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Palynological study of the continental shelf sediments of the Labrador Sea 1986

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PALYNOLOGICAL STUDY OF THE CONTINENTAL SHELF SEDIMENTS OF THE LABRADOR SEA by V. EILEEN WILLIAMS A THESIS SUBMITTED IN PARTIAL FULFILMENT OF THE REQUIREMENTS FOR THE DEGREE OF DOCTOR OF PHILOSOPHY i n THE FACULTY OF GRADUATE STUDIES (Department o f G e o l o g i c a l S c i e n c e s ) We a c c e p t t h i s t h e s i s as c o n f o r m i n g t o t h e r e q u i r e d s t a n d a r d THE UNIVERSITY OF BRITISH COLUMBIA August 1986 (6) V. E i l e e n W i l l i a m s , 1986 In presenting this thesis in partial fulfilment of the requirements for an advanced degree at the University of British Columbia, I agree that the Library shall make it freely available for reference and study. I further agree that permission for extensive copying of this thesis for scholarly purposes may be granted by the head of my department or by his or her representatives. It is understood that copying or publication of this thesis for financial gain shall not be allowed without my written permission. Department of The University of British Columbia 1956 Main Mall Vancouver, Canada V6T 1Y3 Date QcTV&eK /9&6 DE-6(3/81) ABSTRACT A detailed palynological examination was made of Tertiary pollen and spore assemblages from six exploratory wells located along the conti - nental margins of the Labrador Sea. From north to south, the study wells are Kangamiut 1, Hekja 0-71, Karlsefni A-13, Herjolf M-92, Roberval K-92 and Cartier D-70. Using local extinction events of zonally diagnostic species to define the tops of intervals, eight provi- sional pollen and spore zones were established. The zones and their relative ages are as follows: Tsuga igniculus (middle to late Miocene); Fagus granulata (early to middle Miocene); Parviprojectus sp. A (early Oligocene); Araliaceoipollenites megaporifer ( latest Eocene/earliest Oligocene); Rhoipites latus (middle to late Eocene); Pistillipollenites mcgregorii (early to middle Eocene); Tricolpites sp. A (middle to late Paleocene); and Paraalnipollenites alterniporus (early to middle Paleocene). The middle and upper Oligocene is apparently absent in the study welIs. When used in conjunction with dinoflagellate assemblages, the zonation provides the potential for additional biostratigraphic resolution in the Tertiary marine sediments of the Labrador Sea. It is especially useful in upper Eocene and stratigraphical ly higher sections in which pollen and spores are the dominant component of the palynoflora: In addition, the basic s imilar ity of pollen and spore assemblages across much of i i northern and western Canada suggests the zonation may also be success- fu l ly applied in those regions. The relative abundance and distr ibution of four major populations ( i . e . , Paleozoic, Upper Jurassic/Lower Cretaceous, Upper Cretaceous and Paleogene) of redeposited palynomorphs were determined. The species composition of recycled and in-s i tu Paleogene palynomorphs supports i n - dependent clay mineralogical data that much of the sediment (including a high percentage of the palynomorphs) was delivered to offshore Labrador Sea basins via a "super" river system that drained a large portion of the western inter ior and Arct ic regions of Canada during the Tertiary. The taxonomic composition of the indigenous Paleogene pollen and spore f lora supports both paleontol.ogical and isotope data that relat ively high paleotemperatures prevailed at high northern latitudes during the Paleogene. The climatic optimum in the Labrador Sea region was reached in the early to early-middle Eocene. i i i TABLE OF CONTENTS ABSTRACT 11 i LIST OF FIGURES v i i i ACKNOWLEDGEMENTS x CHAPTER 1. GENERAL INTRODUCTION TO PALYNOLOGICAL STUDY OF THE CONTINENTAL SHELF SEDIMENTS OF THE LABRADOR SEA 1 Geological History of the Labrador Sea 5 Lithostratigraphy 7 Precambrian 7 Paleozoic 8 Mesozoic and Cenozoic 9 Thesis Format 18 References Cited 21 CHAPTER 2. PROVISIONAL TERTIARY POLLEN AND SPORE ZONATION OF THE CONTINENTAL SHELF SEDIMENTS OF THE LABRADOR SEA Introduction 23 Previous Work 27 Palynological Zonation 31 1. Tsuga igniculus Interval Zone 33 2. Fagus granulata Interval Zone 36 3. Parviprojectus sp. A Interval Zone 38 4. Araliaceoipollenites megaporifer Interval Zone 41 5. Rhoipites latus Interval Zone 43 6. Pistillipollenites mcgregorii Interval Zone 45 7. Tricolpites sp. A Interval Zone 47 8. Paraalnipollenites alterniporus Interval Zone 50 i v Distribution of Provisional Zones in Study Wells 52 Comparison of Labrador Sea Palynological Zonations 63 Discussion 67 Conclusions 72 References Cited 75 Explanation of Plates 82 Plate 1 83 Plate 2 86 Plate 3 89 Plate 4 93 CHAPTER 3. THE IDENTIFICATION AND DISTRIBUTION OF RECYCLED PALYNOMORPHS IN THE CONTINENTAL SHELF SEDIMENTS OF THE LABRADOR SEA . Introduction 97 Cretaceous and Lower Tertiary Stratigraphy of the Labrador Sea ' 9 9 Identification of Recycled Palynomorphs 104 Categories of Recycled Palynomorphs 111 Paleozoic Group 111 Upper Jurassic/Lower Cretaceous Group 114 Upper Cretaceous Group 115 Results and Discussion 116 Summary 126 References 129 Explanation of Plate 133 Plate 1 134 v CHAPTER 4. PROVENANCE OF IN-SITU AND RECYCLED PALEOGENE PALYNOMORPHS OF THE LABRADOR SEA Introduction 137 Recycled Palynomorphs as Indicators of Provenance 140 Results 143 Discussion 148 Conclusions 158 References 160 CHAPTER 5. PALEOGENE PALEOCLIMATIC TRENDS OF THE LABRADOR SEA REGION Introduction 165 Study Area 167 Results and Discussion 170 Early to Middle Paleocene 173 Late Paleocene 175 Early to Early-Middle Eocene 176 Late Eocene to Early Oligocene 179 Conclusions 181 References 183 CHAPTER 6. SUMMARY 189 BIBLIOGRAPHY 194 APPENDIX 210 Tertiary Pollen and Spore Range Chart: Kangamiut 1 211 Tertiary Pollen and Spore Range Chart: Hekja 0-71 212 Tertiary Pollen and Spore Range Chart: Karlsefni A-13 213 vi Tertiary Pollen and Spore Range Chart Herjolf M-92 Tertiary Pollen and Spore Range Chart Roberval K-92 Tertiary Pollen and Spore Range Chart Cartier D-70 LIST OF FIGURES CHAPTER 1 Figure 1. Figure 2. Page Location map.of the Labrador Sea and the eight offshore wells used in this study. Generalized 1ithostratigraphic columns of of f - shore Labrador and West Greenland (not to scale) 10 CHAPTER 2. Figure 1. Figure 2. Figure 3. Figure 4. Figure 5. Location map of the Labrador Sea and the six offshore wells used in this study. 25 Generalized 1ithostratigraphic columns of the Tertiary sections of the six study wells. 26 Ranges of selected pollen and spores used to establish provisional zones. 34 Distribution of provisional pollen and spore interval zones in the six study wells. 53 Comparison of previously established Tertiary Palynological zonations of the Labrador Sea and the provisional pollen and spore zones. 64 CHAPTER 3. Figure 1. Location map of the Labrador Sea and.the seven offshore wells used in this study. 98 Figure 2. Generalized 1ithostratigraphic columns of of f - shore Labrador and West Greenland (not to scale). 101 Figure 3. Summary of methods used to help identify different groups of redeposited palynomorphs in the Cretaceous and Tertiary shelf sediments of the Labrador Sea. 112 Figure 4. Distribution of relative abundances of recycled Paleozoic (1), Upper Jurassic/Lower Cretaceous (2), and Upper Cretaceous (3) palynomorphs in seven Labrador Sea wells. 117 v i i i CHAPTER 4. Figure 1. Location map of the Labrador Sea and the seven offshore wells used in this study. 138 Figure 2. Generalized 1ithostratigraphic columns of the Tertiary sections of the seven study wells. 144 Figure 3. Distribution of relat ive abundances of Paleogene recycled palynomorphs in the Paleogene sediments of the Labrador Sea. 146 Figure 4. Schematic diagram showing possible drainage patterns of r iver systems supplying sediments to the Labrador Sea during the Tertiary as proposed by McMillan, 1973. 150 CHAPTER 5. Figure 1. Location map of the Labrador Sea and the six offshore wells used in this study. 166 Figure 2. Generalized 1ithostratigraphic columns of the Tertiary sections of the six study wells. 