Cerebro polle n - ites mesozoicus assemblage of Barremian–Aptian age. In this study, it has not been possible to confirm the pres- ence of Barremian strata, but an Aptian age is demon- strated on the Labrador Margin by the presence of the dinocyst Tenua hystrix, which is the taxonomic senior synonym of Cer bia tabulata (see Fensome et al. 2016). Tenua hystrix, misidentified as Cyclonepheliium atta da - li cum, was the index species for an early Aptian zone in the Scotian Basin (Williams 1975). Duxbury (2001) placed the LO of Cerbia tabulata at the top of the Biostratigraphic results Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 21 22 Aptian, which is at 113 Ma on the Gradstein et al. (2012) timescale. Other studies (e.g. Williams 2003b) have confirmed the LO of Cerbia tabulata to be a consistent marker for the top of the Aptian. Also in the Aptian of the Roberval K-92 and South Labrador N-79 wells is a form that we identify as Pseu doceratium sp. Wells with Aptian rocks include Bjarni O-82 (Appen - dix 3.3), Roberval K-92 (Appendix 3.2) and South Labrador N-79 (Appendix 3.4; Figs 1, 7). Palyno - morphs found in the Aptian rocks in our study include the miospores Callialasporites dampieri, Callialasporites obrutus, Cerebropollenites mesozoicus, Par vi saccites amplus, Appendicisporites jansonii, Cicatrico sis porites australiensis and Klukisporites areolatus. Ikermiut-1 Qulleq-1 Offshore West Greeenland Onshore West Greeenland Offshore eastern Canada Labrador Margin, Saglek Basin Gilbert F-53 GRO#3 well Nuussuaq Umiivik-1, Svartenhuk Halvø & North Nuussuaq, surface section Skolp E-07Bjarni O-82 South Labrador N-79 Snorri J-90 Ogmund E-72 Offshore eastern Canada, Labrador Margin, Hopedale Basin 110 115 120 125 105 70 75 80 85 90 95 100 Ma North Leif I-05 Roberval K-92 110 115 120 125 105 70 75 80 85 90 95 100 L at e C re ta ce ou s Ea rl y C re ta ce ou s EpochMa Maastrichtian Campanian Santonian Coniacian Turonian Cenomanian Albian Aptian Age Fig. 7. Cretaceous ages (highlighted in green) identified from palynomorph assemblages in wells from the Hopedale Basin of the Labrador Margin (North Leif I-05, Roberval K-92, Bjarni O-82, South Labrador N-79, Snorri J-90 and Ogmund E-72), the Saglek Basin of the Labrador Margin and Davis Strait (Skolp E-07 and Gilbert T-53), offshore West Greenland (Qulleq-1 and Ikermiut-1), and a well (GRO #3, Nuussuaq), a borehole (Umiivik-1) and two surface sections (Svartenhuk Halvø and north Nuussuaq) from onshore West Greenland. Ages not coloured have not been identified. The timescale (Ma) is from Gradstein et al. (2012). Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 22 23 Albian Albian assemblages in Labrador Margin wells strongly reflect marginal marine to innermost neritic palaeoen- vironments. Dinocyst taxa with Albian LOs include Nyktericysta davisii, Nyktericysta dictyphora, Nyktericysta tripenta, Oligosphaeridium albertense, Vesperopsis longi- cornis and Subtilisphaera perlucida. Nyktericysta davisii was described from middle to upper Albian brackish- water deposits in the Western Interior Seaway of the USA by Bint (1986). In offshore eastern Canada, it has a consistent LO in the Albian and other records of its occurrence in the late Albian are from onshore East and West Greenland and Arctic Canada (Nøhr-Hansen 1992, 1993a, 2008; MacRae 1996; Nøhr-Hansen & McIntyre 1998) and the Scotian Mar gin (Fensome et al. 2008). However, a recent study by Pedersen & Nøhr-Hansen (2014) indicated that large forms of Nyktericysta davisii and Nyktericysta arachnion occur in the early Cenomanian of onshore Nuussuaq Basin based on co-occurrence with the pollen species Rugubi - ve siculites multisaccus, which is indicative of an early Cenomanian age according to Singh (1983). Nykteri - cysta dictyphora is also characteristic of brackish-water deposits in the Aptian–Albian of China (Mao Shaozhi et al. 1999). Senoniasphaera microreticulata oc curs in the Albian of North Leif I-05 (Nøhr-Hansen 2004b). Miospores dominate most Albian assemblages on the Labrador Margin. Bujak Davies Group (1987) defined a Parvisaccites amplus Zone which they considered early Albian. Conventional cores from North Leif I-05 con - tain Parvisaccites radiatus with Rugubivesiculites rugosus, Rugubivesiculites multiplex, Rugubivesiculites reductus and Rugubivesiculites convolutus, and conventional cores from Bjarni O-82 contain Rugubivesiculites rugosus. Wil liams (1975) erected a Rugubivesiculites rugosus As - semblage Subzone of late Albian age for the Scotian Shelf and Grand Banks. Singh (1983) placed the LO of Rugubivesiculites rugosus in the Cenomanian and Nøhr- Hansen (in Sønderholm et al. 2003b) recognised a ?late Albian to ?Cenomanian Rugubivesiculites spp. inter val, based on a study of Skolp E-07 and Ogmund E-72. The cored interval in North Leif I-05 and Bjarni O-82 is thus no older than late Albian. We have identified Albian sediments in Bjarni O-82 (Appendix 3.3), North Leif I-05 (Appendix 3.1), Ogmund E-72 (Appendix 3.6), and Skolp E-02 (Ap - pendix 3.7; Figs 1, 7), and onshore in the Nuussuaq Basin. Several taxa other than those plotted on the events chart (Fig. 5, in pocket) have provided support- ing data for age determinations in the Aptian–Albian, including Pilosisporites verus, Cicatricosisporites reticica- tricosus, Contignisporites glebulentus and Alisporites gran- dis, all with LOs in the Albian (Williams 2007a). Upper Cretaceous Cenomanian This study indicates that the Cenomanian is present in only four wells on the Canadian Margin. However, there are some characteristic markers for this stage, including the dinocyst species Kiokansium williamsii described by Singh (1983) from the Albian and Ceno - manian of Alberta: in this study, it was found in North Leif I-05 and Bjarni O-82. The species was first record- ed as Cleistosphaeridium polypes subsp. A by Williams (1975), who noted that its LO was in the Ceno manian. Other characteristic dinocyst taxa of the Cenomanian are Oligosphaeridium totum and Odonto chitina ancala. Williams et al. (1999) placed the LO of Oligo sphae r - idium totum at 96.2 Ma, in the middle Ce nomanian whereas Fensome et al. (2008) indicated its LO to be earliest Cenomanian. An expecially distinctive morpho- type with an LO in the Cenomanian is the pol len Afropollis (Fensome et al. 2009); Cicatri cos i sporites mi - nu ta estriatus has a Cenomanian LO in Og mund E-72. All the wells with Cenomanian strata – North Leif I-05 (Appendix 3.1), Ogmund E-72 (Ap pendix 3.6) and Skolp E-07 (Appendix 3.7) – are on the Labrador Mar - gin (Figs 1, 7). The upper Cenomanian in the Nuus - suaq Basin is characterised by the FOs of Tri thy ro d i nium suspectum, Isabelidinium magnum and Cauve rid i nium membraniphorum (Pedersen & Nøhr-Hansen 2014; Fig. 5, in pocket). Turonian–Santonian The Turonian appears to be absent from all offshore wells, except possibly lower Turonian in North Leif I- 05. Because of uncertainty we have tended to define a Turonian–Coniacian, rather than a Turonian, interval for the Labrador wells. Species of Rugubivesi culites appear to have their LOs in the Turonian, but may range higher. The lower Turonian in the Nuus suaq Basin is characterised by the FO of Hetero sphaeri dium difficile (Nøhr-Hansen 1997a; Pedersen & Nøhr- Hansen 2014). In the Umiivik-1 borehole on Svarten - huk Halvø (Fig. 2), Dam et al. (1998b) recognised an upper Turonian interval IV and an uppermost Turo - Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 23 24 nian to lower Coniacian interval III; interval IV is charac terised by a Heterosphaeridium difficile acme; He - tero sphaeridium difficile and Circulodinium distinctum are common in the upper part of interval III and Raphi - dodinium fucatum has its acme in the upper part of Interval III. Interval III correlates in part with the early Coniacian Spinidinium echinoideum interval described by Nøhr-Hansen (1996). Bujak Davies Group (1987) recognised a Heterosphaeridium difficile Zone, which they considered to be early Campanian. The top of Nøhr-Hansen’s (1996) Coniacian – early Santonian Heterosphaeridium difficile interval was defined by the LO of Heterosphaeridium difficile at the top of the early Santonian, citing as justification Costa & Davey (1992). Williams et al. (2004) plotted the FO of Hetero sphaeri - dium difficile at about the early–middle Turonian boun - dary and its LO in the late Coniacian in northern mid- latitudes. In a study of some shallow cored boreholes from the Baffin Margin, MacLean et al. (2014) consid- ered Heterosphaeridium difficile to have a range of late Coniacian to early Santonian, but noted that it was oc - casionally found as high as the early Campanian. Nøhr- Hansen (2012) and Radmacher et al. (2014) noted that the species occurred in Turonian–Coniacian sediments in the Kangerlussuaq Basin, southern East Greenland and in the south-western Barents Sea. In this study, we have placed the LO of Heterosphaeridium difficile at the top of the early Santonian. Support for this is provided by the LO of Odontochitina porifera, which Stover et al. (1996) placed in the early San tonian, although other authors (Costa & Davey 1992; Williams et al. 2004) have extended the range of the species into the Cam - panian. Neither Heterosphaeridium difficile nor Odon to - chi tina porifera are found in the only two West Green land wells with Cre taceous rocks, Qulleq-1 (Ap pendix 3.14), and Iker miut-1 (Appendix 3.18), indicating that the oldest sediments in these wells are younger than early Santonian. On the Labrador Margin, Bjarni O-82 (Ap - pendix 3.3) and South Labrador N-79 (Appendix 3.4) appear to have Coniacian sediments (Figs 1, 7). Campanian The LO of Spongodinium (originally Scriniodinium) obscurum is taken here to mark the Santonian–Cam - panian boundary, a somewhat arbitrary decision. Spon - go dinium obscurum was erected by Manum & Cookson (1964), who considered the sample from Graham Is - land, Arctic Canada, from which the species was first re - covered, to be early Late Cretaceous in age. This was based on the occurrence of the species in what these authors considered to be the Hassel Formation, of late Albian to Early Cenomanian age. However, Felix & Burbridge (1976) demonstrated that the sample was from the upper Cenomanian – lower Campanian Kan - guk Formation, and specifically from the upper Kan guk Formation. This reassignment would indicate that the age of the Graham Island sample is Santonian to early Campanian, and that the LO of Spongodinium obscu- rum is within this time interval. The base of the lower to middle Campanian Aquilla pollenites interval de - cribed by Nøhr-Hansen (1996) from the Nuussuaq Basin is defined by the FO of Aquillapollenites species. In the Labrador Margin wells, the following dinocyst species have their LOs at the Campanian–Maastrichtian boundary: Odontochitina co stata, Trichodinium castanea and Xenascus ceratioides. Stover et al. (1996) considered the LO of Odontochitina costata to equate with the Campanian–Maastrichtian boundary but extended the LO of Odontochitina operculata into the earliest Maa - strichtian. These authors also extended the LO of Xe - nas cus ceratioides to the top of the early Maastrichtian, but placed the LO of Tri chodinium castanea just above the base of the late Campanian. Williams et al. (2004) gave the LO of Xe nascus ceratioides as just above the Campanian–Maa strichtian boundary in northern mid- latitudes. Trithyrodinium suspectum and Raphidodinium fuca- tum have LOs within the later Campanian. This range conforms with that in Williams et al. (2004), who placed the LOs of both species in the late Campanian, but considered Raphidodinium fucatum to be the young - er. Nøhr-Hansen (in Sønderholm et al. 2003b) recog- nised an Odontochitina operculata interval, which was regarded as being of late Campanian age. One of the characteristic species was Heterosphaeridium bellii (as Heterosphaeridium heteracanthum), which has its LO in the latest Campanian in the Labrador–Baffin Sea way. Heterosphaeridium bellii was described by Rad macher et al. (2014), who stated that it had a common occurrence in the late Campanian to early Maa strichtian. Rad - macher et al. (2014) defined the top of the early Cam - panian on the LO of Callaiosphaeridium asymmetricum, which accords well with our findings. Wells with Cam - panian sections are Roberval K-92 (Ap pendix 3.2), Bjarni O-82 (Appendix 3.3), Ogmund E-72 (Appendix 3.6), Skolp E-07 (Appendix 3.7) and Gilbert F-53 (Appendix 3.9) on the Labrador Margin and Qulleq-1 (Appendix 3.14) and Ikermiut-1 (Ap pendix 3.18) on the West Greenland Margin (Figs 1, 7). Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 24 25 Maastrichtian Palynomorph taxa with LOs in the Maastrichtian include the dinocyst Isabelidinium cretaceum. In a study of dinocysts from the Campanian–Paleocene of Sey - mour Island and adjacent islands in Antarctica, Askin (1988) defined a Zone 1 that was characterised by Isabelidinium cretaceum. She considered the zone to be of late Campanian age. Bowman et al. (2012), based on updated data from Seymour Island, cited the age to be questionable late Maastrichtian but recognised two younger Maastrichtian zones. Thus, the LO of Isabeli - dinium cretaceum can be considered as early late Maa - strichtian. The species is thus a key index species for determining whether part of the upper Maa strichtian is missing in the Labrador–Baffin Seaway. One stratigraphically significant pollen species is Wodehousiea spinata, which occurs only in Skolp E-07 on the Labrador Margin: its LO approximately equates with the Maastrichtian–Danian boundary. A dinocyst species with a similar LO is Palynodinium grallator. Nøhr-Han - sen (1996) described lower Maastrichtian Cerodi nium die belii and upper Maastrichtian Wode houseia spinata intervals from the Nuussuaq Basin on the basis of the FOs of Cerodinium diebelii and Wode houseia spinata respec- tively, and Nøhr-Hansen (in Sønderholm et al. 2003b) defined a Palynodinium grallator interval for the upper- most Maastrichtian. This was characterised by the LOs of Palynodinium grallator and Wodehouseia spinata. Wil - liams et al. (2004) placed the FO of Palynodinium gralla- tor in northern mid-latitudes within the late Maa - strichtian and its LO in the earliest Danian. Palynodinium grallator has been re corded only from onshore West Greenland and from some Labrador Margin wells. Disphaerogena carposphaeropsis, a dinocyst species that occurs in the latest Maastrichtian of some Labrador Margin wells and in the Nuussuaq Basin (Nøhr- Hansen & Dam 1997; Dam et al. 1998c) also appears to be a good index species. Other such species in the Maastrichtian include Impagidinium victorianum, Isa - be li d i nium cretaceum, Laciniadinium arcticum and Spi - ni ferites scabrosus. Confirmation of the Maastrichtian age for the LO of Impagidinium victorianum comes from combined palynological and micropalaeontologi- cal analyses of South Labrador N-79 by Bujak Davies Group (1987). In an interval designated as Maa strich - tian based on foraminiferal data, they recognised an early Maastrichtian subzone for a taxon they identified as Impagidinium #LL. This taxon is probably conspecif- ic with the species identified here as Impagidinium victorianum and the species that Nøhr-Hansen (1996) identified from the upper Maastrichtian in the Nuus - suaq Basin as Impagidinium sp. cf. I dispertitum. Maa - strich tian strata occur in several wells on the Labrador Margin (Figs 1, 7), including North Leif I-05 (Ap - pendix 3.1), Roberval K-92 (Appendix 3.2), Bjarni O- 82 (Appendix 3.3), South Labrador N-79 (Appendix 3.4), Ogmund E-72 (Appendix 3.6), Skolp E-07 (Ap - pendix 3.7) and Gilbert F-53 (Appendix 3.9). Several taxa other than those plotted on the events chart (Fig. 5, in pocket) have provided supporting data for age determinations in the Late Cretaceous, includ- ing Senoniasphaera protrusa (LO Coniacian; Williams 2007b), Surculosphaeridium longifurcatum (LO Conia - cian), Microdinium ornatum (LO Coniacian), Xenascus sar jean tii (LO Coniacian), Chatangiella ditissima (LO early Campanian) and Stiphrosphaeridium dictyopho- rum (LO Maastrichtian). Triprojectate pollen are also potentially useful (see Braman 2013), but in the sec - tions studied their occurrence was too sporadic and often clearly reworked. Palaeogene Danian–Selandian Some major hiatuses occur in the Palaeogene sections on both margins of the Labrador–Baffin Seaway. The oldest is in the Danian, which seems to be missing or incomplete in all the wells, with the exception of South Labrador N-79. The presence of this stage is indicated by the occurrences of the dinocyst species Cerodinium diebelii, Phelodinium kozlowskii, Spongodinium delitiense, Senoniasphaera inornata, Tanyosphaeridium xan thi opy x - ides and Trithyrodinium evittii. According to Wil liams et al. (2004), Senoniasphaera inornata is restricted to the Da n ian, with its FO near the base and its LO at about 63 Ma in northern mid-latitudes. The same authors placed the LO of Spongodinium delitiense at about 64 Ma in North ern Hemisphere mid-latitudes. The lower Danian Tri thy ro dinium evittii Zone of Nøhr-Hansen et al. (2002) was recognised in North Leif I-05 (Nøhr-Hansen 2004b) and in Ogmund E-72 and Skolp E-07 (Nøhr-Hansen in Sønderholm et al. 2003b), indicating a late Danian – Thanetian hiatus in North Leif I-05 and Ogmund E-72 and a late Danian – Ypresian unconformity/hiatus in Skolp E-07. Williams (2007b) also concluded that in the South Labrador N-79 well, the LO of Trithyrodinium evittii is within the Danian. We place the LO of Cero - dinium diebelii at the Danian–Selandian boundary, based on the records from Bjarni O-82 (Williams 2007a), Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 25 26 South Labrador N-79 (Wil liams 2007b) and Snorri J-90 (Williams 2007c; Appendix 3.5). This is in slight conflict with Williams et al. (2004), who placed its LO at about 60 Ma in Northern Hemisphere mid-latitudes, within the early Selandian. Cerodinium diebelii has been record- ed from the Selandian in Nukik-2 (Nøhr-Hansen 2003; Ap pen dix 3.16), but this may represent reworking. With the exception of this probably reworked record in Nukik-2, none of the index species above occur in the West Greenland Margin wells, indicating that Da n - ian strata are generally absent. However, the presence of Cerodinium kangiliense and Senegalinium iterlaaense in the lower part of Nukik-2 may indicate a late Danian or early Selandian age (Fig. 8) according to Nøhr-Hansen & Heilmann-Clausen (2000). In the Labrador Margin and Davies Strait wells, the Danian is generally incom- plete or missing, with the exception of South Labrador N-79 (Appendix 3.4; Fig. 8). Nøhr-Hansen et al. (2002) erected five dinocyst zones, of which three are correlated to nannofossil zones, for the Danian sedimen tary succes- sion underlying the radiometrically dated Se landian ba - salts in the Nuussuaq Basin. Dinocyst species with an LO within or at the end of the Selandian include Palaeoperidinium pyrophorum, Spini - dinium echinoideum and Palaeocystodinium bulliforme. Nøhr-Hansen (2003) recognised a late Danian and three late Thanetian intervals on the West Greenland Margin. However, Nøhr-Hansen (2003) was following a two- fold division of the Paleocene in which Selandian is represented by the lower part of Thanetian (see Powell 1992 and Mudge & Bujak 1996). The three Thanetian intervals, from oldest to youngest are: the Palaeoperidi - nium pyrophorum interval (P4), correlating with latest Se - landian; the Areoligera interval (P5), correlating with lower Thanetian; and the Apectodinium spp. acme inter- val (P6), correlating with upper Thanetian (equivalences according to Mudge & Bujak 2001). Although not using the three-fold division of the Paleocene, Nøhr-Hansen (2003) recorded several of the species that appear to char- acterise a Selandian age. The top of his Palaeoperidinium pyrophorum (P4) interval is marked by the LOs of Palaeo - peridi nium pyrophorum and Palaeocystodinium bulli- forme. Wil liams et al. (2004) placed the LOs of Palaeo - cystodinium bulliforme and Palaeoperidinium pyropho- rum close to the Selandian–Thanetian boundary. Thus it seems reasonable to equate Nøhr-Hansen’s P4 inter- val with the Selandian. In the present study, the three- fold division is adopted (following Gradstein et al. 2012) and the Palaeoperid inium pyrophorum interval (P4) is referred to the late Selandian for the West Greenland wells (Figs 1, 8), viz. Nukik-2 (Appendix 3.16), Kangâmiut-1 (Appendix 3.17), Ikermiut-1 (Appendix 3.18) and Hellefisk-1 (Ap pendix 3.19). Nøhr-Hansen et al. (2002) defined the base of their late Danian Palaeocystodinium bulliforme Zone by the FO of Palaeocystodinium bulliforme; however they did not record the LO of Palaeocystodinium bulliforme. Po w - ell & Brinkhuis (in Gradstein et al. 2012) placed the LO of Palaeocystodinium bulliforme at the Se landian–Thane - tian boundary. Based on the co-occurrent LOs of Palaeo - peridinium pyrophrum and Palaeo cystodinium bulli forme, we place the latter LO at the Selandian–Thanetian boundary. Thanetian The Thanetian is characterised by maximum abun- dances of Areoligera gippingensis and Glaphyrocysta di - varicata (referred to here as the Areoligera gippingensis complex). The upper part of the Areoligera gippingensis interval (P5) of Nøhr-Hansen (2003) must equate in part with the Thanetian. High abundances of Areoligera gippingensis complex cysts in a number of the wells – such as Gilbert F-53, Gjoa G-37, Hekja O-71, Helle - fisk-1, Ikermiut-1, Kangâmiut-1, Karlsefni A-13, Nu - kik-1, Nukik-2 and Qulleq-1 – allow for correlation with the type Thanetian of southern England (Powell et al. 1996) and with the Skua E-41 (Williams 2003a) and Terra Nova K-18 wells (Williams 2003b) on the Grand Banks, offshore Newfoundland. One species with an LO at the Thanetian–Ypresian boundary is Cerodinium glabrum following immediately above the LO of Cero - dinium speciosum. Gradstein & Williams (1976) and Bujak Davies Group (1987) both defined a Cerodinium Facing page: Fig. 8. Cenozoic ages (highlighted in brown for the Palaeogene and yellow for the Neogene) identified from palynomorph assemblages in wells from the Hopedale Basin of the Labrador Margin (North Leif I-05, Roberval K-92, Bjarni O-82, South Labrador N-79, Snorri J-90 and Ogmund E-72), the Saglek Basin of the Labrador Margin and Davis Strait (Skolp E-07, Gilbert F-53, Rut H-11, Hekja O-71, Ralegh N-18 and Gjoa F-37), offshore West Greenland (Qulleq-1, Nukik-1, Nukik-2, Kangâmiut-1, Ikermiut- 1 and Hellefisk-1) and a well onshore West Greenland (GRO #3, Nuussuaq) and north Nuussuaq surface sections. Ages not coloured have not been identified. The timescale (Ma) is from Gradstein et al. (2012). TD: total depth. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 26 27 O ff sh o re e as te rn C an ad a, L ab ra d o r M ar gi n , H o p ed al e B as in H el le fis k- 1 T D i n A lb ia n T D i n P re ca m - b ri an b as em en t T D i n P re ca m - b ri an b as em en t T D i n b as em en t T D i n b as al t T D i n b as al t T D i n b as al t T D i n b as al t T D i n D an ia n T D i n b as em en t T D i n b as em en t T D in u p p er Sa n to n ia n T D i n A p ti an T D i n C am p a- n ia n sh al es T D i n L o w er C am p a- n ia n T D i n "d ia b as e in tr u si o n " ? ? ?? T D i n A p ti an T D i n P al ae o - zo ic T D i n A p ti an T D (G R O # 3 ) in U p p er C re ta ce o u s O ff sh o re e as te rn C an ad a, L ab ra d o r M ar gi n , S ag le k B as in O ff sh o re a n d o n sh o re W es t G re en la n d N u ki k- 1 N u ki k- 2 K an gâ m iu t- 1 Ik er m iu t- 1 G R O # 3 a n d N . N u u ss u aq o u tc ro p Q u lle q -1 G jo a F- 3 7 R al eg h N -1 8 H ek ja O -7 1 K ar ls ef n i A -1 3 R u t H -1 1 Sk o lp E -0 7 G ilb er t F- 5 3 O gm u n d E -7 2 Sn o rr i J- 9 0 So u th L ab ra d o r N -7 9 B ja rn i O -8 2 N o rt h L ei f I- 0 5 R o b er va l K -9 2 1 0 1 5 2 0 2 5 3 0 3 5 4 0 4 5 5 0 5 5 6 0 6 55 P le is . Plio. Holoc. Miocene Oligocene Eocene Paleocene L E L M E L E L M E L E PalaeogeneNeogene Epoch Age Period Ma D an ia n Se la n d ia n T h an et ia n Y p re si an L u te ti an B ar to n ia n P ri ab o n ia n R u p el ia n C h at ti an A q u it an ia n B u rd ig al ia n L an gh ia n Se rr av al lia n To rt o n ia n M es si n ia n Z an cl ea n P ia ce n zi an G el as ia n Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 27 28 speciosum Zone, which they considered to be late Paleo - cene. Similarily, in his study of the North Leif I-05 well, Nøhr-Hansen (2004b) considered the LO of Cero dinium glabrum (as Cerodinium speciosum subsp. gla brum) to be in the late Thanetian. Two index species that have their LOs near the base of the Thanetian according to Williams et al. (2004) are Alisocysta cir - cumtabulata and Alisocysta margarita. These two species occur in several of the West Greenland Margin, Davis Strait and Labrador Margin wells. For example, Aliso - cysta margarita has been recorded from Gilbert F-53, Hekja O-71, Gjoa G-37, North Leif I-05, Ogmund E- 72, Ralegh N-18, Snorri J-90 and South Labrador N- 79 on the Canadian margin and Hellefisk-1, Iker miut-1, Kangâmiut-1, Nujkik-1, Nukik-2, and Qulleq-2 on the West Greenland Margin. The uppermost Thanetian is characterised by maxi- mum abundances of Apectodinium spp. and the range of Axiodinium augustum (Williams et al. 2015), and equates with the interval P6 of Nøhr-Hansen (2003). High abundances of Apectodinium spp. and the pre - sence of Axiodinium augustum were recorded in several wells, e.g. North Leif I-05, South Labrador N-79, Snorri J-90, Ogmund E-72, Rut H-11, Gjoa G-37, Kangâmiut-1 and Ikermiut-1. Ypresian In the Labrador–Baffin Seaway, some of the richest dinocyst assemblages occur in Ypresian sediments. The top of the stage is considered here to be marked by the frequent but never abundant occurrence of the freshwa- ter fern Azolla. Brinkhuis et al. (2006) stated that Azolla is abundant in basal middle Eocene marine sediments of Nordic seas. These authors placed the onset of this phase at c. 49 Ma and the termination at c. 48.3 Ma, probably based on the Gradstein et al. (2004) timescale. Barke et al. (2012) agreed with Brinkhuis et al. (2006) in considering the Azolla blooms to occur at 49 Ma and also regarded the age as early middle Eocene. Brinkhuis et al. (2006) postulated that the high concentrations of Azolla in an ACEX core taken on the Lomonosov Ridge reflected in-situ growth. Brinkhuis et al.