168 ix ACKNOWLEDGEMENTS I gratefully acknowledge Aquitaine Company of Canada Ltd. (now Canterra) and their former senior geologist, Dr. N. J . McMillan, for sponsoring the research and supplying financial support on behalf of the petroleum exploration Labrador and Baffin-Labrador Groups. I thank the members of my thesis committee, Drs. G. E. Rouse, N. J . McMillan, W. H. Mathews and J . W. Murray for their c r i t i c a l reading of the manuscript and their many helpful comments and suggestions. I am particularly grateful to G. E. Rouse for his continued support, his technical and professional guid- ance and, most of a l l , his patience and bel ief in my work. I also wish to thank D. Mclntyre and R. J . Witmer for their editing assistance and helpful discussions. Special thanks as well to G. L. Williams and J . P. Bujak for their help during my .study of offshore eastern Canadian mate- r ia l at the G.S.C. in Dartmouth, N.S. I thank Unocal for the use of their computer f a c i l i t i e s and other technical help. Thanks also to J . Shepherd, K. Travis and B. Bi l l ings for laboratory work and J . Odermatt for computer assistance. Last, but certainly not least, I would l ike to thank my friends and family members who were so very supportive of me and my work; in particular I wish to mention J . G. Rogers, L. V. Street-Dee, C. D. Sadie, A. Pendragon and my husband, J . F. Williams. x CHAPTER 1. GENERAL INTRODUCTION TO PALYNOLOGICAL STUDY OF THE CONTINENTAL SHELF SEDIMENTS OF THE LABRADOR SEA The continental margins of the Labrador Sea and their structural con- figuration provide a favorable setting for petroleum exploration. The Labrador Sea is situated between Labrador and western Greenland ap- proximately between the latitudes of 53° and 66°N (see Figure 1 for a map of the region). Southern Baffin Island and Davis Strait mark the northern boundary of the basin and, to the south, i t is bounded by the Cartwright Arch and the Farewell Fracture Zone. The continental shelves extend offshore for tens of kilometers and, beyond an inner belt of Precambrian rocks, are characterized by thick sequences of predominantly Cretaceous and Tertiary sediments with isolated outl iers of Paleozoic strata. During the past couple of decades, numerous mag- netic and seismic geophysical surveys have been taken across the va r i - ous basins and in 1971 the f i r s t exploratory well was d r i l l ed off southern Labrador. Since then, over 25 wells have been dr i l l ed on the continental shelves of Labrador, southern Baffin Island and western Greenland. Significant hydrocarbon discoveries have been found in se- veral wells off Labrador and southern Baffin Island and the discovery of additional o i l and gas reserves are anticipated (McMillan, 1980). This intensive d r i l l i n g act iv i ty has provided numerous cuttings and sidewall core samples for paleontological, geochemical and sedimentological analyses, which have resulted in the generation of a 1 Figure 1. Location map of the Labrador Sea and the eight offshore wells used in this study. large volume of data regarding the shelf sediments and geological his- tory of the Labrador Sea. To help aid the understanding of the stratigraphy and paleoecology of the region, the palynology of se- lected Cretaceous and Tertiary intervals of seven Labrador Sea wells were examined in deta i l . The objectives of this research were to: (1) establish a provisional palynological zonation of the T e r t i - ary marine sediments of the Labrador Sea based on pollen and spores, to be used as a framework for more detailed biostratigraphic studies; (2) identify various different age-categories of recycled palynomorphs and determine their relative distribution through time along the Labrador shelf; (3) interpret the l ike ly provenance of the Paleogene sediments of the Labrador Sea based upon the palynofloral composition of contemporaneous and recycled palynomorph assemblages; and (4) interpret the general paleoclimatic trends that persisted in the general Labrador Sea region during the Paleogene. Seven Labrador Sea wells were examined in deta i l . From north to south they are Kangamiut 1, Hekja 0-71, Karlsefni A-13, Skolp E-07, Herjolf M-92, Roberval K-92 and Cartier D-70. An eighth well, Snorri J-90, 3 was examined for recycled palynomorphs. The location of each of the study wells is shown in Figure 1. Prepared palynological slides of selected sections from Kangamiut 1, Karlsefni A-13, Skolp E-07, Herjolf M-92 and Cartier D-70 were provided on loan from Total-Eastcan. The sampling interval for most of these samples was broadly spaced (approximately 100 meters); and cuttings were the most predominant type of sample used. Washed cuttings from Roberval K-92 and unwashed cuttings from Hekja 0-71 were provided by Aquitaine of Canada Ltd. (now Canterra) and processed in the palynological labora- tory at the University of Br it ish Columbia. The Snorri J-90 samples were studied at the Atlantic Geoscience Center in Dartmouth, Nova Scotia, where they are on f i l e . The most northerly of the wells examined was Kangamiut 1, which l ies approximately 120 kilometers offshore West Greenland at latitude 66°N. Dr i l led on a structural high, Kangamiut 1 penetrated Precambrian gneiss at a depth of 3874 meters (Henderson et a l . , 1980). Hekja 0-71 was d r i l l ed offshore southern Baffin Island to a depth of 4566 meters. The basal 1000 meters of Hekja 0-71 is comprised of a lkal ic volcanics interbedded with chalky clays (Klose et a l . , 1982). At a depth of 3212 meters a gas/condensate zone in a Paleocene sand was discovered (McMillan, 1982). Of the f ive wells from offshore Labrador that were studied in deta i l , f a i r l y complete sections of Tertiary sediments were penetrated in 4 Karlsefni A-13, Herjolf M-92, Cartier D-70 and Roberval K-92. Upper Cretaceous marine and Lower Cretaceous f luvia l sands of the Bjarni Formation were encountered in Skolp E-07, Herjolf M-92 and Roberval K-92. In Roberval K-92, a thin Paleozoic carbonate was found beneath Lower Cretaceous volcanics of the Alexis Formation. The wells were d r i l l ed on elevated blocks associated with a northwest-southeast trending structural basin, the Eric Graben, which l ies roughly parallel to the east coast of Labrador. The graben is i n f i l l e d with a thick sequence of Lower Cretaceous, non-marine f luv ia l sediments of the Bjarni Formation. The f i r s t indication of o i l on the Labrador Shelf came from a core of the Bjarni sand in Roberval K-92 (McMillan, 1982). Although no significant hydrocarbon discoveries were made in any of the study wells, f ive large gas/condensate and one o i l show were reported from six other Labrador Sea wells. GEOLOGICAL HISTORY OF THE LABRADOR SEA Magnetic and seismic geophysical surveys of the Labrador Sea indicate a sea-floor spreading model for the origin of the Labrador Sea. The north-south trending mid-Labrador oceanic ridge is positioned approxi- mately midway between Labrador and West Greenland and represents the western arm of a t r ip le junction with the mid-Atlantic ridge. There is a gravity low in the middle of the basin which, is associated with 5 the median valley of the Labrador Sea ridge. Also, on the Labrador side of the ridge axis the structure is progressively more disturbed from south to north (Hinz et a l . , 1979; and Srivastava et a l . , 1980). Van der Linden (1975), Srivastava (1978), Hinz et a l . (1979), Umpleby (1979), Gradstein and Srivastava (1980), Grant (1980), McWhae (1981) and Srivastava et a l . (1980) discuss in detail the history of the Labrador Sea. The i n i t i a l stage of the break-up between Greenland and Labrador was characterized by an updoming of the continental crust followed by r i f t i ng . During up l i f t , normal faulting perpendicular to the present Labrador coastline formed horst and graben structures. Thick sequences of non-marine f luv ia l sediments were shed into the newly formed structural basins. Lamprophyre dikes on southern Labrador and western Greenland and basalt flows on the Labrador and, possibly, the southern Baffin Island shelves indicate an Early Cretaceous age for the r i f t i n g . Eventually, oceanic material was cre- ated and actual sea-floor spreading commenced during Anomaly 32 time (Gradstein and Srivastava, 1980). The actual location of the continental-oceanic crust boundary in the Labrador Sea is uncertain however. The ear l iest marine sediments identif ied palynologically (Barss et a l . , 1979; this study) on the Labrador shelf indicate that the incursion of marine waters into the newly formed basin did not oc- cur until the early Late Cretaceous (Cenomanian to Coniacian). The opening phase of the Labrador Sea coincided with a widespread marine transgression that persisted into the Eocene (Gradstein and Berggren, 6 1981). By the late Eocene, just i ty in the Labrador-Baffin Bay tions were generally replaced by Srivastava, 1980). prior to Anomaly 13, spreading act iv- region ceased and deeper water condi- shallow marine facies (Gradstein and LITHOSTRATIGRAPHY PRECAMBRIAN The structurally complex Precambrian geology and orogenic history of the Labrador, southern Baffin Island and West Greenland region are discussed by Higgs (1977), Umpleby (1979) and S-ri vastava et a l . (1980). Precambrian Shield rocks outcrop extensively on landmasses surrounding the Labrador Sea. In eastern Labrador three Precambrian structural provinces are present. Granitic and granodioritic gneisses of the Nain Province l i e along Labrador's east coast. West of the Nain Province, the northern coast of Labrador and Baffin Island l i e within the Churchill Province which is characterized by high-grade metamorphics (e.g., migmatites, granulites and granulit ic gneisses) and anorthosite plutonics. The southern coast of Labrador is included in the Grenville Province. Though small outcrops of metasediments are present, i t is mainly characterized by amphibolite-granulite facies metamorphics cut by igneous intrusives. The Precambrian of western Greenland is characterized by acidic plutonics and supracrustal 7 metasediments and metavolcanics. Seismic reflectors and well data show that Precambrian shield rocks extend seaward and underlie thick wedges of Cretaceous and Tertiary sediments of the Labrador and West Greenland continental margins. These basement rocks were penetrated in Kangamiut 1, Karlsefni A-13, Herjolf M-92, Cartier D-70 and Roberval K-92 which were d r i l l ed on structural highs. PALEOZOIC Paleozoic rocks are poorly represented in Labrador Sea sediments and on adjacent landmasses. They represent isolated remnants of a sedimentary cover that was la id down in a Lower Paleozoic epeiric sea. Epeirogenic up l i f t associated with the Taconic and Acadian Orogenies of the Appalachian System to the south helped cause the retreat of the sea from the Labrador-West Greenland region (McWhae, 1981). Outliers of Ordovician and Carboniferous carbonates preserved in the Eric Graben have been penetrated in several wells d r i l l ed on the Labrador Shelf. The locations of these outl iers are important because of their gas reservoir potential. Other occurrences of Paleozoic rocks in the area include some Lower Paleozoic errat ics and some outl iers of Cambrian rocks along Labrador's southern coast. In West Greenland there is an outcrop of breccia which contains some Lower Paleozoic ma- rine rocks, and off southern Baffin Island, Ordovician and possibly 8 Si lurian carbonates were dredged and d r i l l ed by the Atlantic Geoscience Center (McMillan, 1980). MESOZOIC AND CENOZOIC The Mesozoic and Cenozoic rocks of the continental shelves of the Labrador Sea are primarily comprised of thick sequences of Cretaceous and Tertiary shales, mudstones and sandstones. Volcanics associated with episodes of tectonism are also found. Schematic 1ithostratigraphic columns of offshore Labrador and West Greenland are i l lustrated in Figure 2. The oldest Mesozoic rocks found to date on the continental shelves of the Labrador Sea are volcanics. On the Labrador shelf they form the Alexis Formation which is characterized by repeated sequences of weathered and hydrothermally altered, grey to purplish to green-grey volcanics. The type section of the Alexis Formation was designated by Umpleby (1979) in the Bjarni H-81 well off southern Labrador. It was also penetrated in Leif M-48, Indian Harbour M-52, Roberval K-92 and Herjolf M-92. The Alexis Formation rests unconformably on much older Paleozoic and/or Precambrian basement rocks. The hiatus is regionally widespread and represents the Labrador Unconformity (McWhae, 1981). The top of the section varies depending upon location. Absolute K-Ar isotope dates on the volcanics range from approximately 104 to 139 Ma (McWhae and Michel, 1975). Assuming the latter age date is correct, 9 LABRADOR SHELF* WEST GREENLAND SHELF* 1 Figure 2. Generalized 1ithostratigraphic columns of offshore Labrador and West Greenland (not to scale). Based on Umpleby (1979)*, McWhae et a l . (1980)* and Rolle (1985)**. 10 on the Harland et al (1982) geologic time scale the Alexis Formation was formed during the Early Cretaceous between latest Berriasian and late Barremian times. King and McMillan (1975) report sedimentary breccias cut by lamprophyre dikes on the east shore of Ford's Bight in southern Labrador. The dikes have been dated Early Cretaceous and are probably coeval with the Alexis Formation. Early Cretaceous volcanics may also be present on the southern Baffin Island shelf. The volcanism of the Alexis Formation marks the commencement of r i f t i ng in the Labrador Sea region prior to sea-floor spreading. The good stratigraphic control established in the petroleum explora- tory wells d r i l l ed along the continental margin of Labrador provides more information about the Mesozoic and Cenozoic rock sequence of the Labrador shelf than in the rest of the area. Based upon the work of Umpleby (1979), McWhae et a l . (1980) and McMillan (1982), the Labrador shelf sedimentary units are br ief ly described in the next few pages. Bjarni Formation. The type section of the Bjarni Formation is located in Herjolf M-92 (Umpleby, 1979). It is characterized by non-marine, deltaic sediments consisting of mainly l ight brown to dark gray, coarse-grained arkosic sandstones. S i l ty shale and thin coal layers are found interbedded sporadically throughout the sands. Shales within the formation have been dated palynologically by Williams (Barss et a l . , 1979) who as- signed an age ranging from Barremian to Albian. The top of the Bjarni 11 Formation is marked by the Avalon Unconformity (McWhae, 1981) which separates Bjarni continental molasse deposits from the overlying Markland Formation. The Labrador Unconformity separates the Bjarni Formation from Precambrian and Paleozoic basement rocks and, loca l ly, i t rests disconformably on the Alexis Formation. It is possible that sedimentation of the basal Bjarni Formation sands was contemporaneous with the youngest basalts of the Alexis Formation. Markland Formation. The Markland Formation consists mainly of f ine- to very fine-bedded, green to dark grey shale and s i l t y shale with rare interbeds of si ltstone and sandstone. Thin dolomitic limestone beds are also lo - cal ly present. The lithology is indicative of a marine ner i t ic to up- per bathyal depositional environment. In several wells, notably Freydis B-87 and Skolp E-07, d r i l l ed along the Labrador shelf, a shal- low marine to paralic arenaceous facies is present, forming the Freydis Member of the Markland Formation. It consists of l ight grey f ine- to coarse-grained quartzose sandstone and poorly sorted arkosic sandstone. The type section of the Markland Formation is in the Bjarni H-81 well (McWhae et a l . , 1980). It is also found in Gudrid H-55, Herjolf M-92, Freydis B-87 and Skolp E-07. Based upon foraminifera (Gradstein and Srivastava, 1980) and dinoflagellate (Barss et a l . , 1979) studies, the Markland Formation ranges in age from Cenomanian to early Paleocene. The Avalon Unconformity (McWhae, 1981) separates the base of the marine Markland Formation from the 12 underlying continental deposits of the Bjarni Formation or, in some wells, from older basement rocks. Deposition of the Markland Forma- tion records the incursion of marine waters into the Labrador Sea basin upon sea-floor spreading. Cartwright Formation. The Cartwright Formation was redefined by McWhae et a l . (1980) to i n - clude only the Tertiary section of the Cartwright Formation as defined by Umpleby (1979). It is characterized by a variety of l ithologies including brown-grey claystone, si ltstone and thin, fine-grained sandstone turbidite partings. Depending upon location, the Cartwright Formation rests conformably or disconformably on the more compact, uniform shales of the Markland Formation. This contact is easily d i s - tinguishable on seismic logs and represents McWhae's Bylot Unconform- i ty. The type section is located in Bjarni H-81 and i t is represented in most of the wells. Thickness of the Cartwright Formation varies from between 114 to 250 meters. Palynological and micropaleontological studies generally agree that the age of the Cartwright Formation ranges from middle Paleocene to early Eocene. Gradstein and Srivastava (1980) consider paleodepths as upper bathyal based upon benthic formaminiferal studies. Gudrid Formation. The Gudrid Formation is a quartzose and arkosic sandstone unit that is latera l ly equivalent to and interdigited with the Cartwright Forma- 13 t ion. It is also middle Paleocene to early Eocene in age. The type section is in the Gudrid H-55 well where i t forms an almost 200 meter thick continuous sandstone unit. In Cartier D-70 i t is divided into upper and lower tongues. The base of the formation rests on the Mark!and Formation at the Bylot Unconformity. The Gudrid Formation represents a turb id i t i c , deep-sea fan deposit. Foraminifera data (Gradstein and Srivastava, 1980) indicate these sands are deep ner i t i c . Mudstones (Kenamu Formation of McWhae et a l . , 1980). Sediments overlying the Cartwright Formation are characterized by brown-grey marine shales, si ltstones and fine-grained sandstone. The lower part is marked by a s l ight ly calcareous and s i l t y brown mudstone. Thin dolomitic limestone beds are found throughout the unit. Near the top of the section is an approximately 200 meter thick fine-grained, quartzose sandstone unit referred to as the Leif Sand. This unnamed Mudstone unit (Kenamu Formation) is well-represented in most of the wells. Foraminiferal studies (Gradstein and Srivastava, 1980) place the age of the sediments between early and late Eocene. Palynological studies (Barss et a l . , 1979; this study), on the other hand, indicate an early Eocene to ear l iest Oligocene age. Marine shelf and bathyal conditions prevailed during deposition of most of the mudstone; however, the l ight colored, clean Leif member sandstone is probably ner i t ic or t idal in orgin (Gradstein and Srivastava, 1980). 