(2006) also list- ed wells from the Labrador–Baffin Seaway (Karlsefni A- 13 in the Saglek Basin and Bjarni O-82, North Leif I-05 and Snorri J-90 in the Hopedale Basin) as having lowermost middle Eocene abundances of Azolla. In this study, these wells were not found to contain notable numbers of Azolla. Some other wells, all in the northern Saglek Basin, had greater numbers: Hekja O-71, Ralegh N-18 and Gjoa G-37 (Appendices 3.11–3.13). Even in these wells, however, Azolla was not recorded in high concentrations, more suggestive of transported material than in-situ growth (see further discussion, p. 42–43). Immediately below the Azolla occurrences are the LOs of the dinocyst species Achilleodinium biformoides, Diphyes brevispinum and Piladinium columna. Michoux (1988) described Piladinium (as Charlesdowniea) co - lumna from upper Ypresian rocks of south-western France, stating that nannofossil analyses indicated an NP13 Zone age. Nøhr-Hansen (2003) designated a Piladinium (as Charlesdowniea) columna interval of late Ypresian age, whose top is marked by the LO of the zonal species. Bujak (1994) plotted the LO of both Pilodinium (as Charlesdowniea) columna and Diphyes brevispinum within the NP13 Zone. In the Norwegian– Greenland Sea, Eldrett et al. (2004) calibrated the LO of Piladinium columna with Chron 22n and within nannoplankton zone NP14a, at the top of the Ypresian; this is somewhat later than other records, but is in close accordance with this study. Piladinium columna is wide spread in the Labrador–Baffin Seaway, occurring in the following wells: Gilbert F-53, Gjoa G-37, North Leif I-05, Ogmund E-72, Ralegh N-18, Snorri J-90 and South Labrador N-79 on the Canadian margin, and Kangâmiut-1, Nukik-2 and Qulleq-1 on the West Greenland Margin (Fig. 1). Species of Apectodinium occur throughout the Ypre s - ian. They include Apectodinium parvum, with an LO immediately above the Thanetian–Ypresian bound ary, and Apectodinium homomorphum, which has a peak abun dance at about 54 Ma. Species of Apectodinium are found in a number of wells, including Gjoa G-37, Gil - bert F-53, Hekja O-71, Karlsefni A-13, North Leif I-05, Ogmund E-72, Falegh N-18, Rut H-11, Skolp E-07 and South Labrador N-79 on the Canadian margin, and Helle fisk-1, Ikermiut-1 and Kangâmiut-1 on the West Greenland Margin. The Ypresian is informally subdivided here into early and late, with the boundary based on the LOs of Petalo - dinium condylos, Evittosphaerula foraminosa and Scale no - dinium scalenum. Supporting evidence comes from Bujak (1994), who plotted the consistent occurrence of Petalo - dinium condylos within the nannofossil NP12 zone. Oc - curring above the LO of Petalodinium condylos is the LO of Ginginodinium? flexidentatum. This species appears to equate with Trinovantedinium #LA of Bujak Davies Group (1987). These authors defined a Trino vante di nium #LA Zone, which they considered to be late Ypresian based on foraminiferal data in South La b rador N-79. Ginginodinium? flexidentatum is present in the Ypres ian Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 28 29 in a number of wells, both on the eastern and western margins of the Labrador–Baffin Sea way. These include Gilbert F-53, Hekja O-71, Karl se fni A-13, North Leif I- 05, Ogmund E-72, Rut H-11, Snorri J-90 and South Labrador N-79 on the Canadian margin, and Ikermiut-1 and Nukik-2 on the West Greenland Margin (Fig. 1). One of the characteristic features of the Ypresian and succeeding Lutetian is the occurrence of fungal spore peaks in some of the wells. Selected fungal taxa are shown in Fensome et al. (2016, plate 20, figs 12–20). Lutetian Although much or all of the Lutetian seems to be absent in many of the wells, especially on the West Greenland Margin (Fig. 8), its top seems to be clearly defined by the LO of Diphyes colligerum. Bujak (1994) placed the last consistent LO of this species at the Lutetian–Bar - tonian boundary. Eldrett et al. (2004) considered the LO of Diphyes colligerum to approximate with the Lutetian–Bartonian boundary in the Norwegian–Green - land Sea. We follow Eldrett et al. (2004) in placing the LO of Diphyes colligerum close to the Lutetian–Bar - tonian boundary; this is in contrast to Nøhr-Han sen (2004b), who recorded the LO of Diphyes collige rum at the top of the Ypresian in North Leif I-05. Another important index species having its LO at the top of the Lutetian is Alterbidinium? bicellulum, originally de scrib - ed by Islam (1983) from the Earnley For mation of the middle Eocene Bracklesham Group of southern Eng - land; the age of the Bracklesham Group is latest Ypresian – Lutetian. Nøhr-Hansen (2003) defined the top of his late Lutetian interval on the LO of four taxa, one of which was Alterbidinium? cf. bicellulum. Recognition of the earliest Lutetian is facilitated by the LOs of Eatonicysta ursulae, Cordosphaeridium gracile and Hystrichosphaeridium tubiferum. Bujak (1994) placed the LO of Eatonicysta ursulae just above the base of the Lutetian, in the nannofossil NP14 Zone. He signified the importance of this species by designating an Eatonicysta ursulae Zone. Eldrett et al. (2004) devel- oped a refined biostratigraphy of a DSDP site and two ODP sites in the Norwegian–Greenland Sea based on magnetostratigraphic calibration. These workers deter- mined that the LO of Eatonicysta ursulae was close to the top of the nannofossil NP14a Zone, broadly confirming the findings of Bujak (1994). This species is found in five wells: Kangâmiut-1 and Nukik-2 on the West Greenland Margin and Gjoa G-37, Snorri J-90 and South Labrador N-79 on the Canadian margin. Bujak (1994) also considered the LO of Hystricho sphaeri - dium tubiferum to be in the Lutetian, but in the lower part of the succeeding nannofossil NP15 Zone. Other LOs within the early Lutetian include those of Diphyes ficu- soides, Stichodinium lineidentatum and So p hismatia tenui - vir gula. Some of the events in the late Lutetian are the LOs of Dapsilidinium pseudoinsertum and Glaphyrocysta vicina and the peak of Trithyro di n ium? conservatum. Bartonian The Bartonian is absent or condensed in the Greenland wells but more developed on the Canadian margin (Fig. 8). Following Bujak (1994), the top of this stage is de - fined at the LO of the dinocyst Rhombodinium poro- sum. Dinocysts with their LOs in the Bartonian include Cerebrocysta bartonensis, Chiropteridium gilbertii, and Ho - mo tryblium tenuispinosum. Chiropteridium gilbertii occurs only in wells on the Labrador Margin (Williams 2007e, under the informal name Hystrichokolpoma ‘gil bertii’). Pollen provide much of the stratigraphic control for recognition of Bartonian strata in the Labrador–Baffin Seaway. These include the LOs of Ex tra tri poropollenites spp., Corsinipollenites oculusnoctis, Pi stilli pollenites macgre- gorii and Cicatricososporites eocenicus. Azolla spp. also occur for the last time. Priabonian Priabonian sediments have been identified in only one West Greenland Margin well (Hellefisk-1) but are pre - sent in most of the Labrador Margin and Davis Strait wells. The key species for defining the top of this stage are Areosphaeridium diktyoplokum, Lentinia serrata and Phthanoperidinium multispinum. Powell & Brinkhuis (in Gradstein et al. 2012) placed the LO of Areo sphae r i - dium diktyoplokum at the Priabonian–Rupelian bound - ary. Unfortunately, this species is found only in Helle - fisk-1 on the West Greenland Margin. The LOs of Len - tinia serrata and Phthanoperidinium multispinum ap - pear to define the top of the Priabonian in some Grand Banks wells (e.g. Williams 2003a, b). Support for the LO of Lentinia serrata is provided by Williams et al. (2004), who placed it 0.2 million years above the Pria - bonian–Rupelian boundary. Lentinia serrata is found in Gilbert F-53, North Leif I-05, Ralegh N-18 and South Labrador N-79 on the Canadian margin. Other LO events in the Priabonian include those of the dinocysts Glaphyrocysta texta, Schematophora speciosa, Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 29 30 Cordosphaeridium funiculatum, Phthanoperidinium stock- mansii, Rhombodinium draco and Heteraulacacysta po - rosa. Williams et al. (2004) placed the LOs of Sche ma - tophora speciosa and Cordosphaeridium funiculatum with- in the Priabonian but, in contrast to the observations in this study, considered Rhombodinium draco to range well into the Rupelian. Most of the above species occur only in one well, all on the Canadian margin. Another distinc- tive Priabonian marker is the spore Cicatricosisporites ornatus, which occurs in Snorri J-90. Rupelian Strata of Rupelian age were not encountered in any of the West Greenland Margin wells, but rocks of this age are widespread on the Canadian margin, being present in Bjarni O-81 (Appendix 3.3), Gilbert F-53 (Appendix 3.9), Hekja O-71 (Appendix 3.11), Karlsefni A-13 (Appendix 3.8), North Leif I-05 (Appendix 3.1), Ralegh N-18 (Appendix 3.12) and South Labrador N-79 (Ap - pendix 3.4; Figs 1, 8). The top of the stage is placed at the LO of the two dinocyst species Enneadocysta magna and Licracysta semicirculata (Fig. 6, in pocket). Enneadocysta magna was described by Fensome et al. (2007) from Oli - go cene sections in wells drilled on the Grand Banks. Wil - liams (2003a) used the then-informal name Enneadocysta magna when he noted that it ap peared to be a consistent Rupelian marker species in some Grand Banks wells. Licracysta (as Areoligera) semicirculata was described by Morgenroth (1966) from the middle Oligocene. Wil - liams et al. (2004) placed the LO of Licracysta (as Areo - ligera) semicirculata just below the Rupelian–Chattian boundary. This seems to accord well with the findings of this study. Other dinocyst species that help to delineate the Rupelian are Licracysta corymbus, Phthanoperidinium coreoides and Apteodinium au stra liense. Miospores with LOs in the Rupelian include Zli visporis spp. and Peri - poropollenites sp. Williams (2007b, e). Chattian The Chattian is difficult to delineate, primarily because it is partly or completely absent in all wells apart from Hekja O-71 and Ralegh N-18. We have been able to determine it based only on the LOs of two dinocyst species, Chiropteridium galea and Deflandrea phosphor - itica. Williams et al. (2004) considered that both these species extended into the early Aquitanian in northern mid-latitudes, but for the purposes of this study the LOs of these species are considered to mark the Chat - tian–Aquitanian boundary. Neogene Miocene Dinocyst assemblages in the Neogene of the Labrador– Baffin Seaway are sparse and preservation is generally poor. Both factors, which reflect the coarse clastics that predominate in this interval, may account for some gaps in our interpretations of ages, including the failure to define the Aquitanian, the oldest stage of the Mio - cene. But there is another possibility – that sediments of Aquitanian age are absent in a number of the wells (Fig. 8). Another difficulty in determining ages in the Neo - gene sections is the abundance of reworked palyno - morphs, both Cretaceous and Palaeogene. How ever, there are some taxa that facilitate recognition of the early Miocene. These are primarily the dinocyst Cor - dosphaer i dium cantharellus and the spore Osmunda ci d - ites wellmannii. Williams et al. (2004) placed the LO of Cor do sphaeridium cantharellus in Northern Hemi sphere mid-latitudes at about 19.5 Ma, within the Burdigalian. Middle Miocene strata are indicated from several wells, though it has not been possible to differentiate the Langhian as all the index taxa appear to extend up into the Serravallian. These taxa include the pollen Cary - apollenites spp. and Tiliaepollenites crassipites, and the dinocysts Cleistosphaeridium diversispinosm, Apteo di nium spiridoides and Cannosphaeropsis passio (Fig. 6, in pock- et). Tiliaepollenites crassipites was previously de scribed as Bombacacidites sp. A by Williams (1975) and Wil liams & Bujak (1977). Williams (1975) considered the LO of this species to be middle Miocene in Scotian Margin wells. This age was slightly modified in Wil liams & Bu - jak (1977), who recorded the species from the Labrador Margin Operculodinium centrocarpum as semblage that they considered provisionally to be mid dle to late Mio - cene. Williams (2007e) agreed with Williams (1975) in assigning a middle Miocene age. Cannosphaeropsis pas - sio, first recorded as Nemato sphae ropsis sp. A by Wil - liams & Brideaux (1975) from the upper Miocene of the Grand Banks, was described by de Verteuil & Norris (1996) from the upper middle Miocene of Maryland. Piasecki (2003) placed the LO of this species at the Serravallian–Tortonian boundary in Qulleq-l, an age confirmed by Williams et al. (2004), who likewise plotted its LO at the Serravallian–Tor tonian boundary in Northern Hemisphere mid-latitudes and Equatorial Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 30 31 low-latitudes. Powell & Brinkhuis (in Gradstein et al. 2012) considered the LO of Apteo di nium spiridoides to be at the top of the early Miocene, which conflicts with the range documented here. Like wise, Head et al. (1989a) recorded the species from the lower Miocene of ODP Hole 645E, Baffin Bay (Figs 1, 2), but did not extend its range into the middle Mio cene. Williams et al. (1999) plotted the LO of Apteodi nium spiridoides within the Serravallian, however, which corresponds more closely with our data. Cleistosphae ri dium diver- sispinosum is generally an abundant species worldwide, but is not common in samples from the offshore wells in the Labrador–Baffin Seaway. Head et al. (1989a) noted, however, that the closely related Clei stosphae r - idium (as Systematophora) ancyreum was com mon in samples from the early and middle Miocene of ODP Hole 645E, Baffin Bay (Figs 1, 2). Another related species is Cleistosphaeridium placacanthum, which Schreck et al. (2012) considered to have an LO at 10.6 Ma (early Tortonian) in the dinocyst assemblages from an almost continuous middle Miocene to Pliocene section in ODP Site 907A in the Iceland Sea. Williams et al. (1999) plot- ted the LO of Cleistos phae ridium diversispinosum at the Serravallian–Tortonian boundary. Upper Miocene sediments are more prevalent in the West Greenland wells than in those on the Canadian side, with the Qulleq-1 well appearing to have the most complete section (Piasecki 2003; Appendix 3.14). LOs occurring within the Tortonian include Mini sphae r - idium latirictum, (formerly Cordosphaer idium mini- mum), Hy stric hokolpoma rigaudiae, Palaeocystodinium gol zo wense, Spiniferites pseudofurcatus, Operculodinium janduchenei, Operculodinium giganteum, Operculo di - nium piaseckii, Ed wardsiella sexispinosa and Labyrintho - dinium truncatum. In this study, the boundary between the two late Miocene stages, Tortonian and Messinian, is marked by the LOs of three dinocyst species Tuber - culodinium vancampoae (at the boundary), and Palaeo - cystodinium golzowense and Operculodinium cen trocar- pum in the late Tortonian. Tuberculodinium vancampoae, described from the Pleistocene by Rossignol (1962) is a cyst of the extant genus Pyrophacus. Head et al. (1989a) recorded Tuber culodinium vancampoae from only one sample in the questionable early late Miocene of Hole 645E. This taxon is found in modern sediments, in warm lower latitudes. It is presumed that changing climatic conditions, as noted below, resulted in its migra- tion from higher to lower latitudes toward the end of the Miocene, although there were warming trends in the Pliocene–Pleistocene. According to Powell & Brinkhuis (in Gradstein et al. 2012), the LO of Palaeocystodinium golzowense is within the later Tortonian. Head et al. (1989a) found that Pa laeo cystodinium golzowense was common in the early and middle Miocene of ODP Hole 545E, but became rare up section, in what these authors considered to be early late Miocene. Two dinocyst species, Spiniferites pseudofurcatus and Dapsilidinium pastielsii have regional LOs within the Tortonian. Head et al. (1989a) recorded rare but consis- tent occurrences of the closely related Dapsilidinium pseu do - colligerum from the middle Miocene in ODP Hole 645E, Baffin Bay, possibly extending into the early late Miocene. Although Mertens et al. (2014) treated Dapsili - di nium pseudocolligerum as a taxonomic junior synonym of Dapsilidinium pastielsii, we prefer to retain Dapsili - dinium pseudocolligerum, which appears to have a restrict- ed stratigraphic range in the Labrador–Baffin Seaway. Head & Westphal (1999) noted that the latitudinal occurrences of this species contracted in the late Miocene and Pliocene, due to the cooling of the North Atlantic in the late Miocene and the evolution of the cold Labrador Current. Thus climatic changes and oceanic currents rather than extinction explain the disappearance of the genus Dapsilidinium and the species Tuberculodinium van campoae from the Labrador–Baffin Seaway in the late Miocene. Within the Messinian, species of the pollen Quer - coidites are common but do not appear to range above the Miocene. Spiniferites ovatus, described from the late Mio - cene of Japan, also has its LO at the top of this stage. Pliocene–Pleistocene We have not been able to differentiate the Pliocene and Pleistocene in the wells analysed for this bulletin, but Piasecki (2003) made some determinations based on analysis of the Qulleq-1 well (Appendix 3.14). He plot- ted the LO of Habibacysta tectata immediately above the base of the Zanclean. This may be too high, based on the findings of Schreck et al. (2012), who placed its LO in the middle Langhian in ODP Hole 907A in the Iceland Sea. A probable explanation for this discrepancy is that the specimens from Qulleq-1 are reworked. Other spe - cies recorded by Piasecki (2003) as having their LOs in the Zanclean include Barssidinium graminosum, Inver to - cysta lacrymosa, Selenopemphix nephroides, Seleno pemp hix bre vi spinosa, and Reticulatosphaera actinocoronata. Pia se - c ki (2003) also distinguished the Piacenzian–Gela sian bound ary based on the LO of Cymatiosphaera invaginata. In our analyses, we recognised the Pliocene–Plei sto - cene based on the presence of the LOs of the pollen taxa, Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 31 32 Zonalapollenites igniculus, Graminidites sp. A of Williams & Brideaux (1975), and Compositoipollenites sp. B of Williams & Brideaux (1975). Williams (1975) defined an Artemisia–Taraxacum Zone, which he con sidered to be Pliocene–Pleistocene. Furthermore, Wil liams & Bu - jak (1977), in a study of four Labrador Margin wells, defined a Zonalapollenites (as Tsugae polle nites) igniculus assemblage of Pliocene–Pleistocene age. Discussion Cretaceous According to Umpleby (1979), the oldest Mesozoic rocks beneath the Labrador Sea are of Barremian age. It has not been possible to confirm a Barremian age in this study, but the presence of Aptian rocks has been determined in the South Labrador N-79, Roberval K-92, Snorri J-90, and Bjarni O-82 wells (Figs 1, 2, 7). Questionable up per Aptian ‒ Albian rocks occur in Og mund E-72 and North Leif I-05. All of these wells are in the Hopedale Basin. In the Saglek Basin, Albian–Cenomanian rocks are encoun- tered in the lowermost 475 m of Skolp E-07. Question - able Cenomanian strata are present in Bjarni O-82, North Leif I-05 and Og mund E-72. In the Bjarni O-82 well, a major hiatus is identified, with much of the Albian and Cenomanian missing. This is equivalent to the Avalon Unconformity (Fig. 3) identified by McWhae et al. (1980) as a regional uncon- formity in the Labrador–Baffin Seaway. We recognise another hiatus in several wells: in South Labrador N-79, Aptian strata are overlain by Coniacian rocks; in Ogmund E-72, the Cenomanian is overlain by Campanian; in North Leif I-05, Ceno manian–Turonian is overlain by Maastrichtian; and in Skolp E-07, Albian– Cenomanian strata are overlain by Campanian strata. Thus, much of the Upper Cre taceous section appears to be missing in the Hopedale and Saglek Basins. These observations accord with those of Balkwill et al. (1990), who noted that the Cen o manian–Santonian succession is condensed, discontinuous and sometimes absent on the Labrador Margin. (Fig. 7). In offshore West Green - land, the oldest drilled Cretaceous rocks are in the Qul leq- 1 well, where upper Santonian rocks were en coun tered in the lowermost c. 300 m of the well. The continuation of the rift phase during the latest Cretaceous is represented by thicker, more continuous sequences, although significant gaps in the succession still occur. In parts of the Hopedale Basin, such as at Bjarni O-82 and Ogmund E-72, the Campanian is incomplete, with the lower part presumed missing. At North Leif I-05, the Campanian is absent. This con - trasts with the situation in Skolp E-07, where the Campanian is about 1050 m thick. In offshore West Greenland, lower Campanian sediments occur only in the Ikermiut-1 and Qulleq-1 wells, with the upper Cam - panian and Maastrichtian absent. Reworked specimens of Albian, Turonian and late Maastrichtian taxa are pre - sent in the lowermost part of the Kangâmiut-1 well, which is dated as Paleocene. The Upper Cretaceous – Palaeogene sequence on the Labrador Margin is variably developed. In the Skolp E- 07 well, for example, the upper Maastrichtian succes - sion appears to be overlain by a thin succession of possi- bly Danian age, which is in turn overlain by Ypresian strata. Other wells such as North Leif I-05 and South Labrador N-79 in the Hopedale Basin have more com - plete sections, including Maastrichtian rocks in the for - mer and Danian rocks in the latter (Nøhr-Hansen 2004b). Onshore, in the Nuussuaq Basin, Aptian? to Al - bian strata are the oldest Mesozoic rocks overlying base- ment (Dam et al. 2009; Pedersen & Nøhr-Hansen 2014). Most of the Upper Cretaceous is represented except for hiatuses in the middle Turonian, lower Cam - panian and middle Maastrichtian (Figs 7, 9). Palaeogene The thickness of Paleocene sediments on the Labrador Margin varies considerably both between and within basins. This is shown by successions in the Gjoa G-37, Hekja O-71 and Ralegh N-18 wells, all of which are in that part of the Saglek Basin that underlies the Davis Strait (Figs 1, 2). Within these three wells, the most complete Paleocene sequence is in Gjoa G-37, which has minimal Danian, partial Selandian and Thanetian rocks. Hekja O-71 appears to have Selandian and Tha - netian strata, whereas Ralegh N-18 has only Thanetian rocks. Wells farther south in the Saglek Basin contain minimal Paleocene (e.g. Skolp E-07, Figs 1, 2, 8) or a condensed Selandian and Thanetian succession (e.g. Gilbert F-53). In the Hopedale Basin, the Paleocene succession is thin and discontinuous in Bjarni O-82 and Ogmund E-72. In North Leif I-05 and Ogmund E-72, only Danian and Thanetian strata are present. And in South Labrador N-79, the Selandian is con - densed (Fig. 8), perhaps reflecting slower sedimenta- tion rates due to uplift. A major Danian hiatus occurs in wells off West Green - land, with upper Paleocene strata directly overlying lower Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 32 33 Campanian rocks in Ikermiut-1 and Qulleq-1 (Fig. 8). A thin Danian section occurs, however, in Nukik-2 (Nøhr- Hansen 2003). Upper Selandian and Thanetian strata occur in the lowermost part of Kangâmiut-1 and Helle - fisk-1, whereas Thanetian seems to be the oldest strata in Nukik-1 (Fig. 8). We consider this hiatus on the two mar - gins to equate with the Bylot Unconformity of McWhae et al. (1980) and with the base-Tertiary unconformity of Sinclair (1988), although the gap is greater on the Green - land margin. This is considered to represent the break-up unconformity marking the onset of drifting in the La b - rador Sea; this conforms with the conclusion of Chal mers & Pulvertaft (2001) that the drift phase started during the Selandian. Onshore in the Nuussuaq Basin, a lower Dan - ian to possibly lower Selandian clastic succession is present (Nøhr-Hansen et al. 2002; Dam et al. 2009; Pedersen & Nøhr-Hansen 2014; Fig. 3); this is overlain by a thick pile of volcanic rocks (Larsen et al. 2016; Fig. 3). A less obvious hiatus, involving the absence of part or all of the Selandian or a condensed sequence, occurs on the Labrador Margin in several wells, including Gjoa G-37 (as noted above) in the Saglek Basin and Bjarni 0- 82, North Leif L-05, Snorri J-90 and South Labrador N-79 in the Hopedale Basin (Figs 1, 2, 8). On the West Greenland Margin, Danian sediments in the Nukik-2 well are overlain by upper Selandian sediments. At first glance, the Selandian hiatus appears to be part of the Bylot Unconformity, but the occurrence of Danian se - di ments suggests a more complex scenario. In a number of wells on both sides of the Labrador Sea, parts of the middle Eocene are marked by a hiatus or a condensed section representing the Mid-Eocene Unconformity of Dalhoff et al. (2003; Fig. 8). These wells are: Bjarni O-82, North Leif I-05, Ogmund E-72 and South Labrador N-79 in the Hopedale Basin; Gilbert F-53, Gjoa G-37 and Ralegh N-18 in the Saglek Basin; and Hellefisk-1, Ikermiut-1 and Kangâmiut-1 off West Greenland (Nøhr-Hansen 2003). Hiatuses in the younger Palaeogene and Neogene are difficult to determine, largely because sedimentation is dominated by coarse clastic rocks with a low preserva- tion potential for palynomorphs. A hiatus is recognised within the Oligocene, however, on both sides of the Labrador Sea and it extends into the Miocene in several wells. On the western margin, this hiatus seems to pri - marily represent the Chattian, though it may include part of the Rupelian. In the southern Hopedale Basin, Chattian strata are absent in South Labrador N-79. In Bjarni O-82, however, the thick Rupelian interval is overlain by strata that may be of Chattian age. In Snorri J-90 in the northern Hopedale Basin, Rupelian sedi- ments appear to be directly overlain by Miocene sedi- ments (Fig. 8; Appendix 3.5). The Rupelian is also thick in some of the Saglek Basin wells, such as Gilbert F-53 to the south, and sediments of this age are present in Gjoa G-37 and Hekja O-71 to the north. In Hekja O- 71, the thick Rupelian section is overlain by up to 30 m of Chattian sediment, an interval not usually pre served in the region. The Oligocene hiatus of the western Labrador Sea pro bably corresponds to the regional unconformity pla ced at the top of the Kenamu Formation by Balkwill et al. (1990), the Baffin Bay Unconformity (Fig. 6, in pocket, Fig. 8). These authors pointed out that most of the inner and central parts of the northern Labrador and south-eastern Baffin Margins were emergent in the middle to late Oligocene, so that the oldest post-drift rocks are represented by the lower member of the Mokami Formation (Fig. 3). Off West Greenland, Rolle (1985) recorded Oligo - cene strata in Hellefisk-1 and possible Oligocene strata in four wells: Ikermiut-1, Kangâmiut-1, Nukik-1 and Nu - kik-2 (Figs 1–3, 8). However, based on more recent bio - stratigraphic data, it is most likely that the Oligocene unconformity extends across to the Greenland side, since Piasecki (2003) recorded an Ypresian–Serravallian hiatus in Qulleq-1. The youngest Palaeogene interval found by Nøhr-Hansen (2003) in Hellefisk-1 is of Priabonian age (Figs 3, 8; Appendix 3.19). This Oligocene unconformity broadly correlates with the cessation of sea-floor spreading in the Rupelian in the northern Labrador Sea and in the Davis Strait, and probably also in Baffin Bay. Srivastava (1978) and Dickie et al. (2011) considered that the cessation of sea- floor spreading occurred during the Priabonian (Ano - maly 13). However, a more likely cause for the uncon- formity was the development of the Antarctic Cir cum - polar Current between 33 and 30 Ma, which marked the onset of Antarctic glaciation. This triggered a drop in sea level that was worldwide (Haq et al. 1987; Haq & Al- Qahtani 2005). Neogene Unconformities spanning the Palaeogene–Neogene bound ary and within the Neogene in the Labrador–Baf - fin Seaway are difficult to identify and correlate. As noted earlier, McWhae et al. (1980) placed the Beau - fort Unconformity between the Mokami Formation and the overlying Saglek Formation (Fig. 3); Grant (1980) postulated a regional upper Miocene unconfor- Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 33 34 0 Ma 5 10 15 20 25 30 35 40 45 50 55 60 65 70 75 80 85 90 95 100 105 110 115 120 125 Late Cretaceous Paleocene Eocene Oligocene Miocene Pliocene Quaternary P er io d / E p o ch A ge ( st ag e) Fo rm at io n M em b er R eg io n al (D ic ki e et a l. 2 0 1 1 ) L ab ra d o r M ar gi n (M cW h ae 1 9 8 1 ) Early Cretaceous Aptian Albian Cenomanian Turonian Coniacian Santonian Campanian Maastrichtian Danian Selandian Thanetian Ypresian Lutetian Bartonian Priabonian Rupelian Chattian Aquitanian Burdigalian Langhian Serravallian Tortonian Messinian Zanclean Piacenzian Mokami Kenamu Cartwright Markland Bjarni Saglek Upper Lower Upper Leif Lower Lower Upper + Middle Gudrid Lower Gudrid Upper Freydis Lower Freydis Upper Sn o rr i J- 9 0 H e k ja O -7 1 N o rt h L e if I- 0 5 B e au fo rt B af fin B ay B yl o t A va lo n L ab ra d o r R o b e rv al K -9 2 B ja rn i O -8 2 O gm u n d E -7 2 S. L ab ra d o r N -7 9 Sk o lp E -0 7 K ar ls e fn i A -1 3 G ilb e rt F -5 3 R u t H -1 1 R al e gh N -1 8 G jo a G -3 7 S N Chronostratigraphy Hiatuses Labrador Margin Preserved stratigraphic interval Labrador Margin lithostratigraphy Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 34 35 Ma H e lle fis k -1 N u k ik -1 N u k ik -2 K an gâ m iu t- 1 Ik e rm iu t- 1 Q u lle q -1 G R O # 3 & s u rf ac e se ct io n s N . N u u ss u aq U m iiv ik -1 , Sv ar te n h u k H al vø & N . N u u ss u aq , su rf ac e s e ct io n s S N Late Cretaceous Paleocene Eocene Oligocene Miocene Pliocene Quaternary P er io d / E p o ch A ge ( st ag e) Early Cretaceous Aptian Albian Cenomanian Turonian Coniacian Santonian Campanian Maastrichtian Danian Selandian Thanetian Ypresian Lutetian Bartonian Priabonian Rupelian Chattian Aquitanian Burdigalian Langhian Serravallian Tortonian Messinian Zanclean 0 5 10 15 20 25 30 35 40 45 50 55 60 65 70 75 80 85 90 95 100 105 110 115 120 125 N o t p en et ra te d o ff sh o re Chronostratigraphy West Greenland Margin Preserved stratigraphic interval Stratigraphic record Labrador 0 % % 100 100 West Greenland (offshore) 0 Piacenzian Fig. 9. Schematic representation of the preserved stratigraphic record on the Labrador and Greenland Margins, comparing the preserved record in the sections individually and collec- tively with the hiatuses linked to unconformities reported in the literature. Dickie et al. (2011) recognised a number of uncon- formities in two or more of three regions – Southwest Greenland Shelf, the Labrador Shelf and the Jeanne d’Arc Basin, offshore Newfoundland (red, all three regions; green, two regions). McWhae (1981) named five unconformities on the Labrador Margin; the hiatuses associated with these unconformities indi- cated here are estimates by McWhae (1981) based on an unspecified timescale and thus should be considered approxi- mate. The ‘cumulative preserva- tion’ plots (right) depict sche - ma tically the proportion of wells that contain sediments of a speci- fied age, based on one million- year slots; note that these calcu - lations only include wells that extend down to/beyond the rele- vant stratigraphic level. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 35 36 mity. In the wells we have examined, a middle to late Miocene hiatus occurs in the Hopedale Basin. For ex - ample in Bjarni O-82 (Fig. 8), the Serravallian is over- lain by Pliocene–Pleistocene sediments, indicating that all of the upper Miocene is absent. A similar situation seems to exist in South Labrador N-79, where Plio - cene–Pleistocene sediments apparently overlie the mid - dle Miocene succession (Fig. 8). Furthermore, in Snorri J-90 in the northern part of the Hopedale Basin, the upper middle Miocene is missing (Fig. 8). Evidence in the Saglek Basin is more tenuous. In Gilbert F-53, the sparse palynomorph assemblage pro - vides inconclusive evidence, but the thin nature of the Miocene strongly suggests a significant hiatus. Un for - tunately, in Gjoa G-37 and Hekja O-71, samples were not available from the upper drilled interval and the uppermost samples analysed are of Rupelian and early Miocene age, respectively. In offshore West Greenland, Piasecki (2003) recorded middle Miocene as the oldest Neogene interval in the Kangâmiut-1 well. A similar situation may exist in the Nukik-1, Nukik-2, Ikermiut-1 and Hellefisk-1 wells, although no marker species were recorded among the sparse palynomorph assemblages in the samples from the upper part of the Ikermiut-1 and Hellefisk-1 wells. In summation, there is convincing evidence that some of the Eocene and all of the Oligocene and lower Miocene are missing on the West Greenland Margin, so that middle Miocene sediments directly overlie those of Ypresian to Priabonian age. On the western margin of the seaway, however, there is a middle to late Mio - cene hiatus, especially in the Hopedale Basin (Fig. 8). This hiatus may be equivalent to the Beaufort Un con - formity (Fig. 3) of McWhae et al. (1980) and McWhae (1981). Palaeoenvironmental results General considerations The general methodology of palaeoenvironmental in - ter pretation in this study is reviewed in this and the following sections. The initial approach for some wells was to develop palaeoenvironmental plots showing the ratio of mio spores to dinocysts, having separated out acritarchs and other organic-walled organisms, such as massullae of Azolla. This ratio provides a rough esti- mate of distance from the shoreline, although it can be misleading be cause of the dominance of bisaccate pol - len far offshore and the general decrease in dinocysts in oligotrophic zones (see below). If there are no dinocysts present it was assumed, perhaps incorrectly, that the sediments were non-marine. Subsequently, the focus of the pa laeo ecological study switched to fluctuations in dino cyst assemblages and how the palaeoenvironmental de terminations compared with previous results in the Labrador–Baffin Seaway region, The palaeoenvironmental interpretations are based on detailed counts for six wells: Bjarni O-82, Gilbert F-53, Gjoa G-37, Hejka O-71, Snorri J-90 and South Lab - rador N-79, but are augmented by general observations from other wells. For these six wells, counts of 100 to 200 specimens per sample were made where possible. Dino - cyst taxa considered significant are listed in Table 1, and the plots in Appendix 2 include a column highlighting palaeoenvironmental interpretations. The co lumn has five subdivisions: non-marine, marginal ma rine, in ner neritic, outer neritic and open ocean, and the environ- mental assessment through time is indicated for each well by a curve in this column. Both quantitative and qualita- tive data have been assessed in developing the palaeoen- vironmental curves. For example, the presence of two or three specimens of Impagidinium was deemed sufficient to interpret the palaeoenvironment as open ocean (Dale 1996), although as Zonneveld et al. (2013) noted, Impa - g idinium is not invariably restricted to open-ocean envi- ronments in recent sediments. However, to strengthen the interpretations, occurrences of Impagidi nium in the Labrador–Baffin Seaway wells were com pared with plank tonic foraminiferal data. Palaeoenvironmental curves for the Palaeogene successions in Greenland wells (Hellefisk-1, Ikermiut- 1, Kangâmiut-1, Nukik-1 and Nukik-2) published in Rasmussen et al. (2003) are included in the present study (Appendices 3.15–3.19). The curves indicate the presence of littoral/lagoonal (transitional), inner nerit- Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 36 37 ic, middle neritic, outer neritic and upper bathyal pa - laeo environments, and were interpreted from the pa ly - no morph content (mainly dinocysts and their species rich ness, freshwater algae, fungal spores, miospores, plant tissues) in association with data from other fossils (mainly foraminifera, radiolarians, diatoms, ostracods, gas tro pods, bivalves and calcareous nannofossils). In gener al, the pa - laeo environmental signals from different fossil groups show similar trends (Rasmussen et al. 2003); the discrep- ancies that do occur may be due to the fact that most of the samples studied are cuttings. Use of dinocysts for palaeoenvironmental interpreta- tions can be misleading. Dinocyst assemblages tend to reflect distance from shore rather than water depth, which is why ‘open ocean’ is used in Appendix 2 rather than ‘bathyal’. Since the relationship between water depth and distance from shore is not a simple one – varying for example in relation to shelf width – the curves presented here should be treated with some circumspection. Further caution is needed because, as with the biostratigraphy, the palaeoenvironmental in - ter pretations are based on data from cuttings that can lead to misinterpretation due to downwell contamina- tion. However, the curves, most of which have been reported previously (Williams 2007a–e), do show gen - er al trends and agree well with interpretations from, for example, foraminiferal and sedimentological data (Bu - jak Davies Group 1987; Miller & d’Eon 1987). Palaeoenvironments and dinocysts: previous studies Pioneering studies in interpreting palaeoenvironments from dinocyst assemblages were by Gocht (1969) and Downie et al. (1971). One early approach involved the ‘gonyaulacacean ratio’, based on an innovative study of the Campanian Bearpaw Formation of Alberta by Har - land (1973). This author defined the ratio as the num - ber of species that have a gonyaulacacean affinity di vided by the number of species having a peridiniacean affini- ty. Thus the ratio reflects number of species rather than number of specimens. Harland assumed that when the number of gonyaulacacean species is higher than the number of peridiniacean species, more open-marine conditions prevailed. The interpretations based on this approach were in agreement with the foraminiferal data for the Bearpaw Formation. In our studies, however, it was found that specimen counts were more meaningful than number of species. Palaeoenvironental studies using dinocysts have ex - panded significantly in the past thirty years. Important works include those by Köthe (1990), Brink huis (1994), Dale (1996), Stover et al. (1996), Powell et al. (1996), Jaramillo & Oboh-Ikuenobe (1999), Sluijs et al. (2005), Sluijs et al. (2008), Sluijs & Brinkhuis (2009), Guerstein et al. (2008), Lebedeva (2010) and Schreck et al. (2012). The comprehensive atlas of the occurrences of modern cyst-forming dinoflagellates by Zonneveld et al. (2013) is also very helpful in projecting modern distri butions into the past. From a review of the literature, it is clear that some palaeoenvironments are more clearly interpreted than others from dinocyst assemblages, and some taxa give clearer signals than others. One such signal comes from the late Early Cretaceous ceratiacean cysts with adnate apical archaeopyles – Nyktericysta and Vesperopsis. Mac - Rae (1996) noted that several studies – including Wight - man et al. (1987), Bint (1986), Banerjee & Davies (1988) and Leckie & Singh (1991) – had suggested that at least some species of Nyktericysta and Vesperopsis were specialised for brackish or freshwater environments. Nøhr-Hansen (1992, 2008), Zippi (1998), Dolby et al. Table 1. Palaeoenvironmental preferences of dinocyst taxa in the Labrador–Baffin Seaway Coastal – marginal marine Inner neritic Outer neritic Open ocean Cannosphaeropsis Impagidinium Nematosphaeropsis Pterodinium Cerodinium Cleistosphaeridium Cordosphaeridium Hystrichokolpoma Hystrichosphaeridium Operculodinium Phelodinium Spiniferites Areoligera Cleistosphaeridium Cribroperidinium Deflandrea Dinogymnium Glaphyrocysta Heterosphaeridium Micrhystridium* Phthanoperidinium Wetzeliella Eocladopyxis Heteraulacacysta Homotryblium Micrhystridium* Nyktericysta Polysphaeridium Tuberculodinium Vesperopsis * Acritarch Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 37 38 (2013) and Pedersen & Nøhr-Hansen (2014) similarly concluded that Vesperopsis mayi and Nyktericysta (as Bal mula) tripenta and similar ceratiacean taxa seem to be associated with non-marine to marginal marine en - vironments. In the Cenozoic, some of the most useful dinocyst taxa for indicating marginal marine palaeoenviron- ments are members of the family Goniodomaceae, in - cluding Homotryblium tenuispinosum (Brinkhuis 1994) and Eocladopyxis (Sluijs et al. 2005). Crouch et al. (2001, 2003) and Sluijs et al. (2005) also noted that abundances of the peridiniacean (wetzelielloidean) Apec - to dinium spp. were common in marginal marine settings in the late Paleocene – early Eocene. Brinkhuis (1994) con - sidered Areoligera, Glaphyrocysta, Homotryblium, Oper cu lo - dinium, Spiniferites and Areosphaeridium to define inner- shelf palaeoenvironments in the early Cenozoic. An example of conflicting palaeoenvironmental in - ter pretations involves the findings of Heilmann- Clausen (1994) and Powell et al. (1996). Heil mann- Clausen (1994) considered Areoligera gippingensis to be indicative of offshore marine enironments. He noted (Heilmann-Clausen 1994, p. 53) that Areoligera gippin- gensis is abundant throughout the latest Selandian – early Thanetian Alisocysta margarita zone in Denmark, where “the entire zone occurs in a clearly offshore set - ting”. Powell et al. (1996), however, described an Areo - ligera-dominated assemblage (probably equivalent to the Areoligera gippingensis complex of this study) from the Thanetian type section of southern England. In their Pegwell Bay section, they noted three intervals where Areoligera was ‘superabundant’ and three where it was ‘abundant’. According to Powell et al. (1996), such horizons denote restricted high-energy, marginal marine settings typical of a transgressive regime. They believed that the richest samples were close to the most condensed interval or maximum flooding surface. As discussed further below, it appears that assemblages rich in specimens of the Areoligera gippingensis complex can give mixed messages. Downie et al. (1971) postulated that their Ypresian Wetzeliella association was estuarine. This association was dominated by species of Wetzeliella and (perhaps) Deflandrea. Dominant taxa included Apectodinium (as Wetzeliella) homomorphum, Apectodinium (as Wetze liel - la) parvum and Deflandrea phosphoritica. Firth (1996), who studied high-latitude North Atlantic dinocyst assemblages from ODP Hole 913B, found relative abundance peaks of Deflandrea spp., together with Phthanoperidinium spp., in strata that are primarily diatom- and radiolarian-rich biosiliceous oozes that clearly originated in a deep-water, open-ocean palaeo - environment. Firth (1996) concluded that these peaks could reflect high palaeoproductivity events. The inter- pretations of Downie et al. (1971) and Firth (1996) demonstrate that similar dinocyst assemblages may re - flect conditions such as nutrient enrichment (usually resulting from upwelling) that may occur in a range of marine settings, as is the case today. More clarity was provided by the studies of Brink - huis et al. (2003) and Sluijs et al. (2003), who showed that lithological, geochemical, grain-size and diatom data indicate that high abundances of Deflandrea and Phthanoperidinium denoted shallow-water palaeoenvi- ronments. Köthe (1990) also concluded that common to abundant occurrences of Phthanoperidinium suggest an inner neritic palaeoenvironment. Clearly, the palaeo - environmental interpretation of dinocyst assemblages is best unravelled with support from other evidence, such as lithological and benthic foraminiferal data. Harding (1990), Eshet et al. (1994), Brinkhuis et al. (1998) and van Mourik et al. (2001) all suggested that high abundances of Palaeoperidinium cysts indicate higher nutrient levels that reflect terrigenous input and therefore palaeoenvironments probably nearer to shore. However, since nutrient enrichment can be related to upwelling processes, as shown later for shelf-edge settings, more than one interpretation is possible for the abundant occurrences of Palaeoperidinium. Oligotrophic palaeoenvironments are commonly associated with mid-shelf settings, where nutrients are low, relative to more nutrient-rich proximal settings, and distal locations where there is upwelling (Sluijs et al. 2005). In the Labrador Margin wells, oligotrophic palaeoenvironments can usually be determined from the dramatic drop in numbers of dinocyst specimens, which is commonly accompanied by a marked relative increase in the number of miospores. This is demon- strable in the interval 2020–1450 m in Gilbert F-53 (Appendix 2.4), in which dinocyst specimen counts are extremely low (Williams 2007e) and where the fora - miniferal data confirm that the palaeoenvironment was middle neritic (Miller & Helenes 1989c). For example there are nine dinocysts compared to 95 miospores at 1940–1930 m. It is extremely difficult to determine which dinocyst species are characteristic of outer neritic palaeoenviron- ments. In their study of early Eocene assemblages, Downie et al. (1971) postulated that their Hystricho - sphaeridium association is indicative of open-sea pa - laeoenvironments. This association included species of Achomosphaera, Cordosphaeridium, Hystricho sphaeri dium Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 38 39 and Spiniferites. Brinkhuis (1994) came to similar but more detailed conclusions: in his Priabonian outer neri - tic dinocyst assemblages, he included the taxa Cleisto - sphaeridium, Spiniferites, Areosphaeridium, Oper culo di- nium, Nematosphaeropsis and Cannosphaeropsis. Other taxa indicating outer neritic palaeoenvironments are species of Hystrichokolpoma; this genus, which can also be associated with Impagidinium, is suggestive of open- ocean conditions (Williams 2007e). Support for this interpretation is provided by foraminiferal data for the Gilbert F-53 well (Bujak Davies Group 1987). Open-ocean palaeoenvironments are characterised by the occurrence of Impagidinium (Sluijs et al. 2005). This conclusion is based on the pioneering study of Wall et al. (1977). Fortunately Impagidinium occurs in the Late Cretaceous, at least in the Maastrichtian in this study, as well as ranging throughout the Cenozoic. Hystrichokolpoma, as discussed above, can also indicate outer neritic to open-ocean palaeoenvironments, just as Areoligera (herein Areoligera gippingensis complex) abun - dances seem to do in the Paleocene. This is confirmed by foraminiferal data in the Labrador Margin wells (Miller & Helenes 1989b; Williams 2007e). Previous palaeoenvironmental interpretations from the Labrador– Baffin Seaway Published palaeoenvironmental conclusions on the western Labrador Sea wells are based on foraminifera (Gradstein & Williams 1976; Gradstein & Srivastava 1980; Bujak Davies Group 1987; Miller & Helenes 1989a–c; Ainsworth et al. 2014), palynomorphs (Grad - stein & Williams 1976, Williams 2007a–f) and nanno- fossils (Crux & Gard 2004). Similar findings for West Greenland utilise foraminiferal, nannofossil and paly- nological studies of the lower Palaeogene (Rasmussen et al. 2003; Sheldon 2003) and dinocyst studies of the Neogene (Piasecki 2003). Using foramineral and palynological data from wells, Gradstein & Williams (1976) concluded that deposi- tional environments on the Labrador Margin evolved from non-marine in the Early Cretaceous to possibly neritic in the Late Cretaceous – Paleocene, then to bathyal in the Eocene, neritic in the Oligocene–Mio - cene, and littoral and non-marine in the Pliocene–Plei - stocene. An apparent conflict is evident between the palynological and foraminiferal data from the Eocene, where the foraminifera indicate bathyal palaeoenviron- ments and the dinocysts suggest inner neritic condi- tions; the most plausible explanation seems to be that the dinocysts were redeposited. In a reappraisal of the data, Gradstein & Srivastava (1980) defined four depositional palaeoenvironments for Labrador Margin wells, again based on foraminifera and palynomorphs. These were: non-marine; shallow neritic (taken to include marginal marine to inner shelf, with water depths less than 100 m); deep neritic (with water depths ranging from 100–200 m); and bathyal or upper slope (with water depths from 200–1000 m). According to these authors, marine sedimentation start ed in the middle Late Cretaceous in the Labrador Sea, but the main transgression began during the Maa - strichtian, thus coinciding with the onset of sea-floor spreading during Anomaly 32. Neritic to bathyal con - ditions persisted throughout Paleocene and Eocene times, with the deepest water (bathyal) palaeoenviron- ments in the Eocene reflecting rapid subsidence at that time. Near the Eocene–Oligocene boundary, at the end of sea-floor spreading, palaeoenvironments changed from deep to shallow marine, the latter conditions per - sisting through the later Cenozoic. According to Grad - stein & Srivastava (1980), the only exception was in Kangâmiut-1 where deeper water environments per - sisted into the Neogene. Foraminiferal analyses of cores from Leg 105, Site 645 in Baffin Bay (Srivastava et. al. 1987) showed that an upper slope palaeoenvironment persisted there in the Miocene. The dinocysts from the same interval indicat- ed open-marine conditions. Higher in the Miocene, open-marine and neritic dinocyst species occur, proba- bly reflecting redeposition of the latter. At Site 646, palaeoenvironments were generally lower bathyal. Results and interpretations Cretaceous The observations made during this study support earli- er findings that non-marine conditions prevailed du r - ing the Early Cretaceous on what is today the Labrador Margin (Gradstein & Williams 1976); this interpreta- tion is based on the fact that many assemblages in this part of the section consist exclusively of miospores. Balkwill et al. (1990) considered the Bjarni Formation, which they dated as early Barremian to Albian, to repre- sent lacustrine deposits. However, the occasional occur- rence of species of Nyktericysta and Vesperopsis on both sides of the seaway suggests a non-marine to marginal marine setting, as does the presence of Subtilisphaera Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 39 40 spp. in Bjarni O-82 and Pseudoceratium sp. in Roberval K-92. The interval containing these dinocysts was inter- preted as non-marine by Miller & d’Eon (1987), but Williams (2007a) interpreted it in part as marginal marine, based on the few dinocysts present. The overlying rocks contain other Aptian dinocyst species, especially Tenua hystrix, which is known only from shallow marine palaeoenvironments. Thus, marine environments extended back to about 120 Ma. Possible evidence for earlier marine conditions in the Davis Strait area are the reworked Late Jurassic dinocysts Peris seia - sphaeridium pannosum and Fromea tornatilis recorded from Qulleq-1 by Nøhr-Hansen et al. (2000). Nyktericysta is present and sometimes common in the Aptian of South Labrador N-79, the Albian–Ce - nomanian in Ogmund E-72, and North Leif I-05 in the Hopedale Basin (Nøhr-Hansen in Sønderholm et al. 2003b; Nøhr-Hansen 2004b; Williams 2007b) and in samples from Nuussuaq and Disko in the Nuussuaq Basin of onshore West Greenland (Nøhr-Hansen 2008; Pedersen & Nøhr-Hansen 2014). These onshore Green - land occurrences accord well with Labrador Sea obser- vations, and suggest that conditions in the entire region fluctuated between shallow marine and lagoonal to la - custrine in the Aptian?/Albian to Cenomanian. Inner neritic conditions became widespread in the Turo nian/Coniacian to Santonian interval. Dinocysts are usually abundant in such settings, especially in the vicinity of discharge from rivers, where nutrients are plentiful. Taxa that appear to indicate inner neritic palaeoenvironments in this interval include Hetero - sphaeridium difficile, Circulodinium distinctum, Chatan - giella and Gillinia hymenophora. These conclusions are based on the studies of shallow-water assemblages from Bylot Island (G.L.Williams, unpublished data), in which foraminifera are absent. More open-ocean, presumably deeper water palaeo - environments developed in the Campanian and Maa - strichtian, as shown in Gilbert F-53 in the Saglek Basin and Bjarni O-82 and South Labrador N-79 in the Hopedale Basin. Foraminiferal data for all three wells indicate that the palaeoenvironments were bathyal (Bu - jak Davies Group 1987). Cenozoic Intervals with occurrences of Phelodinium kozlowskii tend to also contain foraminifera that indicate a bathyal palaeoenvironment (Bujak Davies Group 1987); hence, the former may indicate an outer neritic or open-ocean palaeoenvironment. Phelodinium kozlow skii occurs in some samples between 3200 and 2740 m in Gilbert F- 53, an interval that is of Maastrichtian (3250–3120 m) to Danian (3100–2740 m) age (Wil liams 2007e). This deeper water interpretation seems to be in conflict with the presence of the hiatus between the Cretaceous and Cenozoic sediments in some of the wells. However, upper Maastrichtian and Danian to Selandian strata, including transitional Cretaceous–Ce nozoic strata, oc - cur in Nuussuaq. Other common dinocyst taxa in the Paleocene are Alterbidinium spp., Areoligera gippingensis, Cerodinium diebelii, Cerodinium speciosum, Glaphyrocysta divarica- ta, Hystrichosphaeridium tubiferum, Palaeocystodinium golzowense, Palaeoperidinium pyrophorum and Trithyro - dinium evittii. The pollen Pinuspollenites is also extreme - ly abundant in the Paleocene. That Palaeoperidinium pyrophorum is considered to indicate outer neritic to open-ocean palaeoenvironments is based on foramini - feral data (e.g. Gilbert F-53). This interpretation seems at odds, however, with the conclusions of several au - thors (e.g. Eshet et al. 1994; Brinkhuis et al. 1998; van Mourik et al. 2001), who postulated that high abun- dances of Palaeoperidinium (peridinioid) cysts in dicate higher nutrient levels, thus reflecting terrigenous input and a closer proximity to shore. Dale & Fjellså (1994) pointed out that the assumption that peridinioid cysts are invariably heterotrophic is not always warranted and can lead to erroneous interpretations; they also noted that modern heterotrophic dino flagellates are not re - stricted to areas of high pro ductivity. In addition, nu - trient-rich conditions can develop in various, contrasting settings including inshore areas with abundant terrige- nous input and shelf-edge settings with upwelling, so that different interpretations are en tirely possible. The Gilbert F-53 well (3200–2770 m) provides an example in which an abundance of Palaeoperidinium pyrophorum is related to an offshore setting rather than to a coastal environment. There is a marked increase in the abundance of this species from 3260 to 2740 m (excluding the interval 2860–2760 m) indicative of increasing trophic resources. Over the same interval, the gonyaulacacean ratio, which is considered to be an indicator of distance from shore, varies from 0.5 to 1.4, suggesting progressively more open-marine conditions. The foraminiferal data from this well indicate that the interval from 3200 to 2740 m represents a bathyal setting (Bujak Davies Group 1987). Miller & Helenes (1989b) interpreted the interval from 3330 to 3230 m as middle to outer neritic, and from 3230 to 2520 m as bathyal, with the interval from 2940 to 2750 m as Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 40 41 possibly outer neritic. Similarly, the dinocyst taxa re - corded from about 3250 to 2750 m indicate outer-shelf palaeoenvironments; the presence of Impagidi nium in some samples suggests open-ocean conditions (Dale 1996). During the Danian, the palaeoenvironmental setting of South Labrador N-79 was presumably similar to that of Gilbert F-53; the former well also shows high abundances of Palaeoperidinium pyrophorum in associa- tion with Impagidinium. Thus the abundance of Palaeo - peridinium pyrophorum in both wells is best explained by high nutrient levels at the shelf edge related to deep- water upwelling, conditions that are ideal for plankton whether autotrophic or heterotrophic. Several dinocyst groups proliferated during the Pa - laeogene, an example being the areoligeraceans, espe- cially the genera Areoligera and Glaphyrocysta. Species of these two genera range through parts of the Late Cre - taceous and Palaeogene, and the species Areoligera gip - pingensis and Glaphyrocysta divaricata are especially pro minent in the Paleocene. The two species are hard to distinguish – we would restrict Areoligera gippingensis to specimens with basal ridges at least partially connect- ing processes in process complexes and Glaphyrocysta divaricata to specimens lacking such ridges (see Fen - some et al. 2016). Most records in the literature under- standably just record the complex as Areoligera gip- pingensis or Areoligera spp. (although our experience on the Canadian margin is that most specimens belong to Glaphyrocysta divaricata). As noted above, we refer to the two species collectively herein as the Areoligera gip - pingensis complex. Specimens of the Areoligera gippingensis complex are among the most common dinocysts in the Paleocene of the Labrador Margin. These forms are abundant in the Danian–Selandian of South Labrador N-79 in the Hopedale Basin, in the Maastrichtian (where they are interpreted as caved) to Thanetian of Gilbert F-53, and in the Selandian–Thanetian of Gjoa G-37 and the Thanetian of Karlsefni A-13 in the Saglek Basin. In these wells, peak abundances of the complex can occur throughout the Paleocene. Similar peaks of this species complex have been observed elsewhere, with contrasting interpretations, for example on the Scotian Margin (Fensome et al. 2008), in Denmark (Heilmann-Clausen 1994) and in the type Thanetian of southern England (Powell et al. 1996). Members of the Areoligera gippingensis complex are gonyaulacaceans and thus more likely to be the cysts of autotrophic dinoflagellates. Their presence in domi- nant numbers in wells of the seaway suggests that this was in an area of high nutrient concentrations, presum- ably but not necessarily related to upwelling. If the complex gravitated towards regions of high productivi- ty, it could have occupied a coastal zone or been near to the shelf margin, as discussed earlier in relation to Pa - laeo peridinium pyrophorum. Independent studies of the intervals containing high abundances of the Areoli gera gippingensis complex in the Labrador Margin wells (Bjar ni O-82 and South Labrador N-79) infer an outer- shelf to bathyal environment (Bujak Davies Group 1987; Miller & d’Eon 1987). It is concluded that high abundances of Areoligera and Glaphyrocysta can indicate either outermost shelf or innermost shelf settings, the latter related to a transgressive regime. Accordingly such abundances must be treated with care in determining palaeoenvironments, not least since their great abun- dances would surely have guaranteed their dispersal in currents between environments. Off