14 Mokami Formation. An approximately 700 meter-thick brownish claystone and shale with thin beds of s i l tstone, sandstone, calcareous sandstone and limestone overl ie, possibly unconformably, the mudstone (Kenamu Formation). The unit was named the Mokami Formation by McWhae et a l . (1980) and re- presents part of Umpleby's (1979) Saglek Formation and the lower Saglek Mudstone of McMillan (1982). The age of the Mokami is not well established. However, foraminiferal studies (Gradstein and Berggren, 1981) indicate that i t may range in age from early Oligocene to middle Miocene. Saglek Formation The Saglek Formation as defined by McWhae et a l . (1980) is the upper- most pre-Quaternary unit on the Labrador shelf. It is comprised of unconsolidated, white or brown to grey feldspathic and cherty sands with s i l t and clay interbeds. The sediment is poorly sorted and con- tains abundant pelycepod fragments and some l i gn i te. The unit is widespread on the Labrador shelf and reaches thicknesses of over 1000 meters in the northern part of the shelf. The top is bounded by poorly sorted, unconsolidated Quaternary glacial deposits at an ero- sional unconformity. It was laid down in a marginal to nearshore ma- rine depositional environment. Although an age is d i f f i c u l t to assign to the Saglek because of the paucity of indigenous palynomorphs and an abundance of recycled forms in the sediments, i t is probably late Miocene to Pliocene. 15 The general stratigraphy and structure of the southern Baffin Island continental shelf is br ie f ly described by McMillan (1982) and Klose et a l . (1982). Fair ly thick sequences of Cretaceous and Tertiary c las t ic and volcanic rocks rest unconformably on either local outl iers of Ordovician carbonates or Precambrian crystal l ine basement rocks. Much of our knowledge of the lithology comes from results of the two ex- ploratory wells, Hekja 0-71 and Gjoa G-37. Alkal ic vol cam'cs with interbedded shales and clays are found in the lower section of each well. The age of the volcanics is questionable. Potassium-argon dates on the lower basalts in Hekja 0-71 vary from 105 to 119 Ma whereas paleotological data indicates an early Paleocene age. In Gjoa G-37 the K-Ar age of the uppermost basalt is approximately 56 Ma. The lavas were probably extruded along transform faults identif ied by geophysical surveys of the area. In Hekja 0-71, the basalts are overlain by interbedded l ight colored sandstones (Hekja sand) and dark gray shales of Paleocene age. In Gjoa G-37 the sands are absent. Eocene and younger sediments generally consist of shallow ner i t ic to ner i t ic gray and brown interbedded shales, mudstones and si ltstones. Some coal may be local ly present. Henderson et a l . (1980), Manderscheid (1980) and Rolle (1985) discuss in detail the geology of the Cretaceous-Tertiary sedimentary basin offshore West Greenland. Near the Nussauq Embayment and Disko Island, 16 outcrops of Early Cretaceous upper delta-plain f luv ia l sediments are overlain by Upper Cretaceous and Paleocene marine mudstones and local interbeds of shale and sand. A thick sequence of Tertiary basalts cap the sediments. Offshore western Greenland, f ive dry exploratory wells between latitudes 64°20' and 70°N were d r i l l e d . Unlike the Labrador shelf, the sedimentary cover of the continental margin off southwest- ern Greenland is f a i r l y thin. Further north in the v ic in i ty of Baffin Bay, the shelf widens and the sediments are considerably thicker. Rolle (1985) of the Geological Survey of Greenland has divided the Up- per Cretaceous and Tertiary sedimentary sequence into seven new forma- tions (see Figure 2). The coarse-grained predominantly arkosic Narssarmiut Formation is discontinuous and generally equivalent to the Freydis Member of the Markland Formation along the Labrador shelf. The Ikermiut Formation is characterized mainly by a f a i r l y low-energy shelf to deep marine transgressive sequence of dark gray carbonaceous shaley mudstones. It is f a i r l y widespread and generally corresponds to the Late Cretaceous to Early Tertiary Markland and Cartwright For- mations from offshore Labrador. The Hel lef isk Formation is comprised generally of a gray to dark gray s i l t y mudstone with poorly sorted calcareous sandstone interbeds. It was found in only one of the wells and probably interfingers latera l ly with the Ikermiut Formation. The Eocene Nukik Formation, which has no direct equivalent along the Labrador shelf, is characterized by interbedded, f a i r l y thin turb id i t i c layers of unconsolidated sand and mud, arranged more or 17 less into a coarsening upwards sequence. Conformably overlying the Nukik is the late Eocene-01igocene Kangamiut Formation. It consists of a f a i r l y thick, predominantly unconsolidated sandstone with some interbeds of si ltstone and mud. There are apparently no 1ithological units equivalent to the Kangamiut on the western side of the Labrador basin. The Manitsoq Formation (01igocene? to Miocene) is character- ized by an upward-coarsening argillaceous arkose with interbeds of l ight gray s i l t y and sandy mudstone. It is widespread along the West Greenland shelf and is stratigraphical ly equivalent to the Saglek For- mation from offshore Labrador. The Manitsoq is overlain by Miocene to Pleistocene unconsolidated argillaceous fine sands and muds'. Rolle (1985) ca l l s this upper unit the Ataneq Formation, however, i t ' s over- a l l distr ibution is unknown as i t was found in only one of the wells. THESIS FORMAT The main text of the thesis has been divided into four major chapters, which are to be submitted separately for eventual publication. Though interrelated, each of these sections deals with a specif ic problem re- garding the palynology of the continental shelf sediments of the Labrador Sea. Preceding the main text is a an introductory chapter (CHAPTER 1) in which the purpose of the thesis is stated and the gen- eral geology of the Labrador Sea is described. The f inal chapter (CHAPTER 6) summarizes the main points discussed in the thesis and 18 enumerates the major conclusions which resulted from the study. A brief description of the main body of the thesis follows. The f i r s t major subject (CHAPTER 2) is stratigraphic rather than taxonomic and concerns the palynozonation of Tertiary sediments from the Labrador Sea. In this chapter, the results of my provisional pollen and spore zonation from six Labrador Sea wells are presented and compared with regional palynozones that were established by other workers who based their zones essential ly upon the stratigraphic oc- currences of dinoflagellates. What is being tested is whether or not the pollen and spores recovered from the predominantly marine Tertiary sediments can be used in conjunction with dinoflagellates and other marine algae to increase our biostratigraphic resolution along the continental shelves of the Labrador Sea. Charts showing the stratigraphic ranges of pollen and spore taxa found in the six wells used in this part of the study are located in the APPENDIX at the end of the thesis. The second and third parts of the main text (CHAPTERS 3 and 4) address the problem of redeposited palynomorphs. The former discusses the relative merits of the different parameters used to recognize recyclants. In addition, the distr ibution and relat ive abundances of different age-categories of recycled palynomorphs in the Cretaceous and Tertiary sections of seven of the study wells are discussed. The latter chapter, on the other hand, focuses on the provenance of the 19 abundant recycled and contemporaneous Paleogene palynomorphs from the Labrador Sea. The third major section (CHAPTER 5) of the thesis is interpretive and is based in part upon the results of the previous three chapters. Us- ing published l i terature that relates foss i l palynofloral assemblages with modern f lora l a f f i n i t i e s of known climatic tolerance, the contemporaneous Lower Tertiary pollen and spore assemblages from the Labrador Sea are used to help describe the major climatic trends of the region during the Paleogene. These trends are compared with Ter- t iary climatic patterns of the Canadian Arct ic , Alaska and Br i t i sh Columbia. Because each of these sections has been written as a separate paper, there is some repetition at the beginning of each chapter with regards to the study wells and the general geology. Also, at the end of each section is a l i s t of references cited in that particular chapter. A compilation of a l l of the references is located in the BIBLIOGRAPHY at the end of CHAPTER 6. 