West Greenland, the Areoligera gippingensis complex is abundant in the predominantly outer neritic Selandian interval in the Kangâmiut-1 and Ikermiut-1 wells (Appendices 3.17 and 3.18 respectively), and present to common in the marginal marine to inner neritic Selandian interval in Hellefisk-1, Nukik-1 and Nukik-2 (Appendices 3.19, 3.15, and 3.16 respectively; Rasmussen et al. 2003). Such varied environmental interpretations may also explain the occurrence patterns of the complex on the Canadian side of the seaway. The interpretation of relatively high abundances of areoligeraceans has been mixed. Sluijs et al. (2008) argued that peridinioid dinocysts are less sensitive indi- cators of proximity to shore than gonyaulacoids; within the gonyaulacoids, these authors suggested that the most reliable indicator for the Paleocene–Eocene inter- val is the S/A index (Spiniferites/Spiniferites + Areo - ligera). Sluijs et al. (2008) argued that a high relative abundance of Areoligera (a low S/A ratio) indicated inner neritic palaeoenvironments, whereas a high re - lative abundance of Spiniferites specimens (a high S/A ratio) indicated outer neritic palaeoenvironments. There are two provisos with this approach: firstly, that Glaphyrocysta counts should be included with Areo - ligera; and secondly, that any conclusions based on this approach should, where possible, be supported by plank tonic foraminiferal data. Building on the research of Sluijs et al. (2008), Sluijs & Brinkhuis (2009) equat- ed the dominance of the Areoligera complex (presu - mably including Glaphyrocysta) with inner neritic, high-energy environments and the Spiniferites complex with neritic deposits, with relative abundances increas- ing in outer neritic palaeoenvironments (see also Brink - huis 1994 and Pross & Brinkhuis 2005). From their Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 41 42 study of Paleocene–Eocene assemblages on the New Jersey Shelf, Sluijs & Brinkhuis (2009) concluded that abundant Areoligera appears to be consistently related to third-order transgressive systems tracts, indicating ri - sing sea level in a neritic palaeoenvironment. In debates about the relationship between dinocyst assemblages and palaeoenvironment, one factor missing from the discussion may be evolutionary contingency. The striking acmes of the Areoligera gippingensis com - plex in the Paleocene, especially the Thanetian, may re - flect ideal conditions (including climate) for the pro- li feration of these species at the time of their evolution- ary appearance; under such conditions, the species spread widely, possibly as ecological generalists. The species were present still in the early Eocene, but did not dominate assemblages as they had in the Paleocene, possibly due to competition from other ‘generalists’. Thus, environmental interpretations of the Areoligera gippingensis complex may be specific to particular stages in the evolutionary development of the group, and may change with time. Open-ocean conditions persisted into the early Eo - cene, with the foraminifera indicating deep water (Gradstein & Srivastava 1980). There are some differ- ences between the palaeoenvironmental interpretations for the Eocene based on dinocysts and foraminifera: the dinocysts indicate bathyal palaeoenvironments with some neritic excursions, changing to outer to middle neritic in the Priabonian, whereas the foraminifera in - dicate more consistent bathyal palaeoenvironments changing to outer neritic in the Priabonian (Gradstein & Williams 1976). Collectively, what were the palaeoenvironmental ex - tremes during the Paleocene–Eocene in the seaway as reflected in the offshore wells? This is best illustrated by comparing the data from Gjoa G-37 (Appendix 2.6), Hekja O-71 (Appendix 2.5) and Ralegh N-18 (not illu - strated here). In Gjoa G-37, assemblages from the Paleo - cene and Eocene suggest predominantly outer neritic palaeoenvironments, with open-ocean interludes, pre - sumably denoting deeper water palaeoenvironments. In contrast, assemblages of the same age in Hekja O-71 and Ralegh N-18 suggest primarily marginal marine to inner neritic palaeoenvironments, with occasional episodes of non-marine deposition. Thus, the lowermost Eocene suc cession in Ralegh N-18 contains common specimens of the freshwater alga Pediastrum (Nøhr-Hansen 2004a) and common Taurodinium granulatum, which are as - sumed to be autochthonous. Taurodinium granulatum is also common in Hekja O-71, together with scattered specimens of Pediastrum. However, the rare specimens of these taxa in Gjoa G-37 (Nøhr-Hansen in Sønderholm et al. 2003b; Nøhr-Hansen 2004a) are inferred to have been transported into the depositional environment. Taurodinium granulatum has previously been recorded as “Gen et. sp. Indet” by Hjortkjær (1991) and Piasecki et al. (1992) from the syn-volcanic, probably lacustrine Selandian deposits at Assoq and on Disko, West Green - land, and from pre-basaltic Thanetian–?Ypresian lacus- trine deposits from the Kangerlussuaq Basin in south-eastern Greenland (Nøhr-Hansen 2012). Thus, the common occurrence of freshwater algae and lacus- trine to brackish-water dinocysts in Hekja O-71 and Ralegh N-18 suggests a position close to the Paleocene– Eocene palaeoshoreline. The contrast between the Hekja O-71 and Ralegh N-18 wells on the one hand and the Gjoa G-37 well on the other, is compatible with their relative positions within the basin (Figs 1, 2). The same pattern has also been recognised in offshore West Greenland wells. Rasmussen et al. (2003) showed that Paralecaniella indentata is common in the lower- most Thanetian and lowermost Ypresian of Hellefisk-1, Nukik-1 and Nukik-2. Nøhr-Hansen (2004a) recog- nised an acme of Paralecaniella indentata at the same stratigraphic level in Ralegh N-18. Paralecaniella ap - pears to be most abundant in marginal marine succes- sions but has a tolerance for inner neritic conditions, presumably in the vicinity of river estuaries or deltas, where there is an influx of freshwater (Elsik 1977; Powell et al. 1996). However, Lebedeva (2010) consid- ered that Paralecaniella preferred coastal, high-energy marine settings of normal salinity, with sufficient oxygen levels. An alternative explanation is that the specimens were washed in and are thus allochthonous (Rasmussen et al. 2003). The common occurrence of the freshwater alga Pediastrum at the same stratigraphic level in the outer neritic deposits in Kangâmiut-1 and Ikermiut-1 was interpreted as evidence of redeposition, probably by turbidites (Rasmussen et al. 2003). An intriguing aspect of Labrador Sea – Davis Strait palynomorph assemblages is the common occurrence of Azolla in some Ypresian samples – especially in Gjoa G-37, where it occurs with common specimens of the freshwater alga Pediastrum between 1890 and 2040 m (Nøhr-Hansen in Sønderholm et al. 2003b; Appendix 3.13). The same pattern is seen in the Ypresian of Ralegh N-18 (Appendix 3.12), but only Pediastrum is common in the Ypresian of Hekja O-71 (Appendix 3.11; Nøhr-Hansen 2004a). Azolla is a small moss-like, freshwater to brackish-water fern famous for its nitro- gen-fixing capability (van Kempen et al. 2012). Its modern distribution indicates that it prefers much Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 42 43 warmer temperatures than occur today in the La bra - dor–Baffin Seaway and suggests the possibility of exten- sive freshwater lakes. Massive concentrations of dead Azolla accumulating at the bottom of the lakes could be preserved in sediment, and given the right combination of time and temperature, may yield significant hydro- carbon source rocks. The occurrences of Azolla in La b - rador Sea – Davis Strait wells are restricted to a narrow time interval at the top of the Ypresian. Azolla has not been recorded in the offshore West Greenland wells. Brinkhuis et al. (2006) recorded numerous speci- mens of Azolla in a core from the eastern end of the Lomonosov Ridge in the Arctic Ocean; they suggested that the Ypresian records of Azolla in the Labrador– Baffin Seaway were potentially derived from natural freshwater overspill from the Arctic Ocean, which they proposed was periodically characterised by fresh surface waters. We consider it difficult, however, to visualise a body of water as large as an ocean with a surface that would be calm for long enough to allow Azolla to become established. Even if Brinkhuis et al. (2006) are correct in postulating episodic fresh surface waters in the Arctic during the Ypresian, outlets into the Atlantic Ocean would probably have been via shallow seas adja- cent to East Greenland, not via the La b rador–Baffin Seaway. This observation is based on paleogeographic maps in Monger et al. (2014) and Fen some et al. (2014; Fig. 10). Azolla occurs in wells off the Canadian margin but has not been found in any wells off West Green - land. This distribution may reflect dif ferential drainage into the seaway, such that large rivers on the Canadian side introduced Azolla into the seaway whereas rivers on the Greenland side were too small or non-existent. The palynomorph data indicate a dramatic change in palaeoenvironments from the early to the middle and late Eocene of the Labrador Margin and western Davis Strait, resulting from, or accentuated by, either a signif- icant drop in sea level or uplift. This ultimately led to inner neritic to marginal marine conditions in the Rupelian. The changes may be related to one or more of three events: the end of the drifting phase (within Anomaly 13, approximately at the Priabonian–Rupelian boundary), the development of the Antarctic Ice Sheet (Zachos et al. 2008), or global (eustatic) sea-level fall in the Oligocene (Haq et al. 1977, 1987). Throughout the rest of the Oligocene and during the Miocene to early Pliocene interval, the most useful indicator of shifting palaeo environments is the miospore/dinocyst ratio. This and other evidence indicate that inner neritic to marginal marine palaeoenvironments prevailed in the vicinity of several wells: Bjarni O-82 (Appendix 2.1), Snorri J-90 (Appendix 2.3), and South Labrador N-79 (Appendix 2.2) in the Hopedale Basin; Gilbert F-53 (Appendix 2.4), and Hekja O-71(Appendix 2.5) in the Saglek Basin (Figs 1, 2). In offshore West Greenland, palynomorphs from the Qulleq-1 well indicate that the middle Miocene succession was deposited in an open-marine palaeoenvi- ronment represented by the most diverse dinocyst assem- blages of the entire Neogene; a similar setting is indicated for the upper Miocene to lower Pliocene succession based on the common presence of Impagidinium spp. (Piasecki 2003). The peak in dinocyst species richness and abundance corresponds to the end of the middle Miocene climatic optimum (Zachos et al. 2001). N O R T H A M E R I C A 30°N 30°N LAURASIA N 85 Ma 60 Ma 35 Ma NN 30°N N O R T H A M E R I C A Fig. 10. Palaeogeography of North America for the Late Cretaceous (85 Ma), Paleocene (60 Ma) and Eocene (35 Ma), showing the evolution of the Labrador–Baffin Seaway during that timespan. According to these reconstructions, the seaway was not directly connected with the Arctic basin during the early Cenozoic, which has a major bearing on the source of the Azolla specimens found in some wells (see text for discussion). From Monger et al. (2014) and Fensome et al. (2014); maps courtesy of Ron Blakey. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 43 44 Palaeogeography, palaeoclimatology and palaeoceanography During the Cretaceous and Palaeogene, the Labrador Sea region was considerably warmer than it was during the Neogene. Evidence is sparse for the Cretaceous, with exception of the Maastrichtian. The initial findings were by Gradstein & Srivastava (1980), who recognised two principal influxes of warm-temperate plank tonic fora - minifera – during the Maastrichtian and in the early– middle Eocene. Later research drew attention to the several transient global warming or hyperthermal phases in the late Paleocene and early Eocene, especially the Paleocene–Eocene Thermal Maximum (PETM; Ken - nett & Stott 1991; Koch et al. 1992). Zachos et al. (2008) highlighted several other warm phases, including the two-million-year-long Early Eocene Climatic Op - timum at 53–51 Ma, the shorter Mid-Eocene Climatic Optimum at around 41 Ma, and the fleeting Eocene Ther mal Maximum 2 at around 52.5 Ma. Cooler epi - sodes also occurred in the Eocene, especially towards the end of the epoch, with the onset of Antarctic glaciation at 35 Ma. In the Neogene, a moderate climatic optimum occurred in the middle Miocene. Early Cretaceous dinocyst assemblages in the La b - rador Sea region are too sparse to give any clues to the climatic conditions existing there at that time. The more northerly early Late Cretaceous assemblages show some differences from those on the Scotian Margin and Grand Banks; most notable is the presence of Hetero - sphaeridium difficile, which is common in the Conia - cian section in Bjarni O-82 and South Labrador N-79 in the Hopedale Basin, in shallow cored boreholes from western Baffin Bay (MacLean et al. 2014), and in upper Turonian – lower Coniacian strata from the Umiivik-1 borehole on Svartenhuk Halvø (Dam et al.1998; Figs 1, 2). The available records (e.g. Nøhr-Hansen 1996; Dam et al.1998; Pedersen & Nøhr-Hansen 2014; Rad - macher et al. 2014) and unpublished data (G.L. Wil - liams) from Upper Cretaceous rocks of Bylot Island and Baffin Bay suggest that Heterosphaeridium difficile is a high-latitude species. The assemblages also contain many of the species described by Manum & Cookson (1964) from Graham Island, Arctic Canada, who also recorded Heterosphaeridium difficile. Similarities with other dinocyst assemblages can be determined from Lentin & Williams (1980), who de - scribed provincialism in Campanian peridinialean dino - cysts. These authors defined three assemblages, which they related to climatic belts: the Malloy or tropical– subtropical suite, the Williams or warm-temperate suite and the McIntyre or Boreal suite. Common com - ponents of the Malloy suite at generic level include Andalusiella, Cerodinium, Lejeunecysta and Sene gali - nium; the Williams suite is characterised by Alter bi - dinium, Isabelidinium, Spinidinium, Trithyrodinium, and smaller species of Chatangiella. Diagnostic taxa of the McIntyre suite are Laciniadinium and the larger taxa of Chatangiella. The McIntyre suite is present in Arctic Canada, the Mackenzie Delta, Saskatchewan, Alberta, South Dakota, Wyoming, the northern North Sea (Costa & Davey 1992) and West Greenland (Nøhr- Hansen 1996). Expanding upon the concepts of Lentin & Williams (1980), Mao & Mohr (1992) defined a Helby suite, which included diagnostic dinocyst taxa for the Campanian–Maastrichtian interval in the high- er latitudes of the Southern Hemisphere. The Helby suite is characterised by high abundances of the peridin- ioid dinocyst genera Isabelidinium, Chatangiella and Nelsoniella. As in the McIntyre suite, specimens of Cha - tan giella are large and there are few specimens of An - dalusiella and Senegalinium. Campanian assemblages on the Labrador Margin seem to fall into the Williams suite, although large Cha - tan giella specimens (characteristic of the McIntyre suite) occasionally occur. Dinocyst assemblages from the Bu - chan Gulf (Fig.1) on the north-eastern Baffin Mar gin show McIntyre-suite affinities (MacLean & Williams 1980; Balkwill et al. 1990; MacLean et al. 2014), but with some elements of the Williams suite. These occur- rences indicate that the climate in Baffin Bay during some periods of the Late Cretaceous was warm temperate. According to Gradstein & Srivastava (1980), the Cam - panian–Maastrichtian planktonic foraminifera from Nuussuaq show affinities with coeval assemblages from the North Atlantic; this is based on the common occur- rence of some poorly preserved taxa. These authors also noted, however, that Late Cretaceous climates were more equable than those of today and that species were cosmopolitan, with no specific high-latitude taxa. Ceno - manian to Maastrichtian ammonites have affinities with coeval taxa from the Western Interior Seaway of North America and the Atlantic (Birkelund 1965; Williams & Stelck 1975), thus partially paralleling the distributions shown by the dinocysts. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 44 45 Maastrichtian strata of the Labrador Margin are characterised by the presence of Palynodinium grallator and Isabelidinium cretaceum. Palynodinium grallator is a ubiquitous species but Isabelidinium cretaceum is most abundant at higher latitudes (Askin 1988; Bowman et al. 2012). In their study of Southern Ocean ODP sites from Maud Rise and the Georgia Basin, Mohr & Mao (1997) illustrated the taxon Manumiella cretacea subsp. gravida, which is similar to some of our specimens. Mohr & Mao (1997) considered Manumiella cretacea subsp. gravida to be an endemic Southern Ocean taxon and interpreted their assemblages to indicate cooler water conditions. Thus, it seems reasonable to assume the same conditions existed in the Labrador Sea at that time. A similar possible analogy between high southern and northern occurrences has been described by Nøhr- Hansen & Dam (1997) from the uppermost Maa - strichtian strata at Nuussuaq, onshore West Greenland. Here, Palynodinium grallator occurs with abundant mio spores and a peak of Manumiella sp. that is very similar to Manumiella assemblages described from Sey - mour Island, Antarctica, by Askin (1988) and which she considered were late Campanian to late Paleocene in age. Askin (1988) erected a Zone 1, characterised by Isabelidinium cretaceum and which she considered Cam panian. Isabelidinium cretaceum did not occur higher in the Seymour Island section, being replaced primarily by Manumiella species. The occurrence of Isabelidinium cretaceum in the Labrador Sea suggests a mirror-image, high-latitude Northern Hemisphere re - cord. In a recent palynological study of Seymour Island assemblages, Bowman et al. (2012) proposed a formal zonation with two late Maastrichtian zones, including two subzones, and one early Danian zone. These authors recognised Zone 1 of Askin (1988), but consid- ered the age to be ?late Maastrichtian. Bowman et al. (2012) proposed a South Polar Province for the latest Maastrichtian – earliest Palaeogene, characterised by species of Manu miella, Batiacasphaera reticulata and Tanyo sphaeridium. Again, it seems reasonable for us to consider an equivalent Northern Hemisphere province during the same time span, although this may have been somewhat warmer than its southern equivalent because of the proximity of the Arctic Ocean. An al - most monospecific assemblage of Manumiella see lan - dica was reported from Seymour Island by Askin & Jacobson (1996) and interpreted to represent marginal marine to shallow-shelf conditions; Habib & Saeedi (2007) considered Manu miella-rich assemblages to re - flect cooling during regression at the close of the Maa - strichtian. Determination of Palaeogene climates using dino - cysts has made considerable advances in recent years (Jaramillo & Oboh-Ikuenobe 1999; Sluijs et al. 2005; Sluijs et al. 2008; Sluijs & Brinkhuis 2009). We build on these earlier studies, incorporating taxa that seem to be endemic to mid- or high latitudes, as noted above and as Zonneveld et al. (2013) has shown for modern environments. In the Danian, the dinocyst Trithyro - dinium is common to abundant in the following wells: Bjarni O-82, North Leif I-05, Ogmund E-72 and South Labrador N-79 in the Hopedale Basin (Figs 1, 2); Gilbert F-53 and Skolp E-07 in the Saglek Basin (Figs 1, 2). Lentin & Williams (1980) included Tri - thyro dinium in the Williams suite for the Campanian. Nøhr-Hansen & Dam (1997) and Nøhr-Hansen et al. (2002) recorded abundant Trithyrodinium evittii pulses just above the Cretaceous–Paleocene boundary at Nuus - suaq. Smit & Brinkhuis (1996) and Nøhr-Hansen & Dam (1999) have shown that this species preferred lower latitudes in the Late Cretaceous but later migrat- ed to higher latitudes, suggesting increasing sea-surface temperatures at high latitudes in the early Danian. The abundance of Trithyrodinium in higher latitudes was confirmed by Nøhr-Hansen et al. (2002), who defined an early Danian Trithyrodinium evittii Zone for the succession in the Nuussuaq Basin, by Bowman et al. (2012), who defined an Early Danian Trithyrodinium evittii Zone for rocks on Seymour Island, and by Willumsen & Vajda (2010) in a study of New Zealand dinocyst assemblages. Gradstein & Srivastava (1980) found that the foraminifera of the Labrador Margin and Nuussuaq reflected Atlantic water-mass incursions and that these are supported by mollusc, echinoid and coral faunas on Nuussuaq. Gradstein & Srivastava (1980) considered these observations to indicate tem - perate (warmer) climatic conditions in the La brador Sea region during the Danian; such observations are in accordance with the idea that Trithyro di nium testifies to more temperate conditions in the La brador–Baffin Seaway during the Danian. One species that seems to occur consistently in high- er latitude samples is Palaeocystodinium bulliforme, first described from the Paleocene of Bylot Island by Ioan - nides (1986). In wells encountering Selandian sedi- ments, such as in Bjarni O-82 and South Labrador N-79 in the Hopedale Basin and Gilbert F-53 and Hekja O-71 in the Saglek Basin (Figs 1, 2), Palaeo - cystodinium bulliforme is common. It is also common in middle to late Danian and ?early Selandian successions in the Nuussuaq Basin (Nøhr-Hansen et al. 2002) and occurs in Danian? and Selandian sediments on Bylot Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 45 46 Island (G.L. Williams, unpublished data). Palaeo - cystodinium bulliforme is also present in Selandian strata in warmer climes farther south, being restricted to the Selandian in Morocco (H. Slimani, personal communi- cation 2015) and having its LO in the uppermost Se - landian on the Scotian Margin (Fensome et al. 2008). The variation in ranges between regions may be indica- tive of its origination in more northerly latitudes. The existence of warm climatic conditions in the Ypresian and more temperate conditions in the middle Eocene (Sluijs et al. 2008; Zachos et al. 2008; Schoon et al. 2013) had an impact on the Labrador–Baffin Sea way, as demonstrated by the presence of nannofossils recov- ered from the Kangâmiut-1 well (Sheldon 2003). Fur - ther evidence for a warm interlude is provided by the influx of the dinocyst Apectodinium homomorphum close to the Paleocene–Eocene boundary in Hekja O-71, Hellefisk-1, North Leif I-05, Ogmund E-72 and South Labrador N-79. Bujak & Brinkhuis (1998) con sidered Apectodinium homomorphum to be a warmer water spe - cies. These findings were confirmed in studies of stable isotope and biogeochemical palaeotemperature indica- tors (Sluijs et al. 2006; Zachos et al. 2006; Schoon et al. 2013). Crouch et al. (2001) showed that the earliest ap - pearance of Apectodinium-dominated as semblages seems to be synchronous on a global scale. One Apectodinium peak occurred during the Paleo cene–Eocene Thermal Maximum (PETM) at 55 Ma, which lasted for about 220 000 years. This peak can be correlated with a nega- tive carbon-isotope excursion (CIE), a benthic fora mini - fera extinction event and the calcareous nannofossil zo na tion (Crouch et al. 2001). Ac cording to these authors, the Apectodinium influx re flects higher sea- surface temperatures and a major in crease in marginal marine surface-water productivity. Based on the studies of Iakovleva et al. (2001), Crouch et al. (2003), Sluijs et al. (2008) and others, a marked decline in Apectodinium abundances towards the end of the PETM may record a corresponding temperature de crease and/or a global regression. It is generally agreed that a maximum flood- ing surface, defining the culmination of a global trans- gression, partially coincides with the PETM, although the onset of sea-level rise is thought to have predated the PETM by a few thousand years. In the Labrador–Baffin Seaway, Apecto dinium spp. are common to abundant in the uppermost Thanetian in Nukik-2 (Appendix 3.16), Kangâmiut-1 (Appendix 3.17), Ikermiut-1 (Appendix 3.18), Hekja O-71 (Appendix 3.11), Ralegh N-18 (Appendix 3.12), Gjoa G-37 (Appendix 3.13), North Leif I-05 (Ap pendix 3.1), Ogmund E-72 (Appendix 3.6) and South Labrador N-79 (Appendix 3.4). Several dinocyst taxa indicate warm-water condi- tions in the Ypresian; examples are species of Homo - tryblium, which are common in parts of the Ypresian section in the following wells: Bjarni O-82 (Appendix 3.3), North Leif I-05 (Appendix 3.1) and Snorri J-90 (Appendix 3.5) in the Hopedale Basin; Gilbert F-53 (Appendix 3.9) in the Saglek Basin; and Kangâmiut-1 (Appendix 3.17) and Nukik-1 (Appendix 3.15) in offshore West Greenland (Figs1, 2). Homotryblium is a warm-water genus commonly assumed to favour restricted settings with increased salinity, and thus char- acterising inshore, lagoonal palaeoenvironments (Brink - huis 1992, 1994; de Verteuil & Norris 1996). How ever, in a study of early Oligocene dinocyst assemblages from the Upper Rhine Graben of Germany, Pross & Schmiedl (2002) developed a model proposing different settings for what they termed the Homotryblium assemblage. They found that the Homotryblium assemblage predo - minated in nearshore palaeoenvironments where salin- ity was increased. In these palaeoenvironments, dino cyst species richness was lower. To explain these fluctua- tions, Pross & Schmiedl (2002) postulated that domi- nance of the Homotryblium assemblage was related to relatively dry periods with reduced runoff and poten- tially strong evaporation, leading to high salinity condi- tions in nearshore palaeoenvironments. Ac cor d ing to Zonneveld et al. (2013), the related modern species Polysphaeridium zoharyi occupies coastal, fully marine, subtropical to tropical regions, which may be charac- terised by high productivity and high surface-water salinities. Specimens of Homotryblium are com mon to abundant in the 1890–1930 m interval in Gjoa G-37. The presence of the freshwater fern Azolla in Hekja O- 71, Ralegh N-18 and Gjoa G-37 (Appendices 3.11 to 3.13) provides further evidence for a warm, humid climate around the Ypresian–Lutetian boundary. Counts for Homotryblium and Polysphaeridium in the Ypresian and their absence from middle Eocene and younger rocks indicate that climatic warming was fleet- ing in the Labrador Sea. Further confirmation is pro - vided by the position of the LO of Diphyes colli gerum at the Lutetian–Bartonian boundary in the La brador– Baffin Seaway. According to Brinkhuis & Biffi (1993) and Bujak & Mudge (1994) this species was tempera- ture-sensitive, preferring warmer water palaeo environ - ments, explaining its occurrence in the Ru pelian in Italy. Dinocyst species richness takes a dra matic plunge in Labrador Margin wells in the mid dle Eocene. Consequently, the numbers of species and specimens decline throughout the remainder of the Cenozoic, and the remaining taxa are either ubiquitous or higher-lati- Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 46 47 tude indicators. Much of this decline, which was prob- ably related to the general cooling trends during the transition from a Greenhouse to an Icehouse world (Zachos et al. 2001, 2008), mirrors the global decline in dinocyst species richness during the Cenozoic, as shown by MacRae et al. (1996). Dinocyst assemblages from the Eocene–Oligocene strata of ODP Site 647A in the southern Labrador Sea (Figs 1, 2) provide some clues to Palaeogene oceanic conditions. From a study of ODP assemblages, Head & Norris (1989) concluded that evidence existed for a proto-Gulf Stream in the middle Eocene. The ODP assemblages included taxa known only from the south- western Atlantic, eastern United States, Norwegian Sea, Belgium and Australia. Such a distribution could be best explained by the pattern of oceanic currents. A cooling trend in the late Eocene – Oligocene is indicat- ed by an influx of colder-water taxa, including Gelatia inflata, Svalbardella and protoperidiniaceans (Head & Norris 1989). This cooling trend in the late Eocene – early Oligocene is also a characteristic of high latitudes in the Southern Hemisphere (Guerstein et al. 2008, 2010; Houben et al. 2013) and probably reflects cool- ing conditions in the Oligocene, resulting from a reduc- tion in atmospheric pCO2, which allowed develop ment of a permanent ice sheet in Antarctica (Hren et al. 2013). The relative decline in dinocyst species richness in Labrador Margin wells is accompanied, especially in the Oligocene and Neogene, by a drop in angiosperm po l - len species richness (Williams 1986). However, conifer pollen in the Neogene, primarily Pinuspollenites, are common. General trends suggest rapid and widespread cooling for the Labrador Sea, triggered in part by fluc- tuations in oceanic-circulation patterns. At ODP Site 646, also in the Labrador Sea (Figs 1, 2), the late Miocene – early Pliocene dinocyst associations reflect predominantly temperate to cool surface waters, with Impagidinium pallidum and diverse protoperidini- aceans (Head et al. 1989a). Zonneveld et al. (2013) noted that Impagidi nium pallidum is primarily restrict- ed to higher latitudes with high concentrations in Arctic and Antarctic re gions, whereas of the two species of Protoperidinium, P. americanum is a coastal sub– polar to tropical form whereas P. monospinum is char- acteristically found in “full marine, tropical to equa - torial upwelling areas of NW Africa” (Zonneveld et al. 2013, p. 131). These observations could indicate mixing of warm-temperate and Arctic water in the Labrador Sea, with the West Greenland Current al - ready in place – a situation not dissimilar to present-day conditions. According to de Vernal & Mudie (1989a), the early Miocene assemblages at ODP Site 645 in Baffin Bay (Figs 1, 2) seem to indicate cool-temperate surface waters. De Vernal & Mudie (1989a, b) found that similar conditions persisted into the Pliocene–Pleistocene at both Site 646 and Site 647 (Figs 1, 2). There was a marked drop in species richness in the middle and late Miocene, however, accompanied by an increase in ter rigenous debris. Head et al. (1989b) related these changes to the onset of colder- water conditions and the establishment of circulation pat - terns in Baffin Bay similar to those of today. However, Dapsilidinium pa stielsii, one of the species recorded by these authors, was considered to be a warmer water species by Head & Westphal (1999), who noted that its latitudinal occurrences contracted in the late Miocene and Plio cene; they attributed this to the cooling of the North At lantic in the late Miocene and the evolution of the cold La brador Current. The persistence of Dapsilidinium pa stielsii into the middle Miocene is probably a reflection of the Mid- Miocene Climatic Optimum (Zachos et al. 2008). Piasecki (2003) concluded that the dinocyst assem- blages in Qulleq-1 on the West Greenland Margin (Figs 1, 2; Appendix 3.14) were comparable to North Atlantic assemblages, but had higher latitude elements. The Ser - ravallian samples reflected warmer water, signifying the Mid-Miocene Climatic Optimum. In contrast, the Plio - cene was marked by depleted dinocyst counts re flecting the progressively deteriorating climate. Schreck et al. (2012, 2013), in their study of the dino - cyst assemblages from an almost continuous mid dle Miocene through Pliocene section in ODP Site 907A in the Iceland Sea, recorded high marine productivity in the middle Miocene, with a diminution toward the impover- ished assemblages of the late Pliocene. We con clude that the proto-East Greenland Current was well developed by about 9 Ma. The establishment at around 4.5 Ma of the modern East Greenland Current, which would presum- ably have accelerated the influence and impact of the Labrador Current, may explain the low abundance and species richness of the dinocyst assamblages. De Vernal & Mudie (1989a) determined that the Pliocene–Pleistocene dinocysts at Site 645 (Figs 1, 2) included Boreal and cool-temperate taxa. These data suggest that the major cooling occurred relatively late in the Cenozoic history of Baffin Bay. The waning influ- ence of the Gulf Stream and the development of the Labrador Current were important events in the evolu- tion of the Labrador Sea. Based on foraminiferal data from a study of DSDP Sites 111 and 112, Poore & Berggren (1974) considered the cut-off of the Gulf Stream to have occurred in the middle–late Pliocene. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 47 48 Conclusions A new biostratigraphic framework has been developed for the Aptian (Lower Cretaceous) to Pliocene–Pleisto - cene of the Labrador–Baffin Seaway. This framework is based on 187 bioevents for taxa of dinocysts, mio - spores, fungal spores and Azolla; these define 106 bio - event horizons, mostly last occurrences, but including some local and regional peak- or common-occurrence events. Also incorporated are additional data from pre - vious studies by Piasecki (2003) and Pedersen & Nøhr- Hansen (2014). Most events are concentrated in the Cam panian to Rupelian interval. Integration of the palynological data from wells on both margins of the Seaway provides the first broad biostratigraphic correla- tion of Mesozoic–Cenozoic strata of the region. Detailed biostratigraphic evidence has confirmed the following hiatuses: pre-Aptian in the Hopedale Basin; pre-Albian in the Saglek Basin; Albian–Turonian in some wells of the Hopedale Basin; Turonian–Santo - nian/Campanian in some areas; pre-Campanian and late Campanian–Thanetian on the Greenland Margin; late Maastrichtian and Danian in some wells of the Hopedale Basin and in the Saglek Basin; Selandian in part in the Hopedale Basin, in total in the Saglek Basin and in two wells on the West Greenland Margin; late Ypresian and/or Lutetian on both sides of the seaway; Oligocene to middle Miocene of considerable variabil- ity on both margins, with all of the Oligocene and the lower Miocene missing in all the West Greenland Mar - gin wells; middle to late Miocene on the western side (Figs 7–9). On the Canadian margin, these hiatuses can be matched in part with the five recognised regional unconformities of McWhae (1981) as follows: the pre- Aptian–Albian hiatus of this study is presumed to cor - relate with the Labrador Unconformity; the Aptian/ Albian–Turonian hiatus represents the Avalon Un - conformity; the Bylot Unconformity is represented by the Maastrichtian–Selandian hiatus and the ‘base-Ter - tiary unconformity’ in the Jeanne d’Arc Basin (Sinclair 1988); the Oligocene to middle Miocene hiatus of this study may be equivalent to the Baffin Bay Uncon - formity but we regard it as resulting from the late Oligocene drop in sea level, which is not mentioned by McWhae et al. (1980); and finally the middle to late Miocene hiatus described here matches the proposed age of the Beaufort Unconformity. McWhae (1981) only recognised these five unconformities and restricted them to specific ages. This does not fully match our findings since we recognise seven significant hiatuses which furthermore are of greater duration than indicat- ed by McWhae (1981). The intra-Selandian and the Lutetian hiatuses documented here are not readily corre- lated with the regional unconformities of McWhae (1981), but may match additional seismic unconformi- ties reported by Dickie et al. (2011). On the West Greenland Margin, the hiatuses are fewer and only partly conform to those on the Canadian margin. The absence of a pre-Santonian section in part reflects the depth of the wells, since seismic data indicate that older strata are present. An apparent unconformity separating the Appat seismic sequence from the overlying Kangeq seismic sequence, probably equates with the Avalon Unconformity. The late Campanian to Selan - dian hiatus in two wells and the absence of the Danian and most or all of the Selandian in the other four wells represent the Bylot Unconformity. Thus it appears that the Bylot Unconformity is equivalent to the ‘base-Ter - tiary unconformity’ recognised by Dalhoff et al. (2003). Alternatively, following Dickie et al. (2011), the Bylot Unconformity could be restricted to the Selandian. The intra-Selandian hiatus recognised here, however, demon- strates the difficulty of identifying the Bylot Un con - formity sensu stricto. On the West Greenland margin, Dal hoff et al. (2003) also mapped a Mid Eocene Un con - formity, which we consider equivalent to our Lu tetian hiatus. In three of the wells, the overlying se di ments are middle Miocene in age. In two other wells the Bartonian is overlain by middle Miocene sediments and in one the Priabonian is overlain by middle Miocene sediments. These hiatuses could be regarded as correlating with the Baffin Bay Unconformity, but the time spans are signif- icantly greater than that recorded by McWhae (1981) on the Canadian margin, and they are likely to represent composite unconformities. Palynomorph assemblages show that most of the Ap - tian and Albian sediments on the present-day Labrador Margin were deposited in marginal marine to lagoonal palaeoenvironments, punctuated by a shallow marine episode in the Aptian. A marine transgression starting in the Cenomanian–Turonian led to the most offshore, presumably deepest water palaeoenvironments in the Campanian – late Maastrichian, although this conclusion seems to conflict with the hiatus between the Cre taceous and Cenozoic sediments in many wells, espe cially on the West Greenland Margin. However, the Cretaceous–Pa - Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 48 49 laeo gene boundary and upper Maastrichtian and Da n - ian–Selandian strata occur in the Nuussuaq Basin (Nøhr- Hansen & Dam 1997; Dam et al. 2009). Outer neritic to open-ocean conditions persisted throughout the Paleocene and Ypresian and into the Lutetian, an interval corresponding to a time of sea-floor spreading in the Labrador–Baffin Seaway. The onset of shallowing, prob- ably in the late Lutetian, continued through the Pria - bonian and into the Rupelian, when marginal marine to inner neritic palaeoenvironments predominated. Throug h out the rest of the Oligocene and in the Neogene, inner neritic palaeoenvironments alternated with marginal marine conditions. Dinocysts indicate that climatic conditions in the Labrador–Baffin Seaway region, which had been rela- tively temperate in the Cretaceous, varied dramatically in the Cenozoic. The Palaeogene was a time of increas- ingly warmer climate, a thermal maximum being reached around the Paleocene–Eocene boundary, reflecting the global thermal event at this time. Warm to hot condi- tions prevailed throughout the Ypresian, but began to cool in the Lutetian and cooling accelerated in the Pria - bonian and Rupelian, a trend observed globally (Zachos et al. 2008). Temperatures generally declined through- out the Neogene, reaching a low in the Pleistocene. Acknowledgements During the gestation of this paper of over a decade, we have had the unwavering support of our two institutions, the Geological Survey of Denmark and Greenland (GEUS) and the Geological Survey of Canada (Atlantic), (GSCA), part of the Earth Sciences Sector (ESS) of Natural Resources Canada. We are also grateful for fruit- ful discussions with and feedback from Kate Dickie of GSCA, Lotte M. Larsen, Gunver K. Pedersen and Martin Sønderholm of GEUS, and Stefan Piasecki of the Geological Museum, Natural History Mu seum of Denmark, University of Copenhagen. We are grateful to Lynn Dafoe and Christop her Harrison for incisive reviews of an earlier draft that led to important improve- ments of the manuscript. We thank the two bulletin referees, Raquel Guerstein and Gregers Dam for their very valuable com ments and suggestions. We also thank Bernie Cri lley and Bill MacMillan (both GSC) and Annette Ryge and Dorthe Salomonsen (both GEUS) for processing samples; Nelly Koziel (GSC) for technical support; and Lynn Dafoe (GSC) for collecting and providing con ventional core samples. This paper is ESS Contribution number 20150377. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 49 50 References Ainsworth, N.R., Riley, L.A., Bailey, H.W. & Gueinn, K.J. 2014: Cretaceous – Tertiary stratigraphy of the Labrador Shelf, 56 pp. Riley Geoscience Ltd. Andrews, J.T., Wray, J.L., Guennel, G.K. & Ives, J.D. 1972: An early Tertiary outcrop in north-central Baffin Island, Northwest Territories, Canada: environment and significance. Canadian Journal of Earth Sciences 9 (3), 233–238. Askin, R.A. 1988: Campanian to Paleocene palynological succes- sion of Seymour and adjacent islands, northeastern Antarctic Peninsula. In: Feldmann, R.M. & Woodburne, M.O. (eds): Geology and paleontology of Seymour Island, Antarctic Penin sula. Geological Society of America Memoir 169, 131– 153. Askin, R.A. & Jacobson, S.R. 1996: Palynological change across the Cretaceous–Tertiary boundary on Seymour Island, Antarctica: environmental and depositional factors, 7–25. In: MacLeod, N. & Keller, G. (eds): The Cretaceous–Tertiary boundary mass ex - tinctions: biotic and environmental changes. New York: W.W. Norton & Co. Balkwill, H.R. & McMillan, N.J. 1990: Mesozoic–Cenozoic geol- ogy of the Labrador Shelf (Chapter 7, Part 1). In: Keen, M.J. & Williams, G.L. (eds): Geology of the Continental Margin of Eastern Canada. Geological Survey of Canada, Geology of Canada 2, 295–324 (also Geological Society of America, The Geology of North America I-1). Balkwill, H.R., McMillan, N.J., MacLean, B., Williams, G.L. & Srivastava, S.P. 1990: Chapter 7. Geology of the Labrador Shelf, Baffin Bay, and Davis Strait. Chapter 7. In: Keen, M.J. & Wil - liams, G.L. (eds): Geology of the continental margin of eastern Canada. Geological Survey of Canada, Geology of Canada 2, 293–348 (also Geological Society of America, The Geology of North America I-1). Banerjee, I. & Davies, E.H. 1988: An integrated lithostratigraphic and palynostratigraphic study of the Ostracode Zone and adja- cent strata in the Edmonton embayment, central Alberta. In: James, D.P. & Leckie, D.A. (eds): Sequences, Stratigraphy, Sedi - mentology: Surface and Subsurface. Canadian Society of Petro - leum Geologists Memoir 15, 261–274. Barke, J. et al. 2012: Coeval Eocene blooms of the freshwater fern Azolla in and around Arctic and Nordic seas. Palaeogeography, Palaeoclimatology, Palaeoecology 337–338, 108–119. Barss, M.S. & Williams, G.L. 1973: Palynology and nannofossil processing techniques. Geological Survey of Canada Paper 73– 26, 25 pp. Barss, M.S., Bujak, J.P. & Williams, G.L. 1979: Palynological zona- tion and correlation of sixty-seven wells, eastern Canada. Geo - logical Survey of Canada Paper 78–24, 118 pp. Bell, J.S. (co-ordinator) 1989: East Coast Basin Atlas Series: Lab rador Sea. Atlantic Geoscience Centre, Geological Survey of Canada, Bed - ford Institute of Oceanography, Dartmouth, Nova Scotia, 112 pp. Benedek, P.N. 1972: Phytoplanktonten aus dem Mittel- und Oberoligozän von Tönisberg (Niederrheingebiet). Palaeonto gra - phica Abteilung B, 137, 1–71. Bint, A.N. 1986: Fossil ceratiaceae: a restudy and new taxa from the mid-Cretaceous of the western interior, USA. Palynology 10(1), 135–180. Birkelund, T. 1965: Ammonites from the Upper Cretaceous of West Greenland. Bulletin Grønlands Geologiske Undersøgelse 56, 192 pp. (also Meddelelser om Grønland 179(7), 192 pp.) Bowman, V.E., Francis, J.E., Riding, J.B., Hunter, S.J. & Hay - wood, A.M. 2012: A latest Cretaceous to earliest Paleogene dinfoagellate cyst zonation from Antarctica, and implications for phytoprovincialism in the high latitudes. Review of Palaeobo - tany and Palynology 171, 40–56. Braman, D.R. 2013: Triprojectate pollen occurrence in the Western Canada Sedimentary Basin and the group’s global rela- tionships. Royal Tyrrell Museum of Palaeontology, Contri bu - tion Series 1, 538 pp. Brinkhuis, H. 1992: Late Eocene to early Oligocene dinoflagellate cysts from central and northeast Italy, 169 pp. Unpublished PhD thesis, University of Utrecht, The Netherlands. Brinkhuis, H. 1994: Late Eocene to early Oligocene dinoflagellate cysts from the Priabonian type-area (northeast Italy) – biostrati - graphy and paleoenvironmental interpretation. Palaeogeo gra - phy, Palaeoclimatology, Palaeoecology 107(1–2), 121–163. Brinkhuis, H. & Biffi, U. 1993: Dinoflagellate cyst stratigraphy of the Eocene–Oligocene transition in central Italy. Marine Micro - paleontology 22, 131–183. Brinkhuis, H., Bujak, J.P., Smit, J., Versteegh, G.J.M. & Visscher, H. 1998: Dinoflagellate-based sea surface temperature recon- structions across the Cretaceous–Tertiary boundary. Palaeogeo - graphy, Palaeoclimatology, Palaeoecology 141, 67–83. Brinkhuis, H., Sengers, S., Sluijs, A., Warnaar, J. & Williams, G.L. 2003: Latest Cretaceous– earliest Oligocene and Qua - ternary dinoflagellate cysts, ODP Site 1172, East Tasman Plateau. In: Exon, N.F., Kennett, J.P. & Malone, M.J. (eds): Ocean Drilling Program Proceedings, Scientific Results 189, 1–48. Brinkhuis, H. et al. 2006: Episodic fresh surface waters in the early Eocene Arctic Ocean. Nature 441(7093), 606–609. Bujak, J.P. 1994: New dinocyst taxa from the Eocene of the North Sea. Journal of Micropalaeontology 13, 119–131. Bujak, J.P. & Brinkhuis, H. 1998: Global warming and dinocyst changes across the Paleocene/Eocene epoch boundary. In: Au - bry, M.-P. et al. (eds): Late Paleocene–early Eocene climatic and biotic events in the marine and terrestrial records, 277–295. New York: Columbia University Press. Bujak, J. & Mudge, D. 1994: A high-resolution North Sea Eocene dinocyst zonation. Journal of the Geological Society (London) 151, 449–462. Bujak Davies Group 1987: Biostratigraphy and maturation of 17 Labrador and Baffin Shelf wells. Volume 1: Scope, methodology, Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 50 51 format and recommendations. Geological Survey of Canada Open File Report 1929, 95 pp. Burden, E. & Langille, A.B. 1990: Stratigraphy and sedimentology of Cretaceous and Paleocene strata in half-grabens on the south- east coast of Baffin Island, Northwest Territories. Bulletin of Canadian Petroleum Geology 38(2), 185–196. Burden, E.T. & Langille, A.B. 1991: Palynology of Cretaceous and Tertiary strata, northeast Baffin Island, Northwest Territories, Canada: implications for the history of rifting in Baffin Bay. Palynology 15, 91–114. Chalmers, J.A. 1991: New evidence on the structure of the Labra - dor Sea/Greenland continental margin. Journal of the Geolo gi - cal Society (London) 148, 899–908. Chalmers, J.A. & Laursen, K.H. 1995: Labrador Sea: the extent of continental crust and the timing of the start of sea-floor spread- ing. Marine and Petroleum Geology 12, 205–217. Chalmers, J. & Pulvertaft, T. 2001: Development of the continen- tal margins of the Labrador Sea: a review. In: Wilson, R.C.L. et al. (eds): Non-volcanic rifting of continental margins: a compar- ison of evidence from land and sea. Geological Society Special Publications (London) 187, 77–105. Chalmers, J.A., Pulvertaft, T.C.R., Christiansen, F.G., Larsen, H.C., Laursen, K.H. & Ottesen, T.G. 1993: The southern West Greenland continental margin: rifting history, basin develop- ment and petroleum potential, 915–931. In: Parker, J.R. (ed.): Petroleum geology of Northwest Europe: Proceedings of the 4th conference. Geological Society (London). Chalmers, J.A., Dahl-Jensen, T., Bate, K.J. & Whittaker, R.C. 1995: Geology and petroleum prospectivity of the region off - shore southern West Greenland – a summary. Rapport Grøn - lands Geologiske Undersøgelse 165, 13–21. Christiansen, F.G. et al. 1999: Petroleum geological activities in West Greenland in 1998. Geology of Greenland Survey Bulletin 183, 46–56. Christiansen, F.G. et al. 2001: Petroleum geological activities in West Greenland in 2000. Geology of Greenland Survey Bulletin 189, 24–33. Clarke, D.B. & Upton, B.G.J. 1971: Tertiary basalts of Baffin Island: field relations and tectonic setting. Canadian Journal of Earth Sciences 8, 248–258. Corgnet, J.L. & McWhae, J.R.H. 1973: Well history report Eastcan et al. Bjarni H-81. (Released 14 October 1975). Calgary: East - can Exploration Ltd. Costa, L.I. & Davey, R.J. 1992: Dinoflagellate cysts of the Cre - taceous System. In: Powell, A.J. (ed.): A stratigraphic index of dino flagellate cysts, 99–131. London: British Micropalae on to - log ical Society Special Publication. Costa, L.I. & Downie, C. 1979: The Wetzeliellaceae; Palaeogene dino flagellates. In: Proceedings of the 4th International Palyno - lo gical Conference, Lucknow (1976–1977) 2, 34–46. Crouch, E.M., Heilmann-Clausen, C., Brinkhuis, H., Morgans, H.E.G., Rogers, K.M., Egger, H. & Schmitz, B. 2001: Global dinoflagellate event associated with the late Paleocene thermal maximum. Geology 29(4), 315–318. Crouch, E.M., Dickens, G.R., Brinkhuis, H., Aubry, M-P., Hollis, C.J., Rogers, K.M. & Visscher, H. 2003: The Apectodinium acme and terrestrial discharge during the Paleocene–Eocene thermal maximum: new palynological, geochemical and calcareous nanno- plankton observations at Tawanui, New Zealand. Palaeo geo - graphy, Palaeoclimatology, Palaeoecology 194, 387–403. Crux, J.A. & Gard, G. 2004: Nannofossil Biostratigraphy of the wells Gilbert F-53 and Skolp E-07 from the Labrador Shelf, 10 pp. Unpublished report for Geological Survey of Canada (Atlantic). Dale, B. 1996: Dinoflagellate cyst ecology: modelling and geological applications. In: Jansonius, J. & McGregor, D.C. (eds): Paly no - logy: principles and applications 3, 1249–1275. Dallas: American Association of Stratigraphic Palynologists Foundation. Dale, B. & Fjellså, A. 1994: Dinoflagellate cysts as paleoproductivity indicators: State of the art, potential and limits, 521–537. In: Zahn, R. et al. (eds.): Carbon cycling in the Glacial Ocean: Con - straints on the ocean’s role in global change. Berlin: Springer. Dalhoff, F., Chalmers, J.A., Gregersen, U., Nøhr-Hansen, H., Ras - mussen, J.A. & Sheldon, E. 2003: Mapping and facies analysis of Paleocene–mid-Eocene seismic sequences, offshore southern West Greenland. Marine and Petroleum Geology 20, 935–986. Dalhoff, F., Larsen, L.M., Ineson, J.R., Stouge, S., Bojesen- Koefoed, J.A., Lassen, S., Kuijpers, A., Rasmussen, J.A. & Nøhr- Hansen, H. 2006: Continental crust in the Davis Strait: new evidence from seabed sampling. Geological Survey of Denmark and Greenland Bulletin 10, 33–36. Dam, G., Larsen, M. & Sønderholm, M. 1998a: Sedimentary response to mantle plumes: implications from Paleocene on shore successions, West and East Greenland. Geology 26(3), 207–210. Dam, G., Nøhr-Hansen, H., Christiansen, F.G., Bojesen-Kofoed, J.A. & Laier, T. 1998b: The oldest marine Cretaceous sediments in West Greenland (Umiivik-1 borehole) – record of the Ceno - manian–Turonian Anoxic Event? Geology of Greenland Survey Bulletin 180, 128–137. Dam, G., Nøhr-Hansen, H. & Kennedy, W.J. 1998c: The north- ernmost marine Cretaceous–Tertiary boundary section; Nuus - suaq, West Greenland. Geology of Greenland Survey Bulletin 180, 138–144. Dam, G., Nøhr-Hansen, H., Pedersen, G.K. & Sønderholm, M. 2000: Sedimentary and structural evidence of a new early Cam - panian rift phase in the Nuussuaq Basin, West Greenland. Cretaceous Research 21, 127–154. Dam, G., Pedersen, G.K., Sønderholm, M., Midtgaard, H., Larsen, L.M., Nøhr-Hansen, H. & Pedersen, A.K. 2009: Lithostrati - graphy of the Cretaceous–Paleocene Nuussuaq Group, Nuus - suaq Basin, West Greenland. Geological Survey of Denmark and Greenland Bulletin 19, 171 pp. Deptuck, M.E., MacRae, R.A., Shimeld, J.W., Williams, G.L. & Fensome, R.A. 2003: Revised Upper Cretaceous and lower Pale - o gene lithostratigraphy and depositional history of the Jeanne d’Arc Basin, offshore Newfoundland, Canada. American Asso - ciation of Petroleum Geologists Bulletin 87, 1459–1483. de Vernal, A.M. & Mudie, P.J. 1989a: Late Pliocene to Holocene palynostratigraphy at ODP Site 645, Baffin Bay. In: Srivastava, S.P. et al. (eds): Ocean Drilling Program Proceedings, Scientific Results 105, 387–397. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 51 52 de Vernal, A. & Mudie, P.J. 1989b: Pliocene and Pleistocene paly- nostratigraphy at the ODP Sites 646 and 647, eastern and south- ern Labrador Sea. In: Srivastava, S.P. et al. (eds): Ocean Drilling Program Proceedings, Scientific Results 105, 401–422. de Verteuil, L. & Norris, G. 1996: Middle to upper Miocene Geonettia clineae, an opportunistic coastal embayment dinoflagellate of the Homotryblium complex. Micropaleontology 42, 263–284. Dickie, K., Keen, C.E., Williams, G.L. & Dehler, S.A. 2011: Tec - tonostratigraphic evolution of the Labrador margin, Atlantic Canada. Marine & Petroleum Geology 28,1663–1675. Dolby, G., Demchuk, T.D. & Suter, J.R. 2013: The significance of palynofloral assemblages from the Lower Cretaceous McMurray Formation and associated strata, Surmont and surrounding areas in north-central Alberta. In: Hein, F.J. et al. (eds). Heavy-oil and oil-sand petroleum systems in Alberta and beyond: AAPG Studies in Geology 64, 251–272. Dörhöfer, G. 1977: Palynologie und Stratigraphie der Bückeberg- Formation (Berriasium–Valanginium) in der Hilsmulde (NW- Deutschland). Geologisches Jahrbuch, A42, 122 pp. Downie, C., Hussain, M.A. & Williams, G.L. 1971: Dinoflagellate cyst and acritarch associations in the Paleogene of southeast England. Geoscience and Man 3, 29–35. Duxbury, S. 2001: A palynological zonation scheme for the Lower Cretaceous – United Kingdom Sector, central North Sea. Neues Jahrbuch für Geologie und Paläontologie 219, 95–137. Eldrett, J.S., Harding, I.C., Firth, J.V. & Roberts, A.P. 2004: Magnetostratigraphic calibration of Eocene–Oligocene dinofla- gellate cyst biostratigraphy from the Norwegian–Greenland Sea. Marine Geology 204, 91–127. Elsik, W.C. 1977: Contributions of stratigraphic palynology (with emphasis on North America), Cenozoic palynology. American Association of Stratigraphic Palynologists Contribution Series 5a, 169 pp. Eshet, Y., Almogi-Labin, A. & Bein, A. 1994: Dinoflagellate cysts, paleoproductivity and upwelling systems: a Late Cretaceous example from Israel. Marine Micropaleontol 23, 231–240. Felix, C.J. & Burbridge, P.P. 1976: Age of microplankton studied by Manum and Cookson from Graham and Ellef Ringnes Islands. Geoscience and Man 15, 83–86. Fensome, R.A. 2015: Palynological analysis of two Labrador Shelf wells: Petro Canada et al. Rut H-11 and Eastcan et al. Karlsefni A- 13. Geological Survey of Canada Open Report File 7738, 21 pp. Fensome, R.A. & Williams, G.L. 2005: Scotian Margin PalyAtlas, Version 1. Geological Survey of Canada Open File Report 4677, 180 pp. http://ftp.maps.canada.ca/pub/nrcan_rncan/publications /ess_sst/221/221057/of_4677.zip Fensome, R.A., Williams, G.L., Barss, M.S., Freeman, J.M. & Hill, J.M. 1990: Acritarchs and fossil prasinophytes: an index to genera, species and infraspecific taxa. American Association of Stratigraphic Palynologists Contributions Series 25, 771 pp. Fensome, R.A., Guerstein, G.R. & Williams, G.L. 2007: New insights on the Paleogene Dinoflagellate cyst genera Enneado - cysta and Licracysta gen. nov. based on material from offshore eastern Canada and southern Argentina. Micropalaeontology 52(5), 385–410. Fensome, R.A., Crux, J.A., Gard, I.G., MacRae, R.A., Williams, G.L., Thomas, F.C., Fiorini, F. & Wach, G. 2008: The last 100 million years on the Scotian Margin, offshore eastern Canada: an event-stratigraphic scheme emphasizing biostratigraphic data. Atlantic Geology 44, 93–126. Fensome, R.A., Williams, G.L. & MacRae, R.A. 2009: Late Cretaceous and Cenozoic fossil dinoflagellates and other paly- nomorphs from the Scotian Margin, offshore eastern Canada. Journal of Systematic Palaeontology 7(1), 1–79. Fensome, R.A. et al. 2014: Final approach: Canada 65.5 million years ago. Chapter 10. In: Fensome, R.A. et al. (eds): Four billion years and counting: Canada’s geological heri tage, 192‒215. Canadian Federation of Earth Sciences and Nimbus Publishing (Halifax). Fensome, R.A., Nøhr-Hansen, H. & Williams, G.L. 2016: Cre - taceous and Cenozoic dinoflagellate cysts and other palyno - morphs from the western and eastern margins of the La bra- dor–Baffin Seaway. Geological Survey of Denmark and Greenland Bulletin 36, 143 pp. Firth, J.V. 1996: Upper middle Eocene to Oligocene dinoflagellate biostratigraphy and assemblage variations in Hole 913B, Green - land Sea. In: Thiede, J. et al. (eds): Ocean Drilling Pro gram Proceedings, Scientific Results 151, 203–242. Funck, T., Jackson, H.R., Louden, K.E. & Klingelhöfer, F. 2007: Seismic study of the transform rifted margin in Davis Strait between Baffin Island (Canada) and Greenland: what happens when a plume meets a transform. Journal of Geophysical Re - search, 112 (B04402), http://dx.doi.org/10.1029/2006JB00 4308 Funck, T., Gohl, K., Damm, V. & Heyde, I. 2012: Tectonic evolu- tion of southern Baffin Bay and Davis Strait: Results from a seis- mic refraction transect between Canada and Greenland, Journal of Geophy sical Research-Solid Earth, 117 (B04107), http://dx.doi.org/10.1029/2011JB009110 Gocht, H. 1969: Formengemeinschaften alttertiären Mikroplank - tons aus Bohrproben des Erdölfeldes Meckelfeld bei Hamburg. Palaeontographica, Abt. B 126, l–100. Gradstein, F.M. 1978: Labrador Shelf foraminiferal stratigraphy I – supplement; Eastcan et al. Karlsefni A-13, Labrador Shelf. Re - port No. EPGS-PAL.12-78FMG, 2 pp. Gradstein, F.M. & Agterberg, F.P. 1982: Models of Cenozoic foraminiferal stratigraphy, northwestern Atlantic Margin, 119– 173. In: Cubitt, J.M. & Rayment, R.A. (eds): Quantitative stratigraphic correlation. Chichester: Wiley. Gradstein, F.M. & Srivastava, S.P. 1980: Aspects of Cenozoic stratigraphy and paleoceanography of the Labrador Sea and Baffin Bay. Palaeogeography, Palaeoclimatology, Palaeoecology 30(3–4), 261–295. Gradstein, F.M. & Williams, G.L. 1976: Biostratigraphy of the Labrador Shelf. Geological Survey of Canada Open File Report 349, 39 pp. Gradstein, F.M. & Williams, G.L. 1981: Sediment ages based on foraminifera and palynomorphs of 9 exploration wells, Labrador Shelf. Geological Survey of Canada Open File Report 826, 5 pp. Gradstein, F.M., Kaminski, M.A., Berggren, W.A., Kristiansen, I.L. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 52 53 & D’Ioro, M.A. 1994: Cenozoic biostratigraphy of the North Sea and Labrador Shelf. Micropaleontology 40, Sup plement 1–152. Gradstein, F.M., Ogg, J.G. & Smith, A.G. (eds) 2005: A geologic time scale 2004. Cambridge University Press, Cambridge, 610 pp. Gradstein, F.M., Ogg, J.G., Schmitz, M.D. & Ogg, G.M. 2012 (eds): The geologic time scale 2012. Elsevier, 1176 pp. Grant, A.C. 1975: Geophysical results from the continental margin off southern Baffin Island. In: Yorath, C.J., Parker, E.R. & Glass, D.J. (eds): Canada’s continental margins and offshore petroleum exploration. Canadian Society of Petroleum Geo - logists Memoir 4, 411–431. Grant, A.C. 1980: Problems with plate tectonics: the Labrador Sea. Bulletin of Canadian Petroleum Geology 28, 252–278. Gregersen, U., Hopper, J.R. & Knutz, P.C. 2013: Basin seismic stratigraphy and aspects of prospectivity in the NE Baffin Bay, Northwest Greenland. Marine and Petroleum Geology 46, 1–18. Guerstein, G.R., Guler, M.V., Williams, G.L., Fensome, R.A. & Chiesa, J.O. 2008: Middle Palaeogene dinflagellate cysts from Tierra del Fuego, Argentina: biostratigraphy and palaeoenviron- ments. Journal of Micropalaeontology 27, 75–94. Guerstein, G.R., Guler, M.V., Brinkhuis, H. & Warnaar, J. 2010: Mid Cenozoic palaeoclimatic and palaeoceanographic trends in the Southwest Altantic Basins: a dinoflagellate view, 394–409. In: Madden, R.H. et al. (eds): The Paleontology of Gran Barranca: evolution and environmental change through the mid dle Ceno - zoic of Patagonia. Cambridge: Cambridge University Press. Habib, D. & Saeedi, F. 2007: The Manumiella seelandica global spike: cooling during regression at the close of the Maastrichtian. Palaeogeography, Palaeoclimatology, Palaeoecology 255, 87–97. Hald, N. 1976: Early Tertiary flood basalts from Hareøen and west- ern Nûgssuaq, West Greenland. Grønlands Geologiske Under - søgelse Bulletin 120, 36 pp. Hansen, J.M. & Gudmundsson, L. 1978: A method for separation of acid insoluble microfossils from organic debris. Micro pale - ontology 25, 113–117. Haq, B.U. & Al-Qahtani, A.M. 2005: Phanerozoic cycles of sea- level change on the Arabian platform. GeoArabia 10(2), 127– 160. Haq, B.U., Premoli-Silva, I. & Lohmann, G.P. 1977: Calcareous plankton paleo-biogeographic evidence for major climatic fluc- tuations in early Cenozoic Atlantic Ocean. Journal of Geo phy - sical Research, Oceans and Atmospheres 82(27), 3861–3876. Haq, B.U., Hardenbol, J., & Vail, P.R. 1987: Chronology of fluc- tuating sea levels since the Triassic (250 million years ago to present). Science 235, 1156–1167. Harding, I.C. 1990: Palaeoperidinium cretaceum: A brackish-water perdiniinean dinoflagellate from the Early Cretaceous. Palae on - tology 33(1), 35–48. Harland, R. 1973: Dinoflagellate cysts and acritarchs from the Bearpaw Formation (Upper Campanian) of southern Alberta, Canada. Palaeontology 16(4), 665–706. Harrison, J.C., Mayr, U., McNeil, D.H., Sweet, A.R., McIntyre, D.J., Eberle, J.J., Harington, C.R., Chalmers, J.A., Dam, G. & Nøhr-Hansen, H. 1999: Correlation of Cenozoic sequences of the Canadian Arctic region and Greenland; implications for the tectonic history of northern North America. Bulletin of Cana - dian Petroleum Geology 47(3), 223–254. Harrison, J.C., Brent, T.A. & Oakey, G.N. 2011: Baffin Fan and its inverted rift system of arctic eastern Canada; stratigraphy, tectonics and petroleum resource potential. In: Spencer, A.M. et al. (eds): Arctic Petroleum Geology. Geological Society, Lon - don, Memoirs 35, 595–626. Head, M.J. 2000: Geonettia waltonensis, a new Goniodomacean dinoflagellate from the Pliocene of the North Atlantic region, and its evolutionary implications. Journal of Paleontology 74(5), 812–827. Head, M.J. & Norris, G. 1989: Palynology and dinocyst stratigra- phy of the Eocene and Oligocene in ODP Leg 105, Hole 647A, Labrador Sea. In: Srivastava, S.P. et al. (eds): Ocean Drilling Program Proceedings, Scientific Results 105, 515–550. Head, M.J. & Westphal, H. 1999: Palynology and paleoenviron- ments of a Pliocene carbonate platform: the Clino core, Baha - mas. Journal of Paleontology 73(1), 1–25. Head, M.J., Norris, G. & Mudie, P.J. 1989a: Palynology and dinocyst stratigraphy of the Miocene in ODP Leg 105, Hole 645E, Baffin Bay. In: Srivastava, S.P. et al. (eds): Ocean Drilling Program Proceedings, Scientific Results 105, 467–514. Head, M.J., Norris, G. & Mudie, P.J. 1989b: Palynology and dinocyst stratigraphy of the upper Miocene and lowermost Plio - cene, ODP Leg 105, Site 646, Labrador Sea. In: Srivastava, S.P. et al. (eds): Ocean Drilling Program Proceedings, Scientific Results 105, 423–451. Heilmann-Clausen, C. 1985: Dinoflagellate stratigraphy of the upper- most Danian to Ypresian in the Viborg 1 borehole, central Jylland, Denmark. Danmarks Geologiske Undersøgelse Serie A 7, 69 pp. Heilmann-Clausen, C. 1994: Review of Paleocene dinoflagellates from the North Sea region. GFF 116, 51–53. Stockholm: Geological Society of Sweden. Henderson, G., Rosenkrantz, A. & Schiener, E.J. 1976: Cretace - ous–Tertiary sedimentary rocks of West Greenland, 341–362. In: Escher, A. & Watt, W.S. (eds): Geology of Greenland. Copen hagen: Geological Survey of Greenland. Henriksen, N., Higgins, A.K., Kalsbeek, F. & Pulvertaft, T.C.R. 2009: Greenland from Archaean to Quaternary. Descriptive text to the 1995 geological map of Greenland 1:2  500  000. 2nd edtion. Geological Survey of Denmark and Greenland, Bulletin 18, 126 pp. Hjortkjær, B.F. 1991: Palynologisk undersøgelse af tertiære skifre fra Disko of Nûgssuaq, Vestgrønland, 94 pp. Unpublished MSc thesis, Københavns Universitet, Danmark. Houben, A.J.P. et al. 2013: Reorganization of Southern Ocean plankton ecosystem at the onset of Antarctic glaciation. Science 340(6130), 341–344. Hren, M.T., Sheldon, N.D., Grimes, S.T., Collinson, M.E., Hooker, J.J., Bugler, M. & Lohmann, K.C. 2013: Terrestrial cooling in Northern Europe during the Eocene–Oligocene tran- sition. Proceedings of the National Academy of Sciences of the United States of America 110(19), 7562–7567. Iakovleva, A.I., Brinkhuis, H. & Cavagnetto, C. 2001: Late Palaeocene–Early Eocene dinoflagellate cysts from the Turgay Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 53 54 Strait, Kazakhstan; correlations across ancient seaways. Palaeo - geo graphy, Palaeoclimatology, Palaeoecology 172, 243–268. Ioakim, C. 1979: Étude comparative des dinoflagellés du Tertiaire Inférieur de la Mer du Labrador et de la Mer Nord, 204 pp. Unpublished PhD thesis, Université Pierre-et-Marie-Curie, Paris, France. Ioannides, N.S. 1986: Dinoflagellate cysts from Upper Cretaceous– lower Tertiary sections, Bylot and Devon Islands, Arctic Archi - pe lago. Geological Survey of Canada Bulletin 371, 1–99. Islam, M.A. 1983: Dinoflagellate cyst taxonomy and biostratigra- phy of the Eocene Bracklesham Group in southern England. Micro paleontology 29, 328–353. Jackson, G.D., Iannelli, T.R., Narbonne, G.M., & Wallace, P.J. 1978: Upper Proterozoic sedimentary and volcanic rocks of northwestern Baffin Island. Geological Survey of Canada Paper 78–14, 1–15. Jackson, H.R., Keen, C.E., Falconer, R.K.H. & Appleton, K.P. 1979: New geophysical evidence for sea-floor spreading in central Baffin Bay. Canadian Journal of Earth Sciences 16(11), 2122–2135. Jansonius, J. & Hills, L.V. 1976: Genera file of fossil spores and pollen. 3287 filing cards. Special Publication, Department of Geology, University of Calgary, Canada. Jaramillo, C.A. & Oboh-Ikuenobe, F.E. 1999: Sequence strati- graphic interpretations from palynofacies, dinocyst and litholo - gical data of Upper Eocene – Lower Oligocene strata in southern Mississippi and Alabama, US Gulf Coast. Palaeogeography, Pa - lae o climatology, Palaeoecology 145, 259–302. Kaminski, M.A., Gradstein, F.M., Scott, D.B. & MacKinnon, K.D. 1989: 37. Neogene benthic foraminifer biostratigraphy and deep-water history of sites 645, 646 and 647, Baffin Bay and Labrador Sea. In: Srivastava, S.P. et al. (eds): Ocean Drilling Program Proceedings, Scientific Results 105, 731–756. Keen, M.J., Johnson, J. & Park, I. 1972: Geophysical and geological studies in eastern and northern Baffin Bay and Lancaster Sound. Canadian Journal of Earth Sciences 9(6), 689–708. Kennedy, W.J., Nøhr-Hansen, H. & Dam, G.1999: The youngest Maastrichtian ammonite faunas from Nuussuaq, West Green - land. Geology of Greenland Survey Bulletin 184, 13–17. Kennett, J.P. & Stott, L.D. 1991: Abrupt deep-sea warming, palaeoceanographic changes and benthic extinctions at the end of the Palaeocene. Nature 353, 225–229. Kerr, J.W. 1967: A submerged continental remnant beneath the Labrador Sea. Earth and Planetary Science Letters 2(4), 283– 289. King, A.F. & McMillan, N.J. 1975: A Mid-Mesozoic breccia from the coast of Labrador. Canadian Journal of Earth Sciences 12(1), 44–51. Klose, G.W., Maltere, E., McMillan, N.J. & Zinkan, C.G. 1982: Petroleum exploration offshore southern Baffin Island, northern Labrador Sea, Canada. In: Embry, A.F. & Balkwill, H.R. (eds): Arctic Geology and Geophysics. Canadian Society of Petroleum Geologists, Memoir 8, 233–244. Knutsen, S.M., Arendt, N.P., Runge, M.K., Stilling, J. & Brandt, M.P. 2012: Structural provinces offshore West Greenland and key geological variations influencing play assessment. First Break 30(12), 43‒55. Koch, P.L., Zachos, J.C. & Gingerich, P.D. 1992: Correlation between isotope records in marine and continental carbon reser- voirs near the Palaeocene–Eocene boundary. Nature 358, 319– 322. Koppelhus, E.B. & Pedersen, G.K. 1993: A palynological and sedi- mentological study of Cretaceous floodplain deposits of the Atane Formation at Skansen and Igdlunguaq, Disko, West Green - land. Cretaceous Research 14, 707–734. Köthe, A. 1990: Paleogene dinoflagellates from northwest Germany – biostratigraphy and paleoenvironment. Geologisches Jahrbuch Reihe A 118, 3–111. Lanstorp, J. 1999: En palynologisk undersøgelse af kretassiske og paleocæne sedimenter fra det sydøstlige Nuussuaq, Vest grøn - land. Geologisk Tidsskrift 1999/1, 13–20. Larsen, L.M. 2006: Mesozoic to Palaeogene dyke swarms in West Greenland and their significance for the formation of the Labra - dor Sea and the Davis Strait. Danmarks og Grønlands Geo - logiske Undersøgelse Rapport 2006/34, 118 pp. Larsen, L.M., Heaman, L.M., Creaser, R.A., Duncan, R.A., Frei, R. & Hutchison, M. 2009: Tectonomagmatic events during stret - ching and basin formation in the Labrador Sea and the Davis Strait: evidence from age and composition of Mesozoic to Palaeogene dyke swarms in West Greenland. Journal of the Geological Society (London) 166, 999–1012. Larsen, L.M., Pedersen, A.K., Tegner, C., Duncan, R.A., Hald, N. & Larsen, J.G. 2016: Age of Tertiary volcanic rocks on the West Greenland continental margin: volcanic evolution and event correlation to other parts of the North Atlantic Igneous Province. Geological Magazine 153(03), 487–511, http://dx.doi.org/ 10.1017/S0016756815000515 Le Pichon, X., Hyndman, R.D. & Pautot, G. 1971: Geophysical study of the opening of the Labrador Sea. Journal of Geophysical Research 76, 4724–4734. Lebedeva, N.K. 2010: Palynofacies in Upper Cretaceous sediments of Northern Siberia. Stratigrafiya Geologicheskaya Korrelyastiya 18(5), 70–87. [Original in Russian] English version: 18, 532– 549. Leckie, D.A. & Singh, C. 1991: Estuarine deposits of the Albian Paddy Member (Peace River Formation) and lowermost Shaftes - bury Formation, Alberta, Canada. Journal of Sedimentary Pe - tro logy 61(5), 825–849. Lentin, J.K. & Williams, G.L. 1980: Dinoflagellate provincialism with emphasis on Campanian peridiniaceans. American Asso - ciation of Stratigraphic Palynologists Contribution Series 7, 1–47. McIntyre, D.J. 1975: Morphologic changes in Deflandrea from a Campanian section, District of Mackenzie, N.W.T., Canada. Geoscience and Man 11, 61–76. MacLean, B. & Williams, G.L. 1980: Upper Cretaceous rocks in Baffin Bay. Geological and Mineralogical Association of Canada Annual Meeting Halifax, Abstract, 69 only. MacLean, B. & Williams, G.L. 1983: Geological investigations of Baffin Island Shelf in 1982. In: Current research, part B, Geological Survey of Canada Paper 83-1B, 309–315. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 54 55 MacLean, B., Williams, G.L., Jennings, A. & Blakeney, C. 1986: Bedrock and surficial geology of Cumberland Sound, Northwest Territories. In: Current research, part B, Geological Survey of Canada, Paper 86-1B, 605–615. MacLean, B., Williams, G.L. & Zhang, S. 2014: New insights into the stratigraphy and petroleum potential of the Baffin shelf’s Cretaceous rocks. Bulletin of Canadian Petroleum Geology 62(4), 289–310. MacRae, R.A., Fensome, R.A. & Williams, G.L. 1996: Fossil dinoflagellate diversity, originations, and extinctions and their significance. Canadian Journal of Botany 74(11), 1687–1694. McWhae, J.R.H. 1981: Structure and spreading history of the northwestern Arctic region from the Scotian Shelf to Baffin Bay. In: Kerr, J.W. & Fergusson, A.J. (eds): Geology of the North Atlantic Borderlands. Canadian Society of Petroleum Geologists Memoir 7, 299–332. McWhae, J.R.H., Elie, R., Laughton, D.C. & Gunther, P.R. 1980: Stratigraphy and petroleum prospects of the Labrador Shelf. Bulletin of Canadian Petroleum Geology 28(4), 460–488. Manum, S.B. & Cookson, I.C. 1964: Cretaceous microplankton in a sample from Graham Island, Arctic Canada, collected during the second ‘Fram’ expedition (1898–1902). With notes on microplankton from the Hassel Formation, Ellef Ringnes Island. Skrifter utgitt av Det Norske Videnskaps-Akademi i Oslo, i. Matematisk-Naturvidenskapelig Klasse 17, 1–36. Mao, S. & Mohr, B.A.R. 1992: Late Cretaceous dinoflagellate cysts (?Santonian–Maastrichtian) from the southern Indian Ocean (Hole 748C). Ocean Drilling Program Proceedings, Scientific Results 120, 307–341. Mao, S., Chunbiao, W. & Xiayun Q. 1999: Cretaceous non-marine dinoflagellates from northeast China. Grana 38(2–3), 144–161. Mertens, K.N., Takano, Y., Head, M.J. & Matsuoka, K. 2014: Living fossils in the Indo-Pacific warm pool: a refuge for thermophilic dinoflagellates during glaciations. Geology 42(6), 531–534. Miall, A.D. 1986: The Eureka Sound Group (Upper Cretaceous– Oligocene), Canadian Arctic Islands. Bulletin of Canadian Pe - tro leum Geology 34(2), 240–270. Miall, A.D., Balkwill, H.R. & Hopkins, W.S., Jr. 1980: Cretaceous and Tertiary sediments of Eclipse Trough, Bylot Island area, Arctic Canada, and their regional setting. Geological Survey of Canada Paper 79-23, 20 pp. Michoux, D. 1988: Dinoflagellate cysts of the Wetzeliella-complex from Eocene sediments of the Aquitaine Basin, southwestern France. Palynology 12, 11–41. Miller, P.E. & d’Eon, G.J. 1987: Labrador Shelf – Paleoen viron - ments. Geological Survey of Canada, Open File Report 1722, 186 pp. Miller, P.E. & Helenes, J. 1989a: Paleogeography, I, Labrador Sea, Early to middle Albian and Turonian to Santonian palaeoenvi- ronments, 78–79. In: Bell, J.S. (co-ordinator): East Coast Basin Atlas Series. Labrador Sea. Geological Survey of Canada, Bed - ford Institute of Oceanography. Dartmouth, Nova Scotia: At - lantic Geoscience Centre. Miller, P.E. & Helenes, J. 1989b: Paleogeography, II Labrador Sea, Maastrichtian and early Paleocene palaeoenvironments, 80–81. In: Bell, J.S. (co-ordinator): East Coast Basin Atlas Series. Labrador Sea. Geological Survey of Canada, Bedford Institute of Oceanography, Dartmouth, Nova Scotia: Atlantic Geoscience Centre. Miller, P.E. & Helenes, J. 1989c: Paleogeography, III, Labrador Sea, Earliest early Eocene middle Eocene palaeoenvironments, 82–83. In: Bell, J.S. (co-ordinator): East Coast Basin Atlas Series. Labrador Sea. Geological Survey of Canada, Bedford In - sti tute of Oceanography. Dartmouth, Nova Scotia: Atlantic Geoscience Centre. Mohr, B.A.R. & Mao, S. 1997: Maastrichtian dinocyst flora from Maud Rise and Georgia Basin (Southern Ocean): their stratigra - phic and paleoenvironmental implications. Palynology 21, 41–65. Monger, J. et al. 2014: Pangea Breaks Up and Mountains Rise: Canada 251 to 65.5 Million Years Ago. Chapter 9, 160‒188. In: Fensome, R. et al. (eds): Four billion years and counting: Ca - nada’s geological heritage. Halifax: Canadian Federation of Geo - logical Sciences Nimbus Publishing. Morgenroth, P. 1966: Neue in organischer Substanz erhaltene Mikrofossilien des Oligozäns. Neues Jahrbuch für Geologie und Paläontologie, Abhandlungen, 127, 1–12. Mudge, D.C. & Bujak, J.P. 1996: Palaeocene biostratigraphy and sequence stratigraphy of the UK central North Sea. Marine and Petroleum Geology 13(3), 295–312. Mudge, D.C. & Bujak, J.P. 2001: Biostratigraphic evidence for evolving palaeoenvironment in the lower Paleogene of the Fae roe– Shetland Basin. Marine and Petroleum Geology 18, 577–590. Nøhr-Hansen, H. 1992: Cretaceous marine and brackish (?) dino - flagellate cysts, West Greenland. 8th International Palynological Congress, Aix-en-Provence, 6–12 September, 1992. Abstract, 107 only. Nøhr-Hansen, H. 1993a: Upper Maastrichtian? – lower Paleocene dinoflagellate cysts and pollen from turbidites in the Itilli region, Nuussuaq, central West Greenland – first dating of sediments. Grønlands Geologiske Undersøgelse Rapport 159, 81–87. Nøhr-Hansen, H. 1993b: Dinoflagellate cyst stratigraphy of the Barremian to Albian, Lower Cretaceous, North-East Greenland. Grønlands Geologiske Undersøgelse Bulletin 166, 171 pp. Nøhr-Hansen, H. 1996: Upper Cretaceous dinoflagellate cyst stratigraphy, onshore West Greenland. Grønlands Geologiske Undersøgelse Bulletin 170, 104 pp. Nøhr-Hansen, H. 1997a: Palynology of the Umiivik-1 borehole, Svartenhuk Halvø, West Greenland. Danmarks og Grønlands Geologiske Undersøgelse Rapport 1997/32, 15 pp. Nøhr-Hansen, H. 1997b: Palynology of the boreholes GANE#1, GANK#1 and GANT#1, Nuussuaq, West Greenland. Dan marks og Grønlands Geologiske Undersøgelse Rapport 1997/89, 22 pp. Nøhr-Hansen, H. 1997c: Palynology of the GRO#3 well, Nuus - suaq, West Greenland. Danmarks og Grønlands Geolo giske Undersøgelse Rapport 1997/151, 19 pp. Nøhr-Hansen, H. 2003: Dinoflagellate cyst stratigraphy of the Palaeogene strata from the wells Hellefisk-1, Ikermiut-1, Kangâ - miut-1, Nukik-1, Nukik-2 and Qulleq-1 wells, offshore West Greenland. Marine and Petroleum Geology 20, 987–1016. Nøhr-Hansen, H. 2004a: Dinoflagellate cyst stratigraphy of the Ralegh N-18 well, Saglek Basin, Davis Strait, offshore eastern Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 55 56 Canada. Danmarks og Grønlands Geologiske Undersøgelse Rapport 2004/34, 67 pp. Nøhr-Hansen, H. 2004b: Dinoflagellate cyst stratigraphy of the North Leif I-05 well, Hopedale Basin, Labrador Shelf, offshore eastern Canada. Danmarks og Grønlands Geologiske Under - søgelse Rapport 2004/109, 117 pp. Nøhr-Hansen, H. 2008: Morphological variability within brackish water to marginal marine dinoflagellate cyst assemblages from mid-Cretaceous, West Greenland. DINO8 – 8th International conference on modern and fossil dinoflagellates, Montreal, Ca - nada, 4–10 May, 2008. GEOTOP- UQAM, Canada. Abstract volume, 41–42. Nøhr-Hansen, H. 2012: Palynostratigraphy of the Cretaceous– lower Palaeogene sedimentary succession in the Kangerlussuaq Basin, southern East Greenland. Review of Palaeobotany and Palynology 178, 59–90. Nøhr-Hansen, H. & Dam, G. 1997: Palynology and sedimentology across a new marine Cretaceous–Tertiary boundary section on Nuussuaq, West Greenland. Geology 25, 851–854. Nøhr-Hansen, H. & Dam, G. 1999: Trithyrodinium evittii Drugg 1967 and T. fragile Davey 1969 an artificially split [sic] of one dinoflagellate cyst species – stratigraphic and palaeoenvironmen- tal importance. Grana 38(2–3), 125–133. Nøhr-Hansen, H. & Heilmann-Clausen, C. 2000: Cerodinium kangiliense sp. nov. and Senegalinium iterlaaense sp. nov. – two new, stratigraphically important Paleocene species from West Greenland and Denmark. Neues Jahrbuch für Geologie und Paläontologie. Abhandlungen 219, 153–170. Nøhr-Hansen, H. & McIntyre, D.J. 1998: Upper Barremian to Upper Albian (Lower Cretaceous) dinoflagellate cyst assem- blages, Canadian Arctic Archipelago. Palynology 22, 143–166. Nøhr-Hansen, H., Piasecki, S., Rasmussen, J.A. & Sheldon, E. 2000: Biostratigraphy of well 6354/4-1 (Qulleq-1), West Green - land. Danmarks og Grønlands Geologiske Undersøgelse Rap - port 2000/101, 81 pp. Nøhr-Hansen, H., Sheldon, E. & Dam, G. 2002: A new biostrati- graphic scheme for the Paleocene onshore West Greenland and its implications for the timing of the pre-volcanic evolution. In: Jolley, D.W. & Bell, B.R. (eds): The North Atlantic igneous province: stratigraphy, tectonic, volcanic and magmatic processes. Geological Society Special Publications (London) 197, 111–156. Oakey, G.N. 2005: Cenozoic evolution and lithosphere dynamics of the Baffin Bay-Nares Strait region of Arctic Canada and Greenland, 233 pp. Unpublished PhD thesis, Vrije Universiteit, Amsterdam,The Netherlands. Oakey, G.N. & Chalmers, J.A. 2012: A new model for the Paleogene motion of Greenland relative to North America: plate reconstruc- tions of the Davis Strait and Nares Strait regions between Canada and Greenland. Journal of Geophysical Research, 117, 28 pp., http://dx.doi.org/10.1029/ 2011JB008942 Parsons, M.G. & Norris, G. 1999: Paleogene fungi from the Caribou Hills, Mackenzie Delta, northern Canada. Palaeonto - graphica Abteilung B 250, 77–167. Pedersen, A.K., Larsen, L.M., Riisager, P. & Dueholm, K.S. 2002: Rates of volcanic deposition, facies changes and movements in a dynamic basin: the Nuussuaq Basin, West Greenland, around the C27n-C26r transition. In: Jolley, D.W. & Bell, B.R. (eds): The North Atlantic Igneous Province: Stratigraphy, tectonic, volcanic and magmatic processes. Geological Society Special Publications (London) 197, 157–181. Pedersen, G.K. & Nøhr-Hansen, H. 2014: Sedimentary successions and palynoevent stratigraphy from the non-marine Lower Cretaceous to the marine Upper Cretaceous of the Nuussuaq Basin, West Greenland. Bulletin of Canadian Petroleum Geo - logy 62(4), 216–244. Pedersen, G.K. & Pulvertaft, T.C.R. 1992: The nonmarine Cre - taceous of the West Greenland Basin, onshore West Green land. Cretaceous Research 13, 263–272. Pedersen, G.K., Schovsbo, N.H. & Nøhr-Hansen, H. 2013: Calibration of spectral gamma-ray logs to deltaic sedimentary facies from the Cretaceous Atane Formation, Nuussuaq Basin, West Greenland. Geological Survey of Denmark and Greenland Bulletin 28, 61–64. Piasecki, P. 2003: Neogene dinoflagellate cysts from Davis Strait, offshore West Greenland. Marine and Petroleum Geology 20, 1075–1088. Piasecki, S., Larsen, L.M., Pedersen, A.K. & Pedersen, G.K. 1992: Palynostratigraphy of the lower Tertiary volcanics and marine clastic sediments in the southern part of the West Greenland Basin: implications for the timing and duration of the volcan- ism. Rapport Grønlands Geologiske Undersøgelse 154, 13–31. Pierce, R.L. 1961: Lower Upper Cretaceous plant microfossils from Minnesota. Minnesota Geological Survey Bulletin 42, 86 pp. Poore, R.Z. & Berggren, W.A. 1974: Pliocene biostratigraphy of the Labrador Sea: calcareous plankton. Journal of Foraminiferal Research 4(3), 91–108. Powell, A.J. (ed.) 1992: A Stratigraphic index of dinoflagellate cysts, 290 pp. British Micropalaeontological Society publication series. London, New York: Chapman and Hall. Powell, A.J., Brinkhuis, H. & Bujak, J.P. 1996: Upper Paleocene – lower Eocene dinoflagellate cyst sequence biostratigraphy of southeast England. In: Knox, R.W.O.B. et al. (eds): Correlation of the early Paleogene in Northwest Europe. Geological Society Special Publications (London) 101, 145–183. Pross, J. & Brinkhuis, H. 2005: Organic-walled dinoflagellate cysts as paleoenvironmental indicators in the Paleogene; a synopsis of concepts. Paläontologische Zeitschrift 79, 53–59. Pross, J. & Schmiedl, G. 2002: Early Oligocene dinoflagellate cysts from the northern Rhine Graben (SW Germany): paleoenviron- mental and paleoclimatic implications. Marine Micropaleon to - logy 45, 1–24. Radmacher, W., Tyszka, J. & Mangerud, G. 2014: Distribution and biostratigraphical significance of Heterosphaeridium bellii sp. nov. and other Late Cretaceous dinflagellate cysts from the south western Barents Sea. Review of Palaeobotany and Palynology 201, 29–40. Rasmussen, J.A. & Sheldon, E. 2003: Microfossil biostratigraphy of the Palaeogene succession in the Davis Strait, offshore West Greenland. Marine and Petroleum Geology 20, 1017–1030. Rasmussen, J.A., Nøhr-Hansen, H. & Sheldon, E. 2003: Palaeoe - cology and palaeoenvironments of the lower Palaeogene succes- Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 56 57 sion, offshore West Greenland. Marine and Petroleum Geology 20, 1043–1073. Ricketts, B.D. 1986: New formations in the Eureka Sound Group, Canadian Arctic Islands. Current Research, Part B. Geological Survey of Canada Paper 86-1B, 363–374. Roest, W.R. & Srivastava, S.P. 1989: Sea-floor spreading in the Labrador sea: a new reconstruction. Geology 17(11), 1000–1003. Rolle, F. 1985: Late Cretaceous–Tertiary sediments offshore central West Greenland: lithostratigraphy, sedimentary evolution, and petroleum potential. Canadian Journal of Earth Sciences 22, 1001–1019. Rossignol, M. 1962: Analyse pollinique de sédiments marins quaternaires en Israël II. Sédiments pleistocènes. Pollen et Spores 4(1), 121–148. Schoon, P.L., Heilmann-Clausen, C., Pagh Schultz, B., Sluijs, A., Sinninghe Damsté, J.S. & Schouten, S. 2013: Recognition of early Eocene global carbon isotope excursions using lipids of marine Thaumarchaeota. Earth & Planetary Science Letters 373, 160–168. Schreck, M., Matthiessen, J. & Head, M.J. 2012: A magnetostrati- graphic calibration of Middle Miocene through Pliocene dino - flagellate cyst and acritarch events in the Iceland Sea (Ocean Drilling Program Hole 907A). Review of Palaeobotany and Pa - ly nology 187, 66–94. Schreck, M., Meheust, M., Stein, R. & Matthiessen, J. 2013: Response of marine palynomorphs to Neogene climate cooling in the Iceland Sea (Ocean Drilling Program Hole 907A). Marine Micropaleontology 101, 49–67. Sheldon, E. 2003: Palaeogene nannofossil biostratigraphy of the Kangâmiut-1 and Nukik-2 wells, offshore West Greenland. Marine and Petroleum Geology 20(9), 1031–1041. Sinclair, I.K. 1988: Evolution of Mesozoic–Cenozoic sedimentary basins in the Grand Banks area of Newfoundland and compari- son with Falvey’s (1974) rift model. Bulletin of Canadian Pe - troleum Geology 36(3), 255–273. Singh, C. 1971: Lower Cretaceous microfloras of the Peace River area, northwestern Alberta. Research Council of Alberta Bulletin 28, 301–542. Singh, C. 1983: Cenomanian microfloras of the Peace River area, north- western Alberta. Research Council of Alberta Bulletin 44, 322 pp. Sluijs A. & Brinkhuis, H. 2009: A dynamic climate and ecosystem state during the Paleocene–Eocene Thermal Maximum: infer- ences from dinoflagellate cyst assemblages on the New Jersey Shelf. Biogeosciences 6, 1755–1781. Sluijs, A., Brinkhuis, H., Stickley, C.E., Warnaar, J., Williams, G.L. & Fuller, M. 2003: Dinoflagellate cysts from the Eocene–Oligocene transition in the Southern Ocean; results from ODP Leg 189. In: Exon, N.F., Kennett, J.P. & Malone, M. (eds): Ocean Drilling Program Proceedings, Scientific Results 189, 1–42. Sluijs, A., Pross, J. & Brinkhuis, H. 2005: From greenhouse to icehouse; organic-walled dinoflagellate cysts as paleoenviron- mental indicators in the Paleogene. Earth-Science Reviews 68(3–4), 281–315. Sluijs, A. et al. 2006: Subtropical Arctic Ocean temperatures during the Palaeocene–Eocene thermal maximum. Nature 441, 610–613. Sluijs, A. et al. 2008: Eustatic variations during the Paleocene– Eocene greenhouse world. Paleoceanography 23(4), 17 pp. PA4216, http://dx.doi.org/10.1029/2008PA001615 Smit, J. & Brinkhuis, H. 1996: The Geulhemmerberg Cretaceous– Tertiary boundary section (Maastrichtian type area, SE Nether - lands); summary of results and a scenario of events. Geologie en Mijnbouw 75(2–3), 283–293. Sønderholm, M., Christiansen, F.G., Olsen, J.C., Planke, S., Bojesen-Koefoed, J.A., Dalhoff, F., Nielsen, T., Myklebust, R. & Nøhr-Hansen, H. 2003a: Early rifting of the Labrador Sea and Baffin Bay: new evidence from seismic, well and sea-bed data. American Association of Petroleum Geologists Interna - tional Conference and Exhibition, Barcelona, Spain. Pro gram - me with abstracts, A90. Sønderholm, M., Nøhr-Hansen, H., Bojesen-Koefoed, J.A., Dalhoff, F. & Rasmussen, J.A. 2003b: Regional correlation of Mesozoic–Palaeogene sequences across the Greenland–Canada boundary. Danmarks og Grønlands Geologiske Undersøgelse Rapport 2003/25, 175 pp. Sørensen, A.B. 2006: Stratigraphy, structure and petroleum poten- tial of the Lady Franklin and Maniitsoq basins, offshore south- ern West Greenland. Petroleum Geoscience 12(3), 221–234. Sparkes, K.E. 1989: Stratigraphy and terrestrial palynology of Late Cretaceous Eclipse Group strata, Bylot Island, Northwest Ter - ritories, Canada. Unpublished MSc thesis, Memorial University of Newfoundland, St. Johns, Newfoundland and Labrador, 195 pp. Srivastava, S.P. 1978: Evolution of Labrador Sea and its bearing on early evolution of the North Atlantic. Geophysical Journal of the Royal Astronomical Society 52(2), 313–357. Srivastava, S.P. & Roest, W.R. 1999: Extent of oceanic crust in the Labrador Sea. Marine and Petroleum Geology 16, 65–84. Srivastava, S.P., Arthur, M., Clement, B. et al. 1987: Site 645. Ocean Drilling Program Proceedings, Initial Reports 105, 61–418. Storey, M., Duncan, R.A., Pedersen, A.K., Larsen, L.M. & Larsen, H.C. 1998: 40Ar/39Ar geochronology of the West Greenland Tertiary Volcanic Province. Earth and Planetary Science Letters 160, 569–586. Stover, L.E. et al. 1996: Chapter 19. Mesozoic–Tertiary dinoflagel- lates, acritarchs and prasinophytes. In: Jansonius, J. & Mc Gregor, D.C. (eds): Palynology: principles and applications. Volume 2, 641–750. American Association of Stratigraphic Palynologists Foundation, Dallas. Tozer, E.T. 1963: Mesozoic and Tertiary stratigraphy. In: Fortier, Y.O. et al. (eds): Geology of the North-Central Part of the Arctic Archipelago, Northwest Territories (Operation Franklin). Geological Survey of Canada Memoir 320, 74–95. Troelsen, J.C. 1950: Contributions to the geology of Northwest Greenland, Ellesmere Island and Axel Heiberg Island. Meddelelser om Grønland 149(7), 86 pp. Umpleby, D.C. 1979: Geology of the Labrador Shelf. Geological Survey of Canada Paper 79–13, 34 pp. van Bemmelen, R.W. 1949: The geology of Indonesia. 