20 REFERENCES CITED Barss, M. S., J . P. Bujak and G. L. Williams, 1979. Palynological zonation and correlation of sixty-seven wells, eastern Canada. Geol. Surv. Can., Paper 78-24, 118 pp. Gradstein, F. M. and W. A. Berggren, 1981. Flysch-type agglutinated Foraminifera and the Maestrichtian to Paleogene his- tory of the Labrador and North Seas. Marine Micropaleontology, 6, 211-268. Gradstein, F. M. and S. P. Srivastava, 1980. Aspects of Cenozoic stratigraphy and paleoceanography of the Labrador Sea and Baffin Bay. Palaeogeogr., Palaeoclimatol., Palaeoecol., 30, 261-295. Grant, A. C , 1980. Problems with plate tectonics: the Labrador Sea. Bul l . Can. Petrol. Geo!., 28, 252-278. Harland, W. B., A. V. Cox, P. G. Llewellyn, C. A. G. Pickton, A. G. Smith and R. Walters, 1982. A geologic time scale. Cambridge: University Press, 131 pp. Henderson, G., E. J . Scheiner, J . B. Risum, C. A. Croxton and B. B. Anderson, 1981. The west Greenland basin, in J . W. Kerr and A. J . Fergusson (eds.), Geology of the North Atlantic Borderlands. Can. Soc. Petrol. Geol., Memoir 7, 399-428. Higgs, R. Y., 1977. Provenance of Mesozoic and Cenozoic si 1 ic ic las t i c sediments of the Labrador and West Greenland continental margins. M. Sc. Thesis, U. of Calgary, Calgary, A l ta . , 169 pp. Hinz, K., H. U. Schluter, A. C. Grant, S. P. Srivastava, D. Umpleby and J . Woodside, 1979. Geophysical transects of the Labrador Sea: Labrador to southwest Greenland. Tectonophysics, 59, 151-183. King, A. F. and N. J . McMillan, 1975. A mid-Mesozoic breccia from the coast of Labrador. Can. J . Earth Sc i . , 12, 44-51. Klose, G. W., E. Matterre, N. J . McMillan and C. G. Zinkan, 1982. Petroleum exploration offshore southern Baffin Island, northern Labrador Sea, Canada, in A. Embry (ed.), Third International Symposium on Arctic Geology. Can. Soc. Petrol. Geol., Memoir 8, 233-244. 21 Manderscheid, G., 1980. The geology of the offshore sedimentary basin of West Greenland, in A. D. Mi al1 (ed.), Facts and Principles of World Oil Occurrence. Can. Soc. Petrol. Geo!., Memoir 6, 951-973. McMillan, N.J., 1980. Geology of the Labrador Sea and i t s petroleum potential. in Tenth World Petroleum Congress, Bucharest, 1979, Proceedings, 2, 165-175. , 1982. Canada's East Coast: the new super petroleum province. J . Can. Petrol. Technology, 21, 1-15. McWhae, J . R. H., 1981. Structure and spreading history of the Northwestern Atlantic from the Scotian Shelf to Baffin Bay. in J . W. Kerr and A. J . Fergusson (eds.), Geology of the North Atlantic Borderlands. Can. Soc. Petrol. Geol., Memoir 7, 299-332. McWhae, J . R. H. and W. F. E. Michel, 1975. Stratigraphy of Bjarni H-81 and Leif M-48, Labrador shelf. Bul l . Can. Petrol. Geo!., 23, 361-382. McWhae, J . R. H., R. E l ie , K. C. Laughton and P. R. Gunther, 1980. Stratigraphy and petroleum prospects of the Labrador shelf. Bul l . Can. Petrol. Geol., 28, 460-488. Rolle, F., 1985. Late Cretaceous-Tertiary sediments offshore central West Greenland: 1ithostratigraphy, sedimentary evolution, and petroleum potential. Can. J . Earth Sc i . , 22, 1001-1019. Srivastava, S. P., 1978. Evolution of the Labrador Sea and i t s bearing on the early evolution of the North At lant ic. Royal Astronomical Society, Geophysical J . , 52, 313-357. Srivastava, S. P., R. K.. H. Falconer and B. MacLean, 1980. Labrador Sea, Davis Stra i t , Baffin Bay: Geology and geophysics—a review, in J . W. Kerr and A. J . Fergusson (eds.), Geology of the North American Borderlands. Can. Soc. Petrol. Geo!., Memoir 7, 333-398. Umpleby, D. C , 1979. Geology of the Labrador shelf. Geol. Surv. Can., Paper 79-13, 34 pp. Van der Linden, W. J . M., 1975. Mesozoic and Cainozoic opening of the Labrador Sea, the North Atlantic and the Bay of Biscay. Nature, 253, 320-324. 22 CHAPTER 2. PROVISIONAL TERTIARY POLLEN AND SPORE ZONATION OF THE CONTINENTAL SHELF SEDIMENTS OF THE LABRADOR SEA INTRODUCTION Pollen and spores are commonly found in association with dinoflagellates in marine sediments. Their dispersal in the marine realm is influenced in large part by both the distance and mechanism of transport as well as by the hydrodynamic properties of the grains themselves. Significant concentrations exhibiting the greatest amount of diversity are most commonly associated with nearshore marine, delta lobe and turbidite sedimentary environments. Nevertheless, the strati graphic u t i l i t y of pollen and spores in marine sediments is of- ten overlooked in l ieu of dinoflagellate assemblages which are part ic- ularly suitable for defining zones. In intervals where the concentration of dinofTagellates in comparison to pollen and spores is low, or where only long-ranging dinoflagellate species persist, how- ever, pollen and spore assemblages can be very useful for establishing biostratigraphic control. Although the Cenozoic continental shelf sediments of the Labrador Sea have yielded a f a i r l y diverse and abundant terrestr ia l microflora, pollen and spores have not been used up to this time to establish a biostratigrphic zonation for the Tertiary sediments of the Labrador 23 Sea. Previously established palynological zonations by Williams (in Gradstein and Williams, 1976; Williams and Bujak, 1977; Barss et a l . , 1979) and Ioakim (1979) are based almost exclusively upon dinoflagellate assemblages. Therefore, the Tertiary pollen and spore assemblages from six Labrador Sea wells (Figure 1) were examined in detail for the purpose of determining their biostratigraphic potential in the Labrador Sea region. Four of the wells, Karlsefni A-13, Herjolf M-92, Roberval K-92 and Cartier D-70 (from north to south), are located along the Labrador continental shelf. Hekja 0-71 l ies off the southern t ip of Baffin Island and Kangamiut 1 is situated off the west coast of Greenland. The generalized lithology and stratigraphic distribution of the T e r t i - ary sections studied in each of the wells are i l lustrated in.Figure 2. The dominant l ithologies represented in the wells consist of shales, mudstones, si ltstones and sandstones (Umpleby, 1979; McWhae et a l . , 1980; McWhae, 1981; McMillan, 1980, 1982). Foraminiferal data (Gradstein and Williams, 1981), from six offshore Labrador wells ( i n - cluding Karlsefni A-13, Herjolf M-92 and Cartier D-70) suggests bathyal (slope) to deep ner i t ic deposition in the Paleocene and Eocene and a shift towards shallow ner i t ic to marginal marine in the upper Oligocene, Miocene and Pliocene. Information from Karlsefni A-13 also suggests that non-marine deposition prevailed along the northern part of the shelf during much of the Miocene. 24 Figure 1. Location map of the Labrador Sea and the six offshore wells used in this study. 25 DEPTH IN METERS -1000 KANGAMIUT 1' HEKJA 0-71*2 KARLSEFNI A-13* HERJOLF M-92' ROBERVAL K-92* CARTIER D-70" -3000 NUKIK FM m u> UPPER MDST LEIF SS LOWER MDST CARTWR. FM. LABRADOR " SM. AGlEfl FM M U D ST O N E Z—L~- ttIF MBR K EN A M U  FO RM A TI O N ~~2 - CA RT W RI G H T FO RM A TI O N IAMUA1IO FM. CAHTIM SS, CAH1WR FM I CARU ia ' ss UIF SS ui o HORIZONTAL BARS TO THE RIGHT OF EACH COLUMN REPRESENT SAMPLE LOCATIONS. '•STRATIGRAPHY AFTER ROUE. 1385 •'STRATIGRAPHY AFTER KLOSE ET Al, 1982 'STRATIGRAPHY AFTER TOTAL-EASTCAN ro Figure 2. Generalized 1ithostratigraphic columns of the Tertiary sections of the six study wells. The stratigraphic ranges of over 130 pollen and spore as well as 100 dinoflagellate species were recorded from 171 samples. Prepared palynological slides of selected Tertiary sections from Kangamiut 1, Karlsefni A-13, Herjolf M-92 and Cartier D-70 were provided on loan from Total-Eastcan courtesy of Dr. N. J . McMillan, then of Aquitaine. Most of these samples consisted of cuttings, although a few sidewall core samples were also made available. In addition, raw cuttings samples from Hekja 0-71 and washed cuttings from Roberval K-92 were provided by Aquitaine (now Canterra) and processed at the University of Br i t i sh Columbia. PREVIOUS WORK Since the commencement of d r i l l i n g in the circum-Labrador Sea region in 1971, two palynological zonations of Tertiary Labrador shelf sediments have been published. Both zonations are based primarily on local extinction events of zonally diagnostic dinoflagellate species. A preliminary palynological examination of Cenozoic Labrador Shelf sediments was made and reported by Williams and Bujak (1977). Subse- quent to this i n i t i a l informal palynozonation, Williams (Barss et a l . , 1979) expanded the data base to encompass eleven wells including Karlsefni A-13, Herjolf M-92 and Cartier D-70. A total of ten 27 Cenozoic assemblage zones were ident i f ied. With the exception of the PIiocene-Pleistocene which was defined by the presence and abundance of the conifer pollen Tsuga igniculus, range tops of dinoflagellates were used to characterize the remaining zones. The distr ibution of zones as well as a l i s t of selected palynomorphs found associated within individual zones are described for each well in Barss et a l . , 1979. The middle to late Miocene Operculodinium centrocarpum assemblage and early Miocene Paralecaniella indentata assemblage are present in the majority of wells as are the middle to late Eocene Wetzeliella lunaris and early Eocene Areoligera senonensis assemblages. Generally, the Paleocene is divided into two zones, the early Paleocene Palaeoperidinium pyrophorum and the late Paleocene Deflandrea speciosa assemblages. However, a middle Paleocene Alisocysta circumtabulata assemblage is recognizable in four of the wells. The middle to late Oligocene is absent or poorly defined throughout most of the wells. The informal biostratigraphic zones established by Williams have pro- vided a useful biostratigraphic framework for more detailed palynological studies of Labrador Sea sediments. Ioakim (1979), as part of her doctoral dissertation, palynologically examined the Eocene and Paleocene sections of two southern Labrador shelf wells (Bjarni H-81 and Freydis B-87). Over 120 species of dinoflagellates were re- corded. The highest stratigraphic occurrences of selected species were used to define ten Eocene (six within the lower Eocene) and two 28 Paleocene zones. Most of the Eocene zones were based upon local ly re- str icted ranges of species Ioakim identif ied within the Wetzeliella-Apectodinium complex ( i . e . , Wetzeliella, Rhombodinium, Kisselovia, Dracodinium and Apectodinium) of dinof1agel1ates. The range top of Palaeoperidinium pyrophorum divides the early from the late Paleocene, the upper l imit of which is defined by the last strati graphic appearance of Deflandrea speciosa. A preliminary palynostratigraphic study of the Kangamiut 1 well was made by Croxton (1978). Although palynomorph recovery from the upper 2600 meters of the well was generally poor due to coarse-grained sandy 1ithologies, she was able to zone the remainder of the well. Using Williams' informal dinoflagellate zonation scheme, Croxton recognized a middle to late Eocene Wetzeliella lunaris assemblage; early Eocene Areoligera senonensis assemblage; late Paleocene Deflandrea speciosa assemblage; and early Paleocene Palaeoperidinium pyrophorum assemblage. Her results suggest that dinoflagellate palynoassemblages from offshore southwestern Greenland and the Labrador shelf are correlative for at least the lower Tertiary. Foraminiferal faunas in Paleocene through Eocene Labrador Sea sediments are characterized by a predominance of benthic flysch-type agglutinated foraminifera. At the Eocene/01igocene boundary, the agglutinated forms essentially disappear and are replaced by calcareous benthic forms (Gradstein and Williams, 1976; Gradstein and 29 Srivastava, 1980). Planktic foraminifera have only an intermittent history on the Cenozoic Labrador shelf and, with the exception of cer- tain warm water, low latitude taxa in the early and middle Eocene, are characterized by middle to high latitude types comprising relat ively long-ranging forms with low species divers ity. Gradstein and Williams (1976) reported eight benthic foraminiferal zones of Cenozoic age from four Labrador Sea and northern Grand Banks wells. With an expanded data base which included Karlsefni A-13, Herjolf M-92 and Cartier D-79, Gradstein and Agterberg (1981) used a probabi l i s t ic , quantitative approach to zoning both benthic and planktic foraminiferal assemblages. With their method, they were able to erect a well-delineated, nine-fold stratigraphic subdivision of the Tertiary. Gradstein and Srivastava (1980) discussed the regional stratigraphy and distr ibution of planktic as well as benthic foraminifera in the Labrador Sea and Baffin Bay area, whereas Gradstein and Berggren (1981) compared the flysch-type agglutinated fauna of the Labrador Sea with those of the North Sea. Mi l ler et a l . (1982) examined Late Cretaceous and Early Tertiary deep sea sediment cores from DSDP Site 112 located in the southern Labrador Sea. They reported diverse agglutinated foraminiferal assemblages similar to those found on the Labrador shelf. 30 Detailed stratigraphic charts of the Labrador and Newfoundland shelves comparing planktic and benthic foraminiferal zones with palynological zones were published in Gradstein and Williams (1981). The foraminiferal zones are helpful in providing some chronostratigraphic control for assigning ages to palynozones. Thomas and Gradstein (1981) examined the stratigraphic distribution of diatoms in Tertiary sediments from offshore Eastern Canada? Three wells, including Karlsefni A-13, from the Labrador shelf were part of the study. Diatoms have a very low diversity and are comprised of es- sential ly four pyr it ized, discoid species. The authors found a broad correlation between Gradstein and Agterberg's (1981) foraminiferal zonation and diatom numerical peaks. In general, however, with the exception of an abundance peak of diatoms at the Paleocene/Eocene boundary, diatoms appear to have l i t t l e biostratigraphic value in the Labrador sea region. PALYNOLOGICAL ZONATION Eight provisional palynological interval zones based upon pollen and spores are proposed herein. According to the North American Commis- sion of Stratigraphic Nomenclature (1983), an interval zone is defined as the interval which l ies between successive biostratigraphic events. Because cuttings samples were mainly used in this study, local ex- 31 t inction events (range tops) are used to define the zones. The inter- vals are named after the species whose highest stratigraphic occurrence is used to define the upper l imit of a zone. The zone ex- tends stratigraphical ly downward to but not including the range top of the species defining the top of the immediately underlying zone. Be- cause of widely spaced sample intervals as well as the rar i ty of some of the zonally nominate species, the zones are considered informal. The zones are br ief ly discussed in the following pages in descending stratigraphic order. Included in their descriptions are the diagnos- t i c pollen and spores which best characterize each zonal assemblage. Although not always mentioned in the zone descriptions, gymnosperm pollen and monolete and t r i l e t e fern spores were ubiquitous throughout the wells and, in some horizons, the dominant elements within an assemblage. Some of the dinoflagellates associated with the pollen and spore zones are also included. Because most of the dinoflagellate species ident i - f ied in the study wells were also reported by Williams (Williams and Bujak, 1977; Barss et a l , 1979) and Ioakim (1979) from the Labrador shelf, the reader is referred to those publications for more detailed species l i s t s . The ranges of some of the more zonally diagnostic species of pollen and spores used to characterize the proposed zones are i l lustrated in 32 Figure 3 (see APPENDIX for more detailed range charts of pollen and spore occurrences recorded from each of the study wells). The range bases shown on the chart are not precisely defined because of the a l - most exclusive use of cuttings samples. Where botanical a f f i n - i t i e s with modern genera have been established (Frederiksen, 1969, 1980, 1985; Rouse, 1977), modern extant rather than foss i l form genus names are used. With regards to dating samples, relat ive ages have been provisionally assigned to the zones based mainly upon the well-documented stratigraphic ranges of age-diagnostic dinoflagellates from Canada, the Atlantic coastal plain of North America, North Atlantic and northwestern Europe. ' 1. Tsuga igniculus Interval Zone The top of the zone is defined by the range top of Tsuga igniculus (PI. 1, Fig. 1) and the base by the range top of Fagus granulata. Be- cause the zone represents the uppermost interval in the wells studied, the range top of i ts nominate species must be considered a r t i f i c i a l . For this reason, ranges of taxa that have their last stratigraphic ap- pearance at the top of the Tsuga igniculus zone may extend upwards into the overlying sediments. The T. igniculus zone is found in only two of the wells, Hekja 0-71 and Roberval K-92. It is characterized by a low diversity and re la - 33 AGE PROVISIONAL PALYNOLOGICAL INTERVAL ZONES £ . d o j £ « a « -» 5 e § S 5. 5 5 H ° § 5 s i s i l i r l l» O O O £ O OL < | 8 d S l g co co 5 P » I o Q. a * • E . « to a CD m 3 ̂  « § 3 ~ c 3 5 • 3 T f T T T T T T T T T T *4 i» S e T f "•SI o o « c « 8 i*t II 8 co g ta to ® =5 P * (5 >. a e 2 Ui «t » T f •o "£ co 2 | §| u b » o a ° o « Q. O ? a-£ £ E 0 o C3 S 1 T 5 Ii si <D ft $ DC 3 :< I f & i s» g, I a • & e to c s m o o ? a s-a- o 5 o o s •c -c o <S r- t T » T d | ? B 8 » at o a a S | -j s T T to <D c » a a ? <o o ? I s 81 & £ t a ^ n T T •3 a o <r 5 o H ce -Q » E . S ° a o * S- * s l i s a •2 E o * & "O o to O c 3 g. a J Co co * o co « a ft. Q. o £ <o a 6 Q. » a < a Q. • C C co * o y, (O 5) O O £ 3- = a. 5 * o a e ^ Q. or h- T T T E g> | a a w | E | « S i to * W OS to & -S -£ Q. E E E §. O O O -c S S £ T I T ? 