1A. General geology of Indonesia and adjacent archipelagoes, 732 pp. The Hague Government Printing Office. van Bemmelen, R.W. 1972: Geodynamic models. An evaluation Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 57 58 and synthesis. Developments in Geotectonics 2, 267 pp. Am - ster dam: Elsevier. van Kampen, M.M.L., Smolders, A.J.P., Lamers, L.P.M. & Roe - lofs, J.G.M. 2012: Micro-halocline enabled nutrient recycling may explain extreme Azolla event in the Eocene Arctic Ocean. Plos One 7, 1–6. van Mourik, C.A., Brinkhuis, H. & Williams, G.L. 2001: Mid- to late Eocene organic-walled dinoflagellate cysts from ODP Leg 171B, offshore Florida. In: Kroon, D. Norris, R.D. & Klaus, A. (eds): Western North Atlantic Palaeogene and Cretaceous Palae - oceanography. Geological Society Special Publications (Lon - don) 183, 225–252. Wall, D., Dale, B., Lohmann, G.P. & Smith, W.K. 1977: The envi- ronmental and climatic distribution of dinoflagellate cysts in modern marine sediments from regions in the North and South Atlantic oceans and adjacent areas. Marine Micropaleontology 2, 121–200. Waterfield, J.J. 1989: Stratigraphy, sedimentology and palynology of Cretaceous and Tertiary strata, southwest Bylot Island, Northwest Territories, Canada, 260 pp. Unpublished MSc thesis, Memorial University of Newfoundland, St. John’s, Newfoundland and Labrador. Wightman, D.M., Pemberton, S.G. & Singh, C. 1987: Deposi - tional modelling of the Upper Manville (Lower Cretaceous), east central Alberta: implications for the recognition of brackish water deposits. In: Tillman, R.W. & Weber, K.J. (eds): Reser - voir Sedimentology. Society of Economic Paleontologists and Mineralogists Special Publication 40, 189–220. Williams, G.D. & Stelck, C.R. 1975: Speculations on the Cre - taceous palaeogeography of North America. In: Caldwell, W.G.E. (ed.): The Cretaceous System in the Western Interior of North America. Geological Association of Canada Special Paper 13, 1–20. Williams, G.L. 1975: Dinoflagellate and spore stratigraphy of the Mesozoic–Cenozoic, offshore eastern Canada. In: van der Lin - den, W.J.M. & Wade, J.A. (eds): Offshore Geology of Eastern Canada 2 – Regional Geology. Geological Survey of Canada Paper 74-30, 107–161. Williams, G.L. 2003a: Palynological analysis of Amoco-Imperial- Skelly Skua E-41, Carson Basin, Grand Banks of Newfound land. Geological Survey of Canada Open File Report 1658, 21 pp. Williams, G.L. 2003b: Palynological analysis of Petro-Canada et al. Terra Nova K-18, Jeanne d’Arc Basin, Grand Banks of New - foundland. Geologial Survey of Canada Open File Report 1659, 19 pp. Williams, G.L. 2007a: Palynological analysis of Total Eastcan et al. Bjarni O-82, Hopedale Basin, Labrador Shelf. Geological Sur - vey of Canada Open File Report 5439, 19 pp. (1 sheet.) Williams, G.L. 2007b: Palynological analysis of Chevron et al. South Labrador N-79, Hopedale Basin, Labrador Basin. Geo logical Survey of Canada Open File Report 5446, 26 pp. (1 sheet.) Williams, G.L. 2007c: Palynological analysis of Eastcan et al. Snorri J-90, Hopedale Basin, Labrador Shelf. Geological Survey of Canada Open File Report 5447, 20 pp. (1 sheet.) Williams, G.L. 2007d: Palynological analysis of Aquitaine et al. Hekja O-71, Saglek Basin, Davis Strait, Geological Survey of Canada Open File Report 5448, 18 pp. (1 sheet.) Williams, G.L. 2007e: Palynological analysis of Esso-H.B. Gjoa G- 37, Saglek Basin, Davis Strait. Geological Survey of Canada Open File Report 5449, 15 pp. (1 sheet.) Williams, G.L. 2007f: Palynological analysis of Total Eastcan et al. Gilbert F-53, Saglek Basin, Labrador Shelf. Geological Survey of Canada Open File Report 5450, 22 pp. (1 sheet.) Williams, G.L. & Brideaux, W.W. 1975: Palynological analyses of upper Mesozoic and Cenozoic Rocks of the Grand Banks, Atlantic Continental Margin. Geological Survey of Canada Bulletin 236, 163 pp. Williams, G.L. & Bujak, J.P. 1977: Cenozoic palynostratigraphy of offshore eastern Canada. American Association of Stratigraphic Palynologists Contribution Series 5A, 14–47. Williams, G.L., Ascoli, P., Barss, M.S., Bujak, J.P., Davies, E.H., Fensome, R.A. & Williamson, M.A. 1990: Biostratigraphy and related studies. Chapter 3. In: Keen, M.J. & Williams, G.L. (eds): Geology of the continental margin off eastern Canada. Geology of Canada 2, 87–137. Williams, G.L., Bujak, J.P., Brinkhuis, H., Fensome, R.A. & Weegink, J.W. 1999: Mesozoic–Cenozoic dinoflagellate cyst course, Urbino, Italy, May 17–22, 1999. (Unpublished short course manual.) Williams, G.L., Brinkhuis, H., Pearce, M.A., Fensome, R.A. & Weegink, J.W. 2004: Southern Ocean and global dinoflagellate cyst events compared: index events for the Late Cretaceous– Neogene. In: Exon, N.F. et al. (eds): Ocean Drilling Program Proceedings, Scientific Results 189, 1–98. Williams, G.L., Damassa, S.P., Fensome, R.A. & Guerstein, G.R. 2015: Wetzeliella and its allies – the ‘hole’ story: a taxonomic revision of the Paleogene dinoflagellate subfamily Wetzeliel - loideae. Palynology 39(3), 289–344, http://dx.doi.org/10.1080/ 01916122.2014.993888 Williams, V.E. 1986: Palynological studies of the continental shelf sediments of the Labrador Sea, 210 pp. Unpublished PhD the - sis, University of British Columbia, Vancouver, Canada. Williamson, M.C., Villeneuve, M.E., Larsen, L.M., Jackson, H.R., Oakey, G.N. & Maclean, B. 2001: Age and petrology of off - shore basalts from the southeast Baffin Island Shelf, Davis Strait and the Western Greenland continental margin. GAC/ MAC Annual Meeting. St. John’s, Newfoundland, Canada, 27–30 May. Geological Association of Canada & Mineralogical Asso - ciation of Canada Abstracts 26, 162 only. Willumsen, P.S. & Vajda, V. 2010: A new early Paleocene dinofla- gellate cyst species, Trithyrodinium partridgei: its biostratigraphic significance and palaeoecology. Alcheringa: An Australian Jour - nal of Palaeontology 34(4) 523–538. Zachos, J., Pagani, M., Sloan, L., Thomas, E. & Billups, K. 2001: Trends, rhythms, and aberrations in global climate 65 Ma to present. Science 292(5517), 686–693. Zachos, J.C., Schouten, S., Bohaty, S., Quattlebaum, T., Sluijs, A., Brinkhuis, H., Gibbs, S.J. & Bralower, T.J. 2006: Extreme warming of mid-latitude coastal ocean during the Paleocene– Eocene Thermal Maximum: inferences from TEX86 and isotope data. Geology 34(9), 737–740. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 58 59 Zachos, J.C., Dickens, G.R. & Zeebe, R.C. 2008: An early Ceno - zoic perspective on greenhouse warming and carbon-cycle dyna - mics. Nature 451, 279–283. Zippi, P. 1998: Freshwater algae from the Mattagami Formation (Albian), Ontario: paleoecology, botanical affinities, and syste - matic taxonomy. Micropaleontology 44, supplement 1, 78 pp. Zonneveld, K.A.F. et al. 2013: Atlas of modern dinoflagellate cyst distribution based on 2405 data points. Review of Palaeobotany and Palynology 191, 1–197. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 59 60 Names of taxa used in text with authorships References are not included in the current reference list (unless otherwise used in text) but can be found as follows: Citations are listed as they are given in these sources. Hence the order of references from the same author(s) in the same year (e.g. Eisenack 1954b in the first dinocyst below) follows that given in these sources and thus may not match that given in the companion taxonomic bulletin (Fensome et al. 2016) which has its own internally consistent reference list. Dinocysts Achilleodinium biformoides (Eisenack 1954b) Eaton 1976 Achomosphaera Evitt 1963 Achomosphaera grallaeformis (Brosius 1963) Davey & Williams 1969 Alisocysta circumtabulata (Drugg 1967) Stover & Evitt 1978 Alisocysta margarita (Harland 1979a) Harland 1979a Alterbidinium (Lentin & Williams 1985) Fensome et al. 2016 * Alterbidinium acutulum (Wilson 1967b) Lentin & Williams 1985 Alterbidinium biaperturum (McIntyre 1975) Fensome et al. 2016 * Alterbidinium? bicellulum (Islam 1983b) Lentin & Williams 1985 Alterbidinium ioannidesii Pearce 2010 Alterbidinium varium Kirsch 1991 Andalusiella Riegel 1974 Apectodinium (Costa & Downie 1976) Lentin & Williams 1977b Apectodinium homomorphum (Deflandre & Cookson 1955) Lentin & Williams 1977b Apectodinium hyperacanthum (Cookson & Eisenack 1965b) Lentin & Williams 1977b Apectodinium parvum (Alberti 1961, p. 8–9) Lentin & Williams 1977b Apteodinium australiense (Deflandre & Cookson 1955) Williams 1978 Apteodinium spiridoides Benedek 1972 Areoligera Lejeune-Carpentier 1938a Areoligera gippingensis Jolley 1992 Areoligera semicirculata (Morgenroth 1966b) Stover & Evitt 1978 (now Licracysta semicirculata) Areosphaeridium Eaton 1971 Areosphaeridium diktyoplokum (Klumpp 1953) Eaton 1971 Arvalidinium scheii (Manum 1963) Lentin & Vozzhennikova 1990 Appendix 1 ^ # † > †† ** ^^ * § *** reference in Pierce (1961) reference in Singh (1971) reference in Jansonius & Hills (1976 and updates) reference in Dörhöfer (1977) reference in Singh (1983) reference in Fensome et al. (1990) reference in Zonneveld et al. (2013) reference in Fensome et al. (2016) reference in http://botany.si.edu/ing/ reference in http://fossilworks.org All others can be found in http://dinoflaj.smu.ca/wiki/ Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 60 61 Atopodinium haromense Thomas & Cox 1988 Axiodinium augustum (Harland 1979c) Williams et al. 2015 Balmula tripenta Bint 1986 (now Nyktericysta tripenta) Barssidinium evangelineae Lentin et al. 1994 Barssidinium graminosum Lentin et al. 1994 Batiacasphaera reticulata (Davey 1969b) Davey 1979d Batioladinium jaegeri (Alberti 1961) Brideaux 1975 Callaiosphaeridium asymmetricum (Deflandre & Courteville 1939) Davey & Williams 1966b Cannosphaeropsis Wetzel 1933b Cannosphaeropsis passio de Verteuil & Norris 1996a Cauveridinium membraniphorum (Cookson & Eisenack 1962b) Masure in Fauconnier & Masure 2004 Cerbia tabulata (Davey & Verdier 1974) Below 1981a Cerebrocysta bartonensis Bujak in Bujak et al. 1980 Cerebrocysta magna Bujak 1994 Cerebrocysta poulsenii de Verteuil & Norris 1996a Cerodinium Vozzhennikova 1963 Cerodinium diebelii (Alberti 1959b) Lentin & Williams 1987 Cerodinium glabrum (Gocht 1969) Fensome et al. 2009 Cerodinium kangiliense Nøhr-Hansen & Heilmann-Clausen 2001 Cerodinium pannuceum (Stanley 1965) Lentin & Williams 1987 Cerodinium speciosum (Alberti 1959b) Lentin & Williams 1987 Cerodinium speciosum subsp. glabrum (Gocht 1969) Lentin & Williams 1987 (now Cerodinium glabrum) Charlesdowniea columna (Michoux 1988) Lentin & Vozzhennikova 1990 (now Piladinium columnum) Chatangiella (Vozzhennikova 1967) Fensome et al. 2016 * Chatangiella decorosa (McIntyre 1975) Lentin & Williams 1976 Chatangiella ditissima (McIntyre 1975) Lentin & Williams 1976 Chatangiella madura Lentin & Williams 1976 Chatangiella mcintyrei Nøhr-Hansen 1996 Chiropteridium galea (Maier 1959) Sarjeant 1983 Chiropteridium gilbertii Fensome et al. 2016 * Chlamydophorella nyei Cookson & Eisenack 1958 Chytroeisphaeridia hadra Fensome et al. 2016 * Circulodinium distinctum (Deflandre & Cookson 1955) Jansonius 1986 Cleistosphaeridium Davey et al. 1966 Cleistosphaeridium ancyreum (Cookson & Eisenack 1965a) Eaton et al. 2001 Cleistosphaeridium diversispinosum Davey et al. 1966 Cleistosphaeridium palmatum Fensome et al. 2016 * Cleistosphaeridium placacanthum (Deflandre & Cookson 1955) Eaton et al. 2001 Cleistosphaeridium polypes (Cookson & Eisenack 1962b) Davey 1969a (now Kiokansium unituberculatum) Cleistosphaeridium polypetellum (Islam 1983c) Stover &Williams 1995 Cordosphaeridium Eisenack 1963b Cordosphaeridium cantharellus (Brosius 1963) Gocht 1969 Cordosphaeridium delimurum Fensome et al. 2009 Cordosphaeridium fibrospinosum Davey & Williams 1966b Cordosphaeridium funiculatum Morgenroth 1966a Cordosphaeridium gracile (Eisenack 1954b) Davey & Williams 1966b Cordosphaeridium minimum (Morgenroth 1966a) Benedek 1972 (now Minisphaeridium latirictum) Cribroperidinium Neale & Sarjeant 1962 Cribroperidinium giuseppei (Morgenroth 1966a) Helenes 1984 Cyclonepheliium attadalicum Cookson & Eisenack 1962b Dapsilidinium pastielsii (Davey & Williams 1966b) Bujak et al. 1980 Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 61 62 Dapsilidinium pseudocolligerum (Stover 1977) Bujak et al. 1980 Dapsilidinium pseudoinsertum Fensome et al. 2016 * Deflandrea Eisenack 1938b Deflandrea galeata (Lejeune-Carpentier 1942) Lentin & Williams 1973 Deflandrea majae (Schiøler 1993) Fensome et al. 2016 * Deflandrea oebisfeldensis Alberti 1959b Deflandrea phosphoritica Eisenack 1938b Dinogymnium Evitt et al. 1967 Dinogymnium longicorne (Vozzhennikova 1967) Harland 1973 Dinogymnium sibiricum (Vozzhennikova 1967) Lentin & Williams 1973 Diphyes brevispinum Bujak 1994 Diphyes colligerum (Deflandre & Cookson 1955) Cookson 1965a Diphyes ficusoides Islam 1983b Disphaerogena carposphaeropsis Wetzel 1933b Eatonicysta furensis (Heilmann-Clausen in Heilmann-Clausen & Costa 1989) Stover & Williams 1995 Eatonicysta ursulae (Morgenroth 1966a) Stover & Evitt 1978 Edwardsiella sexispinosa Versteegh & Zevenboom in Versteegh 1995 Endoceratium dettmanniae (Cookson & Hughes 1964) Stover & Evitt 1978 Enneadocysta magna Fensome et al. 2007 Eocladopyxis Morgenroth 1966a Eocladopyxis peniculata Morgenroth 1966a Evittosphaerula? foraminosa Fensome et al. 2016 * Fibrocysta bipolaris (Cookson & Eisenack 1965b) Stover & Evitt 1978 Gelatia inflata Bujak 1984 Geonettia de Verteuil & Norris 1996b Gillinia hymenophora Cookson & Eisenack 1960a Ginginodinium? flexidentatum Fensome et al. 2016 * Glaphyrocysta Stover & Evitt 1978 Glaphyrocysta divaricata (Williams & Downie 1966c) Stover & Evitt 1978 Glaphyrocysta exuberans (Deflandre & Cookson 1955 ex Eaton 1976) Stover & Evitt 1978 Glaphyrocysta retiintexta (Cookson 1965a) Stover & Evitt 1978 Glaphyrocysta spineta (Eaton 1976) Stover & Evitt 1978 Glaphyrocysta texta (Bujak 1976) Stover & Evitt 1978 Glaphyrocysta vicina (Eaton 1976) Stover & Evitt 1978 Gonyaulacysta fastigiata Duxbury 1977 Gonyaulacysta pectinigera (Gocht 1970b) Fensome 1979 Habibacysta tectata Head et al. 1989b Hapsocysta? benteae Nøhr-Hansen 1993 Heteraulacacysta Drugg & Loeblich Jr. 1967 Heteraulacacysta porosa Bujak in Bujak et al. 1980 Heterosphaeridium Cookson & Eisenack 1968 Heterosphaeridium bellii Radmacher et al. 2014 Heterosphaeridium difficile (Manum & Cookson 1964) Ioannides 1986 Heterosphaeridium heteracanthum (Deflandre & Cookson 1955) Eisenack & Kjellström 1972 Homotryblium Davey & Williams 1966b Homotryblium abbreviatum Eaton 1976 Homotryblium tenuispinosum Davey & Williams 1966b Hurlandsia rugara (Piasecki 1984) Lister & Batten 1988a Hystrichokolpoma Klumpp 1953 Hystrichokolpoma bulbosum (Ehrenberg 1838) Morgenroth 1968 Hystrichokolpoma rigaudiae Deflandre & Cookson 1955 Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 62 63 Hystrichosphaeridium Deflandre 1937b Hystrichosphaeridium quadratum Fensome et al. 2016 * Hystrichosphaeridium tubiferum (Ehrenberg 1838) Deflandre 1937b Hystrichosphaeropsis perforata Schiøler 1993 Hystrichosphaeropsis quasicribrata (Wetzel 1961) Gocht 1976 Impagidinium Stover & Evitt 1978 Impagidinium dispertitum (Cookson & Eisenack 1965a) Stover & Evitt 1978 Impagidinium victorianum (Cookson & Eisenack 1965a) Stover & Evitt 1978 Impagidinium pallidum Bujak 1984 Impletosphaeridium apodastum Fensome et al. 2016 * Invertocysta lacrymosa Edwards 1984 Isabelidinium Lentin & Williams 1977a Isabelidinium cooksoniae (Alberti 1959b) Lentin & Williams 1977a Isabelidinium cretaceum (Cookson 1956) Lentin & Williams 1977a Isabelidinium magnum (Davey 1970) Stover & Evitt 1978 Isabelidinium microarmum (McIntyre 1975) Lentin & Williams 1977a Kiokansium unituberculatum (Tasch in Tasch et al. 1964) Stover & Evitt 1978 Kiokansium williamsii Singh 1983 Kleithriasphaeridium mantellii (Davey & Williams 1966b) Fensome et al. 2016 * Labyrinthodinium truncatum Piasecki 1980 Laciniadinium McIntyre 1975 Laciniadinium arcticum (Manum & Cookson 1964) Lentin & Williams 1980 Lejeunecysta Artzner and Dörhöfer 1978 Lentinia serrata Bujak in Bujak et al. 1980 Licracysta corymbus Fensome et al. 2007 Licracysta? semicirculata (Morgenroth 1966b) Fensome et al. 2007 Lingulodinium Wall 1967 Lithodinia Eisenack 1935 Manumiella Bujak & Davies 1983 Manumiella cretacea subsp. gravida (Mao Shaozhi & Mohr 1992) Lentin & Williams 1993 Manumiella seelandica (Lange 1969) Bujak & Davies 1983 Mendicodinium Morgenroth 1970 Microdinium ornatum Cookson & Eisenack 1960a Minisphaeridium latirictum (Davey & Williams 1966b) Fensome et al. 2009 Nelchinopsis kostromiensis (Vozzhennikova 1967) Wiggins 1972 Nelsoniella Cookson & Eisenack 1960a Nematosphaeropsis Deflandre & Cookson 1955 Nyktericysta Bint 1986 Nyktericysta arachnion Bint 1986 Nyktericysta davisii Bint 1986 Nyktericysta dictyophora He Chengquan et al. 1992 Nyktericysta tripenta (Bint 1986) Fensome et al. 2009 Odontochitina ancala Bint 1986 Odontochitina costata Alberti 1961 Odontochitina operculata (Wetzel 1933a) Deflandre & Cookson 1955 Odontochitina porifera Cookson 1956 Oligosphaeridium albertense (Pocock 1962) Davey & Williams 1969 Oligosphaeridium totum Brideaux 1971 Operculodinium Wall 1967 Operculodinium centrocarpum (Deflandre & Cookson 1955) Wall 1967 Operculodinium giganteum Wall 1967 Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 63 64 Operculodinium janduchenei Head et al. 1989b Operculodinium piaseckii Strauss & Lund 1992 Palaeocystodinium australinum (Cookson 1965b) Lentin & Williams 1976 Palaeocystodinium bulliforme Ioannides 1986 Palaeocystodinium golzowense Alberti 1961 Palaeohystrichophora infusorioides Deflandre 1935 Palaeoperidinium Deflandre 1934 ex Sarjeant 1967b Palaeoperidinium pyrophorum (Ehrenberg 1838 ex Wetzel 1933a) Sarjeant 1967b Palynodinium grallator Gocht 1970a Perisseiasphaeridium pannosum Davey & Williams 1966b Petalodinium condylos (Williams & Downie 1966b) Williams et al. 2015 Phelodinium Stover & Evitt 1978 Phelodinium kozlowskii (Górka 1963) Lindgren 1984 Phthanoperidinium Drugg & Loeblich Jr. 1967 Phthanoperidinium alectrolophum Eaton 1976 Phthanoperidinium coreoides (Benedek 1972) Lentin & Williams 1976 Phthanoperidinium geminatum Bujak in Bujak et al. 1980 Phthanoperidinium levimurum Bujak in Bujak et al. 1980 Phthanoperidinium multispinum Bujak in Bujak et al. 1980 Phthanoperidinium regale Bujak 1994 Phthanoperidinium stockmansii (de Coninck 1975) Lentin & Williams 1977b Piladinium columna (Michoux 1988) Williams et al. 2015 Polysphaeridium Davey & Williams 1966b Polysphaeridium zoharyi (Rossignol 1962) Bujak et al. 1980 Protoperidinium Bergh 1881a Protoperidinium americanum (Paulsen 1907) Zonneveld & Dale 1994 ^^ Protoperidinium monospinum (Gran & Braarud 1930) Balech 1974 ^^ Pseudoceratium Gocht 1957 Pseudoceratium interiorense Bint 1986 Pterodinium Eisenack 1958a Pyrophacus Stein 1883 Raphidodinium fucatum Deflandre 1936b Reticulatosphaera actinocoronata (Benedek 1972) Bujak & Matsuoka 1986 Rhombodinium draco Gocht 1955 Rhombodinium porosum Bujak 1979 Scalenodinium scalenum Fensome et al. 2016 * Schematophora speciosa Deflandre & Cookson 1955 Scriniodinium obscurum Manum & Cookson 1964 (now Spongodinium obscurum) Selenopemphix brevispinosa Head et al. 1989c Selenopemphix nephroides Benedek 1972 Senegalinium Jain & Millepied 1973 Senegalinium iterlaaense Nøhr-Hansen & Heilmann-Clausen 2001 Senoniasphaera inornata (Drugg 1970b) Stover & Evitt 1978 Senoniasphaera microreticulata Brideaux & McIntyre 1975 Senoniasphaera protrusa Clarke & Verdier 1967 Senoniasphaera rotundata Clarke & Verdier 1967 Simplicidinium insolitum (Eaton 1976) Fensome et al. 2016 * Sirmiodinium grossii Alberti 1961 Sophismatia tenuivirgula (Williams & Downie 1966b) Williams et al. 2015 Spinidinium Cookson & Eisenack 1962b Spinidinium densispinatum Stanley 1965 Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 64 65 Spinidinium echinoideum (Cookson & Eisenack 1960a) Lentin & Williams 1976 Spiniferites Mantell 1850 Spiniferites ovatus Matsuoka 1983b Spiniferites pseudofurcatus (Klumpp 1953) Sarjeant 1970 Spiniferites scabrosus (Clarke & Verdier 1967) Lentin & Williams 1975 Spiniferites solidago de Verteuil & Norris 1996a (=Achomosphaera grallaeformis (Brosius 1963) Davey & Williams 1969) Spongodinium delitiense (Ehrenberg 1838) Deflandre 1936b Spongodinium grossum (Manum & Cookson 1964) Fensome et al. 2016 * Spongodinium obscurum (Manum & Cookson 1964) Fensome et al. 2016 * Stichodinium lineidentatum (Deflandre & Cookson 1955) Williams et al. 2015 Stiphrosphaeridium dictyophorum (Cookson & Eisenack 1958) Lentin & Williams 1985 Subtilisphaera Jain & Millepied 1973 Subtilisphaera perlucida (Alberti 1959b) Jain & Millepied 1973 Surculosphaeridium longifurcatum (Firtion 1952) Davey et al. 1966 Svalbardella Manum 1960 Systematophora ancyrea Cookson & Eisenack 1965a (now Cleistosphaeridium ancyreum) Talladinium pellis Fensome et al. 2016 * Tanyosphaeridium Davey & Williams 1966b Tanyosphaeridium xanthiopyxides (Wetzel 1933b ex Deflandre 1937b) Stover & Evitt 1978 Taurodinium granulatum Fensome et al. 2016 * Tenua hystrix Eisenack 1958a Thalassiphora fenestrata Liengjarern et al. 1980 Trichodinium castanea Deflandre 1935 ex Clarke & Verdier 1967 Trinovantedinium Reid 1977 Trithyrodinium Drugg 1967 Trithyrodinium? conservatum Fensome et al. 2016 * Trithyrodinium evittii Drugg 1967 Trithyrodinium quinqueangulare Marheinecke 1992 Trithyrodinium suspectum (Manum & Cookson 1964) Davey 1969b Tuberculodinium Wall 1967 Tuberculodinium vancampoae (Rossignol 1962) Wall 1967 Vesperopsis Bint 1986 Vesperopsis longicornis (Batten & Lister 1988) Harding 1990b Vesperopsis mayi Bint 1986 Vesperopsis nebulosa Bint 1986 Wallodinium luna (Cookson Eisenack 1960a) Lentin & Williams 1973 Wetzeliella Eisenack 1938b emend. Williams, Damassa, Fensome & Guerstein in Fensome et al. 2009 Wetzeliella homomorpha Deflandre & Cookson 1955 (now Apectodinium homomorphum) Wetzeliella parva Alberti 1961 (now Apectodinium parvum) Xenascus ceratioides (Deflandre 1937b) Lentin & Williams 1973 Xenascus sarjeantii (Corradini 1973) Stover & Evitt 1978 Acritarchs and algae Cymatiosphaera invaginata Head et al. 1989a ** Fromea nicosia Jansonius 1989 * Fromea quadrangularis Fensome et al. 2016 * Fromea tornatilis (Drugg 1978) Lentin & Williams 1981 Micrhystridium Deflandre 1937b Microsphaeridium ancistroides Benedek 1972 Paralecaniella indentata (Deflandre & Cookson 1955) Cookson & Eisenack 1970b Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 65 66 Pediastrum Meyen 1829 * Tetraporina Naumova 1939 Plant microfossils Afropollis Doyle et al. 1982 * Alisporites grandis (Cookson 1953) Dettmann 1963 # Appendicisporites jansonii Pocock 1962 # Aquilapollenites Rouse 1957 * Artemisia Linneaus 1753 § Azolla Lamarck in Lamarck et al. 1783 Balmeisporites holodictyus Cookson & Dettmann 1958 † Bombacacidites Couper 1960 † Callialasporites dampieri (Balme 1957) Dev 1961 * Callialasporites obrutus Norris 1969 * Caryapollenites Raatz 1938 ex Potonié 1960 * Cerebropollenites mesozoicus (Couper 1958) Nilsson 1958 * Cicatricosisporites australiensis (Cookson 1953) Potonié 1956 # Cicatricosisporites minutaestriatus (Bolkhovitina 1961) Pocock 1964 * Cicatricosisporites ornatus Srivastava 1972 * Cicatricosisporites reticicatricosus Döring 1965a > Cicatricososporites eocenicus (Selling 1944) Jansonius & Hills 1976 * Compositoipollenites Potonié 1951 ex Potonié 1960 * Contignisporites glebulentus Dettmann 1963 # Corsinipollenites oculusnoctis (Thiergart 1940) Nakoman 1965 * Extratriporopollenites Pflug in Thomson & Pflug 1952 ex Pflug in Thomson & Pflug 1953 * Graminidites Cookson 1947 ex Potonié 1960 * Klukisporites areolatus Singh 1971 # Osmundacidites wellmannii Couper 1953 * Parvisaccites amplus Brenner 1963 * Parvisaccites radiatus Couper 1958 * Periporopollenites Pflug & Thomson in Thomson & Pflug 1953 * Pilosisporites verus Delcourt & Sprumont 1955 *** Pinus Linnaeus 1753 § Pinuspollenites Raatz 1938 ex Potonié 1958 † Pistillipollenites macgregorii Rouse 1962 * Plicatella bifurcata (Singh 1964) Dörhöfer 1977 > Quercoidites Potonié et al. 1950 ex Potonié 1960 * Rugubivesiculites Pierce 1961 ^ Rugubivesiculites convolutus Pierce 1961 † Rugubivesiculites multiplex Pierce 1961 ^ Rugubivesiculites multisaccus Singh 1983 †† Rugubivesiculites reductus Pierce 1961 ^ Rugubivesiculites rugosus Pierce 1961 ^ Taraxacum Wiggers 1780 § Tiliaepollenites crassipites (Wodehouse 1933) Fensome et al. 2016 * Tsugaepollenites igniculus Potonié 1931 * (now Zonalapollenites igniculus) Wodehouseia spinata Stanley 1961 * Zlivisporis Pacltová 1961 * Zonalapollenites igniculus (Potonié 1931) Thomson & Pflug 1953 * Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 66 67 Palaeoenvironmental analysis of six wells on the Canadian margin (for location, see Fig. 1), based on palaeoecolo - gical interpretation of palynological data (by Graham L. Williams). Legend for Appendices 2.1–2.6 Appendix 2 Cuttings sample Cuttings sample (secondary suite) Side-wall core (SWC) Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 67 68 Pliocene – Pleistocene Serravallian early Miocene Chattian Rupelian Priabonian Bartonian 405–415 430–440 465–475 490–500 525–535 555–565 585–595 615–625 645–655 675–685 700–710 735–745 765–775 790–800 825–835 855–865 885–895 950–960 970–980 1035–1045 1065–1075 1095–1105 1125–1135 1155–1165 1215–1225 1275–1285 1305–1315 1335–1345 1365–1375 1395–1405 1425–1435 1455–1465 1485–1495 DEPOSITIONAL ENVIRONMENT DEPOSITIONAL ENVIRONMENT N o n -m ar in e C o as ta l – M ar gi n al m ar in e In n er n er it ic O u te r n er it ic O p en o ce an SAMPLE DEPTH (m)AGE PERIOD/ EPOCH AGE PERIOD/ EPOCH SAMPLE DEPTH (m) 400 (m) 500 600 700 800 900 1000 1100 1200 1300 1400 1500 Lutetian Ypresian Bartonian basal Ypresian Danian Selandian Maastrichtian e. Campanian Turonian– Coniacian early Albian Cenomanian? Aptian 1525–1535 1545–1555 1575–1585 1605–1615 1635–1645 1660–1670 1725–1735 1695–1705 1755–1765 1785–1795 1815–1825 1875–1885 1905–1915 1935–1945 1965–1975 1995–2005 2025–2035 2055–2065 2085–2095 2115–2125 2145–2155 2175–2185 2205–2215 2235–2245 2265–2275 2295–2305 2350–2360 2330–2340 2380–2390 2415–2425 2445–2455 2475–2485 2535–2545 2565–2575 2595–2605 2625–2635 2645–2655 1500 1600 1700 1800 1900 2000 2100 2200 2300 2400 2500 2600 N o n -m ar in e C o as ta l – M ar gi n al m ar in e In n er n er it ic O u te r n er it ic O p en o ce an M O C E N E O L IG O C E N E E O C E N E E L E L M M E O C E N E P A L E O C E N E C R E T A C E O U S M E L E L E Appendix 2.1. Stratigraphy and palaeoenvironmental interpretation of the Bjarni O-82 well. Kelly Bushing height: 12.0 m above sea level. Water depth: 144 m. Total depth: 2650.0 m. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 68 69 Pliocene– Pleistocene middle Miocene M O C E N E O L IG O C E N E E O C E N E Rupelian Ypresian early Miocene Priabonian Bartonian early Lutetian 720–730 750–760 780–790 810–820 840–850 870–880 900–910 930–940 960–970 990–1000 1020–1030 1050–1060 1080–1090 1110–1120 1140–1150 1170–1180 1200–1210 1230–1240 1260–1270 1290–1300 1320–1330 1350–1360 1380–1390 1410–1420 1440–1450 1470–1480 1500–1510 1530–1540 1560–1570 1590–1600 1620–1630 1650–1660 1680–1690 1710–1720 1740–1750 1770–1780 1800–1810 1920–1930 1950–1960 1980–1990 2010–2020 2040–2050 2070–2080 2100–2110 2130–2140 1830–1840 1890–1900 800 (m) 900 1000 1100 1200 1300 1400 1500 1600 1700 1800 1900 2000 2100 Thanetian Danian Aptian Precambrian early Ypresian Selandian early Maastrichtian Campanian Coniacian 2130–2140 2160–2170 2190–2200 2220–2230 2250–2260 2280–2290 2310–2320 2340–2350 2370–2380 2400–2410 2430–2440 2460–2470 2490–2500 2550–2560 2580–2590 2610–2620 2640–2650 2700–2710 2730–2740 2760–2770 2790–2800 2820–2830 2850–2860 2520–2530 2880–2890 2910–2920 2940–2950 2970–2980 3000–3010 3030–3040 3060–3070 3090–3100 3120–3130 3150–3160 3180–3190 3210–3220 3240–3250 3270–3280 3300–3310 3330–3340 3360–3370 3390–3400 3420–3430 3450–3460 3480–3490 3510–3520 3540–3550 3545–3555 3571.5 3565–3571.5 2200 (m) 2300 2400 2500 2600 2700 2800 2900 3000 3100 3200 3300 3400 3500 DEPOSITIONAL ENVIRONMENT N o n -m ar in e C o as ta l – M ar gi n al m ar in e M ar gi n al m ar in e In n er n er it ic O u te r n er it ic O p en o ce an DEPOSITIONAL ENVIRONMENT N o n -m ar in e C o as ta l – In n er n er it ic O u te r n er it ic O p en o ce an AGE PERIOD/ EPOCH AGE PERIOD/ EPOCH SAMPLE DEPTH (m) SAMPLE DEPTH (m) Ypresian M E E E L M E E E L L E O C E N E P A L E O C E N E C R E T A C E O U S Appendix 2.2. Stratigraphy and palaeoenvironmental interpretation of the South Labrador N-79 well. Kelly Bushing height: 11.3 m above sea level. Water depth: 449.9 m. Total depth: 3571.5 m. Bulletin37.qxp_Bulletin 37 26/01/17 13.59 Side 69 70 Pliocene– Pleistocene Pliocene late Miocene 384.05–393.19 414.53–423.67 445.01–454.15 475.49–484.63 505.97–515.11 536.45–545.59 566.93–576.07 597.41–606.55 627.89–637.03 658.37–667.51 688.85–697.99 719.33–728.47 749.81–758.95 780.29–789.43 810.77–819.91 841.25–850.39 932.69–941.83 950.98–960.12 978.41–987.55 1005.84–1014.98 1033.27–1042.42 1124.71–1133.86 1152.14–1161.29 1261.87–1271.02 1295.4 1316.74–1325.88 1344.17–1353.31 1371.6 1399.03–1408.18 1426.46–1435.61 1453.90–1463.04 1481.33–1490.47 1508.76–1517.91 1536.19–1545.34 1563.62–1572.77 1591.06–1597.16 1618.49–1627.63 1645.92 1673.35–1682.50 1700.79–1709.93 1728.22–1737.37 1755.65–1764.80 1776.98 1783.09–1792.23 400 (m) 500 600 700 800 900 1000 1100 1200 1300 1400 1500 1600 1700 1800 Bartonian Lutetian Ypresian basal Ypresian Thanetian Selandian Danian Aptian Precambrian 1810.52–1819.66 1837.95–1847.09 1865.38–1874.53 1892.81–1901.96 1920.25–1929.39 1947.68–1956.82 1975.11–1984.25 2005.59–2014.73 2029.97–2039.12 2072.64 2084.83–2093.98 2112.27–2121.41 2139.70–2148.85 2161.03 2194.57–2203.71 2240.29 2249.43–2258.57 2293.63 2304.29–2313.44 2340.87 2359.16–2368.30 2386.59–2395.74 2420.12 2441.46–2450.60 2468.89–2478.03 2497.23–2497.54 2499.37–2499.67 2520.70 2551.18–2560.33 2578.62–2587.76 2609.10–2618.24 2636.53–2645.67 2663.96–2673.10 2700.53 2724.91 2763.32 2779.78–2788.93 2820.02 2840.74–2849.89 2871.22–2880.37 2889.51 2915.42 2932.18–2941.33 2962.66–2971.81 2993.15–3002.29 3025.45 3037.34 3054.11–3063.25 3127.56 3145.55–3154.69 3176.03–3185.17 3200.41–3209.55 1800 1900 2000 2100 2200 2300 2400 2500 2600 2700 2800 2900 3000 3100 3200 DEPOSITIONAL ENVIRONMENT N o n -m ar in e C o as ta l – M ar gi n al m ar in e In n er n er it ic O u te r n er it ic O p en o ce an DEPOSITIONAL ENVIRONMENT N o n -m ar in e C o as ta l – M ar gi n al m ar in e In n er n er it ic O u te r n er it ic O p en o ce an AGE PERIOD/ EPOCH AGE PERIOD/ EPOCH SAMPLE DEPTH (m) SAMPLE DEPTH (m) early–middle Miocene early Oligocene early Priabonian early Priabonian P L IO C E N E – P L E IS T O C E N E M O C E N E O L IG O C E N E E O C E N E P L IO C E N E L L E O C E N E P A L E O C E N E C R E T A C E O U S L M E E E L E E-M Appendix 2.3. Stratigraphy and palaeoenvironmental interpretation of the Snorri J-90 well. Kelly Bushing height: 11.3 m above sea level. Water depth: 140.8 m. Total depth: 3209.8 m. Bulletin37.qxp_Bulletin 37 26/01/17 14.00 Side 70 71 late Miocene early–middle Miocene Chattian Rupelian Priabonian Bartonian Lutetian Ypresian 525–535 555–565 585–595 615–625 645–655 675–685 705–715 735–745 765–775 795–805 825–835 855–865 885–895 915–925 945–955 975–985 1005–1015 1035–1045 1065–1075 1095–1105 1125–1135 1155–1165 1185–1195 1215–1225 1245–1255 1275–1285 1305–1315 1335–1345 1365–1375 1395–1405 1425–1435 1455–1465 1485–1495 1515–1525 1545–1555 1575–1585 1605–1615 1635–1645 1665–1675 1695–1705 1725–1735 1755–1765 1785–1795 1815–1825 1845–1855 1875–1885 1905–1915 1935–1945 1965–1975 1995–2005 2025–2035 2055–2065 520–530 550–560 580–590 610–615 640–650 670–680 700–710 730–740 760–770 790–800 820–830 850–860 880–890 910–920 940–950 970–980 1000–1010 1030–1040 1060–1070 1090–1100 1120–1130 1150–1160 1180–1190 1210–1220 1240–1250 1270–1280 1300–1310 1330–1340 1360–1370 1390–1400 1420–1430 1450–1460 1480–1490 1510–1520 1540–1550 1570–1580 1600–1610 1630–1640 1660–1665 1700–1710 1720–1730 1750–1760 1780–1790 1810–1820 1840–1850 1870–1880 1900–1910 1930–1940 1960–1965 1990–2000 2020–2030 2050–2060 DEPOSITIONAL ENVIRONMENT DEPOSITIONAL ENVIRONMENT N o n -m ar in e C o as ta l – M ar gi n al m ar in e In n er n er it ic O u te r n er it ic O p en o ce an N o n -m ar in e C o as t a l – M ar gi n al m ar in e In n er n er it ic O u te r n er it ic O p en o ce an 600 (m) 700 800 900 1000 1100 1200 1300 1400 1500 1600 1700 1800 1900 2000 Thanetian Selandian Danian la te Maastrichtian late Campanian I late Campanian II e. Campanian ea rl y 2085–2095 2115–2125 2145–2155 2175–2185 2205–2215 2235–2245 2265–2275 2295–2305 2325–2335 2350–2360 2380–2390 2410–2420 2440–2450 2470–2480 2500–2510 2530–2540 2560–2570 2590–2600 2620–2630 2650–2660 2670–2680 2700–2710 2730–2740 2760–2770 2790–2800 2820–2830 2850–2860 2880–2890 2910–2920 2940–2950 2970–2980 3000–3010 3030–3040 3060–3070 3090–3100 3120–3130 3150–3160 3180–3190 3210–3220 3240–3250 3270–3280 3300–3310 3330–3340 3360–3370 3390–3400 3420–3430 3450–3460 3480–3490 3510–3520 3540–3550 3570–3580 3595–3605 2080–2090 2110–2120 2135–2145 2170–2180 2200–2210 2240–2250 2260–2270 2290–2300 2320–2330 2360–2370 2560–2570 2680–2690 2705–2715 2740–2750 2770–2780 2800–2810 2830–2840 2860–2870 2890–2900 2920–2930 2950–2960 2980–2990 3010–3020 3040–3050 3070–3080 3100–3110 3130–3140 3160–3170 3190–3200 3220–3230 3250–3260 3280–3290 3310–3320 3340–3350 3370–3380 3410–3420 3430–3440 3460–3470 3490–3500 3520–3530 3550–3560 3580–3590 2100 2200 2300 2400 2500 2600 2700 2800 2900 3000 3100 3200 3300 3400 3500 3600 AGE Suite 1 Suite 2 PERIOD/ EPOCH SAMPLE DEPTH (m) AGE Suite 1 Suite 2 PERIOD/ EPOCH SAMPLE DEPTH (m) basal Ypresian M IO C E N E O L IG O C E N E E O C E N E E O C E N E P A L E O C E N E C R E T A C E O U S L L E E E L L E M L E-M Appendix 2.4. Stratigraphy and palaeoenvironmental interpretation of the Gilbert F-53 well. Kelly Bushing height: 12.1 m above sea level. Water depth: 183 m. Total depth: 3608.0 m. Bulletin37.qxp_Bulletin 37 26/01/17 14.00 Side 71 72 800 900 1000 1100 1200 1300 1400 1500 1600 1700 1800 1900 2000 2100 2200 2300 2400 2500 Miocene Chattian Rupelian Priabonian Bartonian Lutetian 800–810 890–900 920–930 950–960 980–990 1060–1070 1090–1100 1120–1130 1150–1160 1180–1190 1230–1240 1260–1270 1290–1300 1330–1340 1360–1370 1390–1400 1420–1430 1460–1470 1490–1500 1520–1530 1550–1560 1580–1590 1610–1620 1640–1650 1660–1670 1720–1730 1750–1760 1780–1790 1840–1850 1870–1880 1900–1910 1930–1940 1970–1980 2000–2010 2030–2040 2060–2070 2090–2100 2120–2130 2150–2160 2180–2190 2210–2220 2240–2250 2270–2280 2300–2310 2330–2340 2360–2370 2390–2400 2420–2430 2460–2470 2490–2500 2520–2530 2550–2560 1040–1050 1110–1120 1220–1230 1465–1475 1510–1520 1650–1660 1690–1700 1805–1815 1895–1905 2080–2090 2170–2180 2200–2210 2230–2240 2215–2225 2260–2270 2365–2375 2391–2401 2435–2445 2470–2480 2510–2520 2551–2561 1816.0 2435.6 2587.0 2600 2610–2620 2700 2800 2900 3000 3100 3200 3300 3400 3500 3600 3700 3800 3900 4000 4100 4200 4300 4400 4500 Ypresian Ypresian Thanetian Selandian 2670–2680 2700–2710 2730–2740 2790–2800 2820–2830 2850–2860 2880–2890 2895–2905 2920–2930 2940–2950 2970–2980 3000–3010 3030–3040 3060–3070 3090–3100 3120–3130 3140–3150 3150–3160 3180–3190 3210–3220 3270–3280 3310–3320 3350–3360 3410–3420 3450–3460 3510–3520 3570–3580 3610–3620 3650–3660 3730–3740 3770–3780 3830–3840 3870–3880 3930–3940 3970–3980 4010–4020 4030–4040 4050–4060 4070–4080 4090–4100 4110–4120 4130–4140 4150–4160 4170–4180 4190–4200 4210–4220 4230–4240 4250–4260 4270–4280 4290–4300 4310–4320 4330–4340 4350–4360 4370–4380 4390–4440 4410–4420 4430–4440 4450–4460 4470–4480 4490–4500 4510–4520 4530–4540 4550–4560 4340–4350 4353–4363 4380–4390 4400–4410 4432–4442 4420–4430 4440–4450 4460–4470 4480–4490 4500–4510 4538–4548 4540–4550 4560–45664565–4566 4566–4566 2655–2665 2690–2700 2740–2750 2770–2780 2870–2880 2920–2930 2930–2940 2931–2941 2960–2970 2985–2995 3045–3055 3091–3101 3121–3131 3139–3149 3141–3151 3160–3170 3181–3191 3200–3210 3211–3221 3225–32353230–3240 3245–32553251–3261 3265–3275 3271–3281 3300–3310 3360–3370 3320–3330 3400–3410 3480–3490 3500–3510 3520–3530 3600–3610 3640–3650 3700–3710 3630–3640 3680–3690 3720–3730 3760–3770 3840–3850 3795–3805 3800–3810 3880–3890 3920–3930 3900–3910 3960–3970 4000–4010 4040–4050 4080–4090 4120–4130 4180–4190 4200–4210 4220–4230 4260–4270 4300–4310 2766.0 2918.0 3245.8 3250.0 3258.0 3546.0 4100–4110 4001–4011 2640–2650 N o n -m ar in e C o as ta l – M ar gi n al m ar in e In n er n er it ic O u te r n er it ic O p en o ce an DEPOSITIONAL ENVIRONMENT DEPOSITIONAL ENVIRONMENT N o n -m ar in e C o as ta l – M ar gi n al m ar in e In n er n er it ic O u te r n er it ic O p en o ce an AGE PERIOD/ EPOCH SAMPLE DEPTH (m) M IO - C E N E O L IG O C E N E E O C E N E E O C E N E E L L M E E P A L E O C E N E L Suite 1 Suite 2 AGE PERIOD/ EPOCH SAMPLE DEPTH (m) Suite 1 Suite 2 SWC Appendix 2.5. Stratigraphy and palaeoenvironmental interpretation of the Hekja O-71 well. Kelly Bushing height: 12.5 m above sea level. Water depth: 350.8 m. Total depth: 4566.0 m. Bulletin37.qxp_Bulletin 37 26/01/17 14.00 Side 72 73 1500 (m) 1600 1700 1800 1900 2000 2100 2200 2300 2400 2500 2600 2700 Rupelian Priabonian Bartonian Lutetian Thanetian 2050–2060 2110–2120 2190–2200 2290–2300 1490–1500 1510–1520 1530–1540 1520–1530 1550–1560 1565–1575 1570–1580 1575–1585 1600–1610 1620–1630 1610–1620 1640–1650 1630–1640 1660–1670 1670–1680 1690–1700 1700–1710 1710–1720 1740–1750 1760–1770 1750–1760 1780–1790 1770–1780 1800–1810 1820–1830 1840–1850 1830–1840 1858–1868 1860–1870 1890–1900 1950–1960 1920–1930 1990–2000 2020–2030 2030–2040 2070–2080 2150–2160 2200–2210 2230–2240 2250–2260 2310–2320 2270–2280 2320–2330 2350–2360 2380–2390 2390–2400 2410–2420 2440–2450 2470–2480 2430–2440 2500–2510 2510–2520 2530–2540 2550–2560 2580–2590 2590–2600 2600–2610 2620–2630 2650–2660 2670–2680 2630–2640 2680–2690 2690–2700 2710–2720 2800 (m) 2900 3000 3100 3200 3300 3400 3500 3600 3700 3800 3900 Thanetian Selandian Danian 2740–2750 2750–2760 2770–2780 2800–2810 2790–2800 2830–2840 2840–2850 2870–2880 2890–2900 2920–2930 2917–2927 2940–2950 2960–2970 2950–2960 3000–3010 2990–3000 3030–3040 3060–3070 3090–3100 3070–3080 3120–3130 3110–3120 3150–3160 3180–3190 3190–3200 3200–3210 3230–3240 3270–3280 3300–3310 3320–3330 3330–3340 3350–3360 3360–3370 3390–3400 3420–3430 3450–3460 3470–3480 3430–3440 3480–3490 3510–3520 3540–3550 3550–3560 3560–3570 3590–3600 3620–3630 3600–3610 3650–3660 3680–3690 3670–3680 3710–3720 3740–3750 3770–3780 3790–3800 3750–3760 3810–3820 3830–3840 3860–3870 3890–3900 3870–3880 3910–3920 3900–3910 3940–3950 3920–3930 3970–3980 3980–3990 3950–3960 3960–3970 3988–3998 DEPOSITIONAL ENVIRONMENT DEPOSITIONAL ENVIRONMENT N o n -m ar in e C o as ta l – M ar gi n al m ar in e In n er n er it ic O u te r n er it ic O p en o ce an AGE PERIOD/ EPOCH AGE SAMPLE DEPTH (m) PERIOD/ EPOCH SAMPLE DEPTH (m) N o n -m ar in e C o as ta l – M ar gi n al m ar in e In n er n er it ic O u te r n er it ic O p en o ce an Ypresian E O C E N E P A L E O C E N E P A L E O C E N E O L I E L M E E L L Appendix 2.6. Stratigraphy and palaeoenvironmental interpretation of the Gjoa G-37 well. Kelly Bushing height: 24.0 m above sea level. Water depth: 1000 m. Total depth: 3998 m. Bulletin37.qxp_Bulletin 37 26/01/17 14.00 Side 73 74 Appendices 3.1–3.19 are located in pockets attached to the inside covers Palynological event summary charts for the 19 wells used in this study, in order from south to north (for well loca- tions, see Fig. 1). Although the information included varies from chart to chart, wireline logs, a simplified lithology log, lithostratigraphic units, palynological events and chronostratigraphic subdivisions are included for all wells. Charts of wells analysed by Henrik Nøhr-Hansen (Hellefisk-1, Ikermiut-1, Kangâmiut-1, Nukik-1, Nukik-2, Qulleq-1, North Leif I-05, Ogmund E-72, Skolp E-07, Hekja O-71, Ralegh N-18 and Gjoa G-37) include, in addi- tion to palynological events, a biostratigraphic zonation for the Aptian–Albian to Priabonian of the West Greenland and Labrador Margins of the Labrador Sea; this zonation was published by Nøhr-Hansen in Sønderholm et al. (2003b), Nøhr-Hansen et al. (2000, 2002) and Nøhr-Hansen (2003, 2004a, b). Some of the well charts listed above also show dinocyst species diversity, Azolla abundances and palaeoenvironmental interpretations for the Palaeogene (after Rasmussen et al. 2003). Plots generated by Graham L. Williams and Robert A. Fensome (Bjarni O-82, Gilbert F-53, Karlsefni A-13, Roberval K-92, Rut H-11, Snorri J-90 and South Labrador N-79) show events and ages only; a biozonation was not developed. KB: Kelly Bushing. Appendix 3 Bulletin37.qxp_Bulletin 37 26/01/17 14.00 Side 74 75 Bulletin37.qxp_Bulletin 37 26/01/17 14.00 Side 75 76 De Nationale Geologiske Undersøgelser for Danmark og Grønland (GEUS) Geological Survey of Denmark and Greenland Øster Voldgade 10, DK-1350 Copenhagen K Denmark The series Geological Survey of Denmark and Greenland Bulletin started in 2003 and replaced the two former bulletin series of the Survey, viz. Geology of Greenland Survey Bulletin and Geology of Denmark Survey Bulletin. The twenty-one volumes published since 1997 in those two series are listed on the following pages. The present series, together with Geological Survey of Denmark and Greenland Map Series, now form the peer-reviewed scientific series of the Survey. Geological Survey of Denmark and Greenland Bulletin 1 The Jurassic of Denmark and Greenland, 948 pp. (28 articles), 2003. Edited by J.R. Ineson & F. Surlyk. 500.00 2 Fish otoliths from the Paleocene of Denmark, 94 pp., 2003. By W. Schwarzhans. 100.00 3 Late Quaternary environmental changes recorded in the Danish marine molluscan faunas, 268 pp., 2004. By K.S. Petersen. 200.00 4 Review of Survey activities 2003, 100 pp. (24 articles), 2004. Edited by M. Sønderholm & A.K. Higgins. 180.00 5 The Jurassic of North-East Greenland, 112 pp. (7 articles), 2004. Edited by L. Stemmerik & S. Stouge. 160.00 6 East Greenland Caledonides: stratigraphy, structure and geochronology, 93 pp. (6 articles), 2004. Edited by A.K. Higgins & F. Kalsbeek. 160.00 7 Review of Survey activities 2004, 80 pp. (19 articles), 2005. Edited by M. Sønderholm & A.K. Higgins. 180.00 8 Structural analysis of the Rubjerg Knude Glaciotectonic Complex, Vendsyssel, northern Denmark, 192 pp., 2005. By S.A.S. Pedersen. 300.00 9 Scientific results from the deepened Lopra-1 borehole, Faroe Islands, 156 pp. (11 articles), 2006. Edited by J.A. Chalmers & R. Waagstein. 240.00 10 Review of Survey activities 2005, 68 pp. (15 articles), 2006. Edited by M. Sønderholm & A.K. Higgins. 180.00 11 Precambrian crustal evolution and Cretaceous–Palaeogene faulting in West Greenland, 204 pp. (12 articles), 2006. Edited by A.A. Garde & F. Kalsbeek. 240.00 12 Lithostratigraphy of the Palaeogene – Lower Neogene succession of the Danish North Sea, 77 pp., 2007. By P. Schiøler, J. Andsbjerg, O.R. Clausen, G. Dam, K. Dybkjær, L. Hamberg, C. Heilmann-Clausen, E.P. Johannessen, L.E. Kristensen, I. Prince & J.A. Rasmussen. 240.00 13 Review of Survey activities 2006, 76 pp. (17 articles), 2007. Edited by M. Sønderholm & A.K. Higgins. 180.00 14 Quaternary glaciation history and glaciology of Jakobshavn Isbræ and the Disko Bugt region, West Greenland: a review, 78 pp., 2007. By A. Weidick & O. Bennike. 200.00 15 Review of Survey activities 2007, 96 pp. (22 articles), 2008. Edited by O. Bennike & A.K. Higgins. 200.00 16 Evaluation of the quality, thermal maturity and distribution of potential source rocks in the Danish part of the Norwegian–Danish Basin, 66 pp., 2008. By H.I. Petersen, L.H. Nielsen, J.A. Bojesen-Koefoed, A. Mathiesen, L. Kristensen & F. Dalhoff. 200.00 17 Review of Survey activities 2008, 84 pp. (19 articles), 2009. Edited by O. Bennike, A.A. Garde & W.S. Watt. 200.00 18 Greenland from Archaean to Quaternary. Descriptive text to the 1995 Geological map of Greenland, 1:2 500 000. 2nd edition, 126 pp., 2009. By N. Henriksen, A.K. Higgins, F. Kalsbeek & T.C.R. Pulvertaft. 280.00 19 Lithostratigraphy of the Cretaceous–Paleocene Nuussuaq Group, Nuussuaq Basin, West Greenland, 171 pp., 2009. By G. Dam, G.K. Pedersen, M. Sønderholm, H.H. Midtgaard, L.M. Larsen, H. Nøhr-Hansen & A.K. Pedersen. 300.00 20 Review of Survey activities 2009, 106 pp. (23 articles), 2010. Edited by O. Bennike, A.A. Garde & W.S. Watt. 220.00 21 Exploration history and place names of northern East Greenland, 368 pp., 2010. By A.K. Higgins. 200.00 22 Lithostratigraphy of the Upper Oligocene – Miocene succession of Denmark, 92 pp., 2010. By E.S. Rasmussen, K. Dybkjær & S. Piasecki. 240.00 23 Review of Survey activities 2010, 84 pp. (19 articles), 2011. Edited by O. Bennike, A.A. Garde & W.S. Watt. 200.00 Bulletin37.qxp_Bulletin 37 26/01/17 14.00 Side 76 77 24 The East Greenland rifted volcanic margin, 96 pp., 2011. By C.K. Brooks. 200.00 25 Upper Cretaceous chalk facies and depositional history recorded in the Mona-1 core, Mona Ridge, Danish North Sea. 2011. By K. Anderskouv & F. Surlyk. 200.00 26 Review of Survey activities 2011, 88 pp. (21 articles), 2012. Edited by O. Bennike, A.A. Garde & W.S. Watt. 200.00 27 Neoglacial and historical glacier changes around Kangersuneq fjord in southern West Greenland, 68 pp., 2012. By A. Weidick, O. Bennike, M. Citterio & N. Nørgaard-Pedersen. 200.00 28 Review of Survey activities 2012, 76 pp. (17 articles), 2013. Edited by O. Bennike, A.A. Garde & W.S. Watt. 200.00 29 Tectono-magmatic evolution of the younger Gardar southern rift, South Greenland, 124 pp., 2013. By B.G.J. Upton. 240.00 30 Stratigraphic landscape analysis, thermochronology and the episodic development of elevated, passive continental margins, 150 pp., 2014. By Paul F. Green, Karna Lidmar-Bergström, Peter Japsen, Johan M. Bonow and James A. Chalmers. 250.00 31 Review of Survey activities 2013, 98 pp., 2014. Edited by O. Bennike, A.A. Garde & W.S. Watt 200.00 32 A catalogue of Danian gastropods from the Baunekule facies, Faxe Formation, Denmark, 117 pp., 2014 By B.W. Lauridsen & K.I. Schnetler. 240.00 33 Review of Survey activities 2014, 88 pp. (20 articles), 2015. Edited by O. Bennike, A.A. Garde & W.S. Watt. 200.00 34 The ammonites of the Middle Jurassic Cranocephalites beds of East Greenland, 145 pp., 2015. By J.H. Callomon, P. Alsen & F. Surlyk. 250.00 35 Review of Survey activities 2015, 106 pp. (24 articles), 2015. Edited by A.A Garde, O. Bennike, K. Thrane & W.S. Watt. 200.00 36 Cretaceous and Cenozoic dinoflagellate cysts and other palynomorphs from the western and eastern margins of the Labrador–Baffin Seaway, 143 pp., 2016. By R.A. Fensome, H. Nøhr-Hansen & G.L. Williams. 250.00 37 Biostratigraphic correlation of the western and eastern margins of the Labrador–Baffin Seaway and implications for the regional geology, 75 pp., 2016. By H. Nøhr-Hansen, G.L. Williams & R.A. Fensome. 200.00 Geological Survey of Denmark and Greenland Map Series 1 Explanatory notes to the Geological map of Greenland, 1:500 000, Humboldt Gletscher, Sheet 6, 48 pp. + map, 2004. By P.R. Dawes. 280.00 2 Explanatory notes to the Geological map of Greenland, 1:500 000, Thule, Sheet 5 (1991), 97 pp. + map, 2006. By P.R. Dawes. 300.00 3 Explanatory notes to the Geological map of Greenland, 1:100 000, Ussuit 67 V.2 Nord, 40 pp. + map, 2007. By J.A.M. van Gool & M. Marker. 280.00 4 Descriptive text to the Geological map of Greenland, 1:500 000, Dove Bugt, Sheet 10, 32 pp. + map, 2009. By N. Henriksen & A.K. Higgins. 240.00 5 Descriptive text to the Geological map of Greenland, 1:100 000, Kangaatsiaq 68 V.1 Syd and Ikamiut 68 V.1 Nord, 41 pp. + 2 maps, 2010. By A.A. Garde & J.A. Hollis. 280.00 Geology of Greenland Survey Bulletin (173–191; discontinued) 173 Cambrian shelf stratigraphy of North Greenland, 120 pp., 1997. By J.R. Ineson & J.S. Peel 250.00 174 The Proterozoic Thule Supergroup, Greenland and Canada: history, lithostratigraphy and development, 150 pp., 1997. By P.R. Dawes 300.00 175 Stratigraphy of the Neill Klinter Group; a Lower – lower Middle Jurassic tidal embayment succession, Jameson Land, East Greenland, 80 pp., 1998. By G. Dam & F. Surlyk. 250.00 176 Review of Greenland activities 1996, 112 pp. (18 articles), 1997. Edited by A.K. Higgins & J.R. Ineson. 200.00 177 Accretion and evolution of an Archaean high-grade grey gneiss – amphibolite complex: the Fiskefjord area, southern West Greenland, 115 pp., 1997. By A.A. Garde. 200.00 178 Lithostratigraphy, sedimentary evolution and sequence stratigraphy of the Upper Proterozoic Lyell Land Group (Eleonore Bay Supergroup) of East and North-East Greenland, 60 pp., 1997. By H. Tirsgaard & M. Sønderholm. 200.00 Bulletin37.qxp_Bulletin 37 26/01/17 14.00 Side 77 << /ASCII85EncodePages false /AllowTransparency true /AutoPositionEPSFiles true /AutoRotatePages /None /Binding /Left /CalGrayProfile (Dot Gain 20%) /CalRGBProfile (Apple RGB) /CalCMYKProfile (U.S. Web Coated \050SWOP\051 v2) /sRGBProfile (sRGB IEC61966-2.1) /CannotEmbedFontPolicy /Warning /CompatibilityLevel 1.6 /CompressObjects /Tags /CompressPages true /ConvertImagesToIndexed true /PassThroughJPEGImages true /CreateJobTicket false /DefaultRenderingIntent /Default /DetectBlends true /DetectCurves 0.0000 /ColorConversionStrategy /LeaveColorUnchanged /DoThumbnails false /EmbedAllFonts true /EmbedOpenType false /ParseICCProfilesInComments true /EmbedJobOptions true /DSCReportingLevel 0 /EmitDSCWarnings false /EndPage -1 /ImageMemory 1048576 /LockDistillerParams false /MaxSubsetPct 100 /Optimize false /OPM 1 /ParseDSCComments true /ParseDSCCommentsForDocInfo true /PreserveCopyPage true /PreserveDICMYKValues true /PreserveEPSInfo true /PreserveFlatness false /PreserveHalftoneInfo false /PreserveOPIComments false /PreserveOverprintSettings true /StartPage 1 /SubsetFonts true /TransferFunctionInfo /Apply /UCRandBGInfo /Remove /UsePrologue false /ColorSettingsFile () /AlwaysEmbed [ true ] /NeverEmbed [ true ] /AntiAliasColorImages false /CropColorImages false /ColorImageMinResolution 300 /ColorImageMinResolutionPolicy /OK /DownsampleColorImages true /ColorImageDownsampleType /Bicubic /ColorImageResolution 300 /ColorImageDepth -1 /ColorImageMinDownsampleDepth 1 /ColorImageDownsampleThreshold 1.50000 /EncodeColorImages true /ColorImageFilter /DCTEncode /AutoFilterColorImages true /ColorImageAutoFilterStrategy /JPEG /ColorACSImageDict << /QFactor 0.15 /HSamples [1 1 1 1] /VSamples [1 1 1 1] >> /ColorImageDict << /QFactor 0.15 /HSamples [1 1 1 1] /VSamples [1 1 1 1] >> /JPEG2000ColorACSImageDict << /TileWidth 256 /TileHeight 256 /Quality 30 >> /JPEG2000ColorImageDict << /TileWidth 256 /TileHeight 256 /Quality 30 >> /AntiAliasGrayImages false /CropGrayImages false /GrayImageMinResolution 300 /GrayImageMinResolutionPolicy /OK /DownsampleGrayImages true /GrayImageDownsampleType /Bicubic /GrayImageResolution 300 /GrayImageDepth -1 /GrayImageMinDownsampleDepth 2 /GrayImageDownsampleThreshold 1.50000 /EncodeGrayImages true /GrayImageFilter /DCTEncode /AutoFilterGrayImages true /GrayImageAutoFilterStrategy /JPEG /GrayACSImageDict << /QFactor 0.15 /HSamples [1 1 1 1] /VSamples [1 1 1 1] >> /GrayImageDict << /QFactor 0.15 /HSamples [1 1 1 1] /VSamples [1 1 1 1] >> /JPEG2000GrayACSImageDict << /TileWidth 256 /TileHeight 256 /Quality 30 >> /JPEG2000GrayImageDict << /TileWidth 256 /TileHeight 256 /Quality 30 >> /AntiAliasMonoImages false /CropMonoImages false /MonoImageMinResolution 1200 /MonoImageMinResolutionPolicy /OK /DownsampleMonoImages true /MonoImageDownsampleType /Bicubic /MonoImageResolution 1200 /MonoImageDepth -1 /MonoImageDownsampleThreshold 1.50000 /EncodeMonoImages true /MonoImageFilter /CCITTFaxEncode /MonoImageDict << /K -1 >> /AllowPSXObjects false /CheckCompliance [ /None ] /PDFX1aCheck false /PDFX3Check false /PDFXCompliantPDFOnly true /PDFXNoTrimBoxError false /PDFXTrimBoxToMediaBoxOffset [ 0.00000 0.00000 0.00000 0.00000 ] /PDFXSetBleedBoxToMediaBox true /PDFXBleedBoxToTrimBoxOffset [ 0.00000 0.00000 0.00000 0.00000 ] /PDFXOutputIntentProfile (Coated FOGRA27 \050ISO 12647-2:2004\051) /PDFXOutputConditionIdentifier (FOGRA27) /PDFXOutputCondition () /PDFXRegistryName (http://www.color.org) /PDFXTrapped /False /CreateJDFFile false /Description << /ENU >> /ExportLayers /ExportVisibleLayers /Namespace [ (Adobe) (Common) (1.0) ] /OtherNamespaces [ << /AsReaderSpreads false /CropImagesToFrames true /ErrorControl /WarnAndContinue /FlattenerIgnoreSpreadOverrides false /IncludeGuidesGrids false /IncludeNonPrinting false /IncludeSlug false /Namespace [ (Adobe) (InDesign) (4.0) ] /OmitPlacedBitmaps false /OmitPlacedEPS false /OmitPlacedPDF false /SimulateOverprint /Legacy >> << /AddBleedMarks false /AddColorBars false /AddCropMarks true /AddPageInfo false /AddRegMarks false /BleedOffset [ 8.503940 8.503940 8.503940 8.503940 ] /ConvertColors /NoConversion /DestinationProfileName () /DestinationProfileSelector /NA /Downsample16BitImages true /FlattenerPreset << /PresetSelector /HighResolution >> /FormElements false /GenerateStructure false /IncludeBookmarks false /IncludeHyperlinks false /IncludeInteractive false /IncludeLayers false /IncludeProfiles false /MarksOffset 6 /MarksWeight 0.250000 /MultimediaHandling /UseObjectSettings /Namespace [ (Adobe) (CreativeSuite) (2.0) ] /PDFXOutputIntentProfileSelector /DocumentCMYK /PageMarksFile /RomanDefault /PreserveEditing true /UntaggedCMYKHandling /LeaveUntagged /UntaggedRGBHandling /LeaveUntagged /UseDocumentBleed false >> << /AllowImageBreaks true /AllowTableBreaks true /ExpandPage false /HonorBaseURL true /HonorRolloverEffect false /IgnoreHTMLPageBreaks false /IncludeHeaderFooter false /MarginOffset [ 0 0 0 0 ] /MetadataAuthor () /MetadataKeywords () /MetadataSubject () /MetadataTitle () /MetricPageSize [ 0 0 ] /MetricUnit /inch /MobileCompatible 0 /Namespace [ (Adobe) (GoLive) (8.0) ] /OpenZoomToHTMLFontSize false /PageOrientation /Portrait /RemoveBackground false /ShrinkContent true /TreatColorsAs /MainMonitorColors /UseEmbeddedProfiles false /UseHTMLTitleAsMetadata true >> ] >> setdistillerparams << /HWResolution [2400 2400] /PageSize [612.000 792.000] >> setpagedevice