2 o S f i I ago, ^1 * a c t S | a <o o - o a a- S ° - a £ a E g 111 » T T Tsuga Igniculus M. Fagus granulata Parvlprolectus sp. A L. Arallaceolpollenlles megaporller I I I I Rhoipites latus Pistillipollenites mcgregorii I I L. M. Trlcolpltes sp. A I I I I I I Paraalnlpollenltes allernlporus Figure 3. Ranges of selected pollen and spores used to establish provisional zones U J t ive ly sparse f lora l assemblage which is dominated by an abundance of Picea spp., Pinus spp. and Tsuga igniculus. Common to the assemblage are Osmunda (PI. 1, Fig. 2) and Laevigatosporites. Small numbers of the deciduous broadleaf tree pollen Alnus, Betula (Plate 1, Fig. 3), Quercus form B (PI. 1, Fig. 5) and Tilia are also present. Rare oc- currences of Chenopodipollis sp. (PI. 1, Fig. 4) and Gramineae (PI. 1, Fig. 5) spp. were also recorded. Although dinoflagellates within the zone are extremely rare, several were noted. These include a few specimens of Paralecaniella indentata, Operculodinium cf. 0. centrocarpum and an undescribed dinoflagellate cyst characterized by a smooth, medium sized, rounded to oval cavate form, in which the paratabulation is not indicated and the archeopyle type is uncertain. This species in informally referred to as Form sp. A herein. The age of the assemblage is d i f f i c u l t to determine. Whereas Norn's (1986) and Bujak )personal communication) report a late Miocene range top of Tsuga igniculus for the Canadian Arct ic , a Pleistocene range top for T. igniculus is reported from the Grand Banks and Scotian Shelf (Williams and Brideaux, 1975; Barss et a l . , 1979), as well as from the Pliocene/Pleistocene of the Labrador Sea (Barss et a l . , 1979; Mudie, personal communication). In l ight of the modern climatic t o l - erance and range of Tsuga in offshore eastern Canada (Mudie, 1982), i t is l ike ly that during the Pleistocene temperatures in the Labrador Sea 35 region would have been too cold to support i ts growth. The younger occurrences of T. igniculus may, therefore, represent recycled grains. Although a younger age can not be discounted, the T. igniculus assemblage in the study wells is interpreted as probable late middle to late Miocene. The f lora l elements, though less diverse, are simi- lar to those reported by Martin and Rouse (1966) from the Upper Skonun Formation on the Queen Charlotte Islands. Champigny et a l . (1981) correlated molluscan faunas within the Upper Skonun with the Wishkakan stage of coastal Washington State and the latest or post-Seldovian stage in Alaska which, according to Berggren and van Couvering's 1974 time scale, is 11-13 Ma. Also, Norris (1986) records the range top of T. igniculus from the southern Beaufort Sea to l i e within the Mackenzie Bay Formation, which he interprets as probable Miocene.. 2. Fagus granulata Interval Zone The top of the zone is defined by the range top of F. granulata (PI. 1, Figs. 6-7) and the base by the range top of Parviprojectus sp. A. The Fagus granulata zone is well-defined by i t s constituent pollen and spore assemblage. It is characterized by a greater diversity of deciduous, broadleaved tree pollen than in the overlying Tsuga igniculus zone. Some of the pollen include: Liquidambar forms A and B (PI. 1, Figs. 10-11), Quercus form A (PI. 1, Fig. 8), Juglans, 36 Ulmus, Carya, Pterocarya and T i l i a vescipites. Most of these taxa make their last stratigraphic appearance within the zone. Picea-Pinus, Taxodium, Sequoia (PI. 1, Fig. 12), Metasequoia, Tsuga igniculus, T. viridifluminipites (PI. 1, Fig. 13), ericaceous tetrads, Sphagnum and Laevigatosporites are common constituents of this palynomorph assemblage. Several dinoflagellate species were noted. Those making their last stratigraphic appearance in the zone are Cordosphaeridium cantharellum, Systematophora ancyrea, Paleocystodinium golzowense, Paralecaniella indentata, and Svalbardella sp. A. Even though the samples in this interval are marine, they are dominated by an abun- dance of ter res t r i a l l y derived organic matter, which can make finding dinoflagellates on a sample sl ide d i f f i c u l t . Fluorescence microscopy can be a useful tool for helping to locate dinoflagellates in such i n - tervals, especially i f the sample is unstained and the material on the slide is too densely distributed. An early Miocene age is assigned to this interval based mainly upon the range top of Cordosphaeridium cantharellum. The extinction of C. cantharellum in the early Miocene is recorded from the Grand Banks on the Atlantic continental margin of Eastern Canada (Williams and Brideaux, 1975; Williams and Bujak, 1977), the Atlantic coastal plain region of the southeastern United States (Stover, 1977) and the Norwegian-Greenland Sea (Manum, 1976). Although a l l of the aforemen- 37 tioned terrestr ia l f lora and dinoflagellate cysts associated within this zone have known ranges that extend down into the Oligocene, sup- port for an early Miocene age is furthered by the presence of Gramineae spp. at the base of the zone in a sidewall core sample from Karlsefni A-13. The f i r s t stratigraphic occurrence of Gramineae at high northern latitudes is in the early Miocene (Rouse, personal com- munication). Mudie (1985) has reported the presence of some of the species (e.g., Liquidambar and Juglans) that have their range tops within this zone in younger strata from the Artie and Labrador Sea. Because these spe- cies were not found in the overlying T. igniculus zone, plus the fact that Cordosphaeridium cantharellum and Systematophora ancyrea are present, indicates that the younger recorded occurrences by Mudie may represent redeposited grains. In order to better resolve and better document the range tops of some of these taxa, better sample control and additional sections need to be studied. 3. Parviprojectus sp. A Interval Zone The range top of Parviprojectus sp. A (PI. 1, Fig. 14) marks the top of the interval and the range top of Araliaceoipollenites megaporifer the base. The zone is generally characterized by the common occur- rence of triporate pollen including Corylus/Carpinus (PI. 1, Figs. 38 15-16) and Myrica (PI. 1, Fig. 17). Also characteristic of the assemblage though not restr icted to i t are Ilex spp. (PI. 1, Figs. 18-21), Fagus, Quercus, Liquidambar, T i l i a (PI. 2, Fig. 1), Alnus (PI. 2, Fig. 3), Ulmus (PI. 2, Figs. 2 and 6), Juglans, (PI. 2, Fig. 7, Carya (PI. 2, Figs. 4-5) and Pterocarya. Although infrequent to rare, several zonally diagnostic species make their last stratigraphic ap- pearance in this interval. They are Parviprojectus sp. A, Diervilla echinata, Jussiaea sp. (PI. 2, Fig. 8) Boisduvalia clavatites (PI. 2, Fig. 9) and Acanthaceae sp. (PI. 2, Fig. 13). Other range tops re- corded within the zone are Nyssapollenites (PI. 2, Fig. 15), Araliaceoipollenites granulatus (PI. 2, Figs. 11-12), A. profundus (PI. 2, Fig. 17), Rousea araneosa (PI. 2, Fig. 10), R. monilifera (PI. 2, Fig. 14), and Ephedra claricristata (PI. 2, Fig. 16). Rounding out the terrestr ia l f lora l assemblage are common occurrences of ericaceous tetrads, Picea-Pinus, Taxodium, Metasequoia, Laevigatosporites and Osmunda. Parviprojectus resembles Aquilapollenites in that they are both char- acterized by three equatorial projections and pronounced polar areas. Some workers consider Parviprojectus a reworked species of Aquilapollenites (Srivastava, personal communication). However, with the exception of a couple of species that range up into the early to middle Paleocene of the western interior of the United States and Canada .(Leffingwell, 1971; Sweet, 1978; this author, unpublished tech- nical report), most Aquilapollenites species became extinct at the 39 Cretaceous/Tertiary boundary. The Oligocene species of Parviprojectus, however, has not been described from either Senonian or Paleocene assemblages. Because of i t s d i s t inct morphology, i t is considered herein as part of the indigenous f lora . Dinoflagellates are very rare in the samples examined from this inter- val. Only several occurrences of the long-ranging species Paralecaniella indentata were noted; An early Oligocene age is assigned to the Parviprojectus sp A. zone based upon the restricted range top of Parviprojectus within the early Oligocene of the Canadian Arct ic (Staplin, 1976; Rouse, 1977; Norris, 1986) and Br i t i sh Columbia (Rouse, 1977; Rouse and Mathews, 1979). Wiggins (personal communication) has also found similar pollen types from the Oligocene of Alaska, In addition, the range top of Boisduvalia clavatites has been recorded from the early Oligocene of inter ior Br i t i sh Columbia (Pi e l , 1971; Hopkins et a l , 1972; Rouse, 1977; Rouse and Mathews, 1979) and the Canadian Arct ic (Rouse, 1977; Ioannides and Mclntyre, 1980). Jussiaea has also been recorded from the early Oligocene in central Br i t i sh Columbia (Rouse, 1977). Piel (1977) shows the range of Jussiaea extending up into the early Miocene, however, that one occurrence is now considered to have been reworked (P ie l , personal communication). 40 The assignment of an early Oligocene age to this zone reveals an ap- parent hiatus in the stratigraphic record that spans much of the Oligocene. A possible explanation for the presumed gap in the record is suggested by Gradstein and Srivastava (1980) who used micropaleontological data to identify a broad shelf regression during this time period. 4. Araliaceoipollenites megaporifer Interval Zone The range top of Araliaceoipollenites megaporifer (PI. 3, Figs. 1~2) defines the top of the zone and the range top of Rhoipites latus the base. The f lora l assemblage associated with the zone is dominated by pollen and spores and is characterized, in part, by the f a i r l y common occurrence of many of the same taxa (e.g., Juglans, T i l i a , Carya, Pterocarya, Ulmus and Liquidambar) found in the overlying Parviprojectus sp. A zone. Fagus, Quercus and onagraceous pollen, however, are rare and, with the exception of one specimen, Parviprojectus sp. A is absent. Araliaceoipollenites megaporifer, most species of Verrutricolporites spp., Tetracolporites cf. T. brevis (PI. 3, (Fig. 3), Momipites coryloides and M. microfoveolatus (PI. 3, Figs. 7-8) make their last stratigraphic appearance within the zone. With the exception of one occurrence in Herjolf M-92 (sample 4500 f t . ) , the range top of Gothanipollis cockfieldensis (PI. 3, Fig. 4) is also associated within this zone. In general, there is a drop 41 in the number of triporates from the previous zone and a gradual i n - crease in tricolporates. Also, ericaceous tetrads (PI. 3, Fig. 9-10) which are found throughout the Tertiary of the Labrador Sea reach their peak abundance in this zone. Gymnosperm pollen and fern spores are also ubiquitous. Dinoflagellates are uncommon and are comprised mainly of Paralecaniella indentata and Form sp. A with rare occurrences of Chiropteridium cf. C. aspinatum, Deflandrea sp. A and Phthanoperidinium sp. A. In Herjolf M-92, the acritarch genus, Hichrystridium, is abundant. The age of the zone is uncertain and is considered here as t rans i - tional across the Eocene/01igocene boundary. The ranges of dinoflagellates associated with this zone are not age-diagnostic. Re- garding the pollen and spores, Frederiksen (1969, 1980) reports the ranges of Araliaceoipollenites megaporifer, Verrutricolporites cruciatus (PI. 3, Figs. 5-6), Momipites coryloides and M. microfoveolatus extending up into the lower part of the Vicksburg Group (lower Oligocene) and Gothanipollis cockfieldensis only up into the Yazoo Clay (upper Eocene). On the Grand Banks, Williams and Brideaux (1975) show the range of Verrutricolporites spp. extending up into the lowermost Oligocene. In south central Br i t i sh Columbia, the range top of Gothanipollis cockfieldensis was extended from the Eocene (Rouse, 1977) to the early Oligocene (Rouse and Mathews, 1979). Until 42 a more detailed study can be made that would u t i l i ze shorter sampling intervals and sidewall core material, the age-range of the zone can not be precisely determined at this time. 5. Rhoipites latus Interval Zone The top of the zone is defined by the range top of Rhoipites- latus (PI. 3, Fig. 11). and the base by the range top of P i s t i l l i p o l l e n i t e s mcgregorii. This zone is well-defined in each of the study wells and is characterized by an abundance and diversity of tricolporate pollen mainly belonging .to the genera Araliaceoipollenites, Verrutricolporites (PI. 3, Figs. 5-6 and 19-22)- and Cupuliferoipollenites. T i l i a becomes more common and Fagus, Quercus and Corylus/Carpinus are absent to rare, suggesting that their range bases l i e within this zone. Fungal spores are a relat ively common component of the f lora with Punctodiporites sp. (PI. 3, Fig. 25), Striadiporites spp. (PI. 3, Figs. 28-29), Fusiformisporites sp. A (PI. 3, Figs. 26-27) and Ctenosporites making their last stratigraphic ap- pearance. Aside from Rhoipites latus, the following species have their range tops within this interval: C a p r i f o l i i p i t e s sp. A (PI. 3, Fig. 12), Tricolporopollenites kruschii (PI. 3, Fig. 18), Symplocoipollenites spp. (PI. 3, Figs. 16-17), Holkopollenites sp. A, Lonicera sp. A, Myrtaceidites parvus, Verrutricolporites sp. A (PI. 3, Fig. 19) and Ailanthipites sp. B (PI. 3, Fig. 23). Near the base of 43 the zone, Bombacacidites bombaxoides (PI. 3, Fig. 24) makes i ts last stratigraphic appearance. The lower half of the Rhoipites latus zone is characterized by an abundance of small, 12-17 yum pollen belonging to the genera, Cupuliferoipollenites (Plate 3, Figs. 13-15). Because th i rpeak oc- currence is consistent and easi ly recognizable, i t should be consid- ered a subzone of the Rhoipites latus interval. Dinoflagellates make up a s ignif icant proportion of the total palynomorph assemblage in Kangamiut 1, Karlsefni A-13, Herjolf M-92 and Cartier D-70, especially near the base of the zone. Among the species present are Achilliodinium biformoides, Araneosphaera araneosa, Diphyes colligerum and Wetzeliella lunaris, a l l of which have their range tops in this interval . A late-middle to late Eocene age is assigned to the Rhoipites latus zone based mainly upon the the well-defined range top of Diphyes colligerum from the late Eocene of England (Eaton, 1976), the North Sea (Ioakim, 1979), the Norwegian-Greenland Sea (Manum, 1976), the Grand Banks and Scotian Shelf (Williams and Brideaux, 1975; Williams and Bujak, 1977) and the Canadian Arctic (Ioannides and Mclntyre, 1980). Eaton (1976) also reports the range tops of Araneosphaera araneosa and Achilleodinium biformoides in the late Eocene of England. Achilleodinium biformoides is also reported from the late Eocene of 44 the Grand Banks and Scotian Shelf (Williams and Bujak, 1977; Barss et a l . , 1979). 6. Pistillipollenites mcgregorii Interval Zone The top of the zone i s defined by the range top of Pistillipollenites mcgregorii (PI. 4, Figs. 1, 6, 11-12). and the base, ten ta t i ve l y , by the range top of Tricolpites sp. A. It i s a wel l -def ined zone that i s found in a l l s ix of the study wel l s . The zone i s characterized by an abundance of t r i co lpo ra te pollen (e.g., Rhoipites, Araliaceoipollenites, Verrutricolporites, Caprifoliipites and Tricolporopollenites). The number of Cupuliferoipollenites drops o f f rather sharply from the immediately overlying zone. Tilia, Carya, Juglans, Rhoipites latus, and R. angustus (PI. 4, Fig. 2) are f a i r l y common. Fungal spores, e.g., Dicellaesporites, Multicellaesporites and Pesavis tagluensis (PI. 4, Fig. 4), have t he i r greatest abundance in th i s i n t e r v a l . Towards the base of the zone, the number of Verrutricolporites drops of f and the frequency of t r i c o l pate pollen increases. Juglandaceous pollen of the Momipites complex (e.g., M. coryloides) are more frequent than in the previously described zones. The range top of Platycarya (PI. 4, Figs. 3 and 7) coincides with the range top of Pistillipollenites mcgregorii in Hekja 0-71, Kar lsefni A-13 and Herjo l f M-92 and in the remaining wel ls i t s range top extends into the base of the overlying Rhoipites latus zone. Azolla g loch id ia 45 (PI. 4, Fig. 5), which are usually associated with the Maastrichtian and lower Paleocene (Leffingwell, personal communication; Sweet, per- sonal communication), are found in the P i s t i l l i p o l l e n i t e s mcgregorii interval . The specimens are f a i r l y common and well-preserved and are considered at present to be in place. Norris (1986) also reports mid- dle Eocene occurrences of Azolla from the southern Beaufort Sea. The dinoflagellate assemblage associated with this zone is generally the most diverse and abundant of those found in the Tertiary interval from the Labrador Sea. It is distinguished by an abundance of Areoligera senonensis, Adnatosphaeridium spp. and Glyphyrocysta sp. Also relat ively common to the zone are Wetzeliella spp., Deflandrea phosphor itica, Cordosphaeridium sp., Apectodinium homomorphum, Paleotetradinium exilimurum, Spiniferites spp. and Thalassiphora pelagica. Among the dinoflagellates making their last stratigraphic appearance are Eatonicysta ursalae, Homotryblium tenuispinosum, and Rhombodinium condylos. The range tops of Apectodinium quinquelatum, A. cf. A. hyperacanthum and A. parvum were recorded near the base of the zone. The age of the P i s t i l l i p o l l e n i t e s mcgregorii zone is interpreted as early Eocene to early middle Eocene. The range top of Eatonicysta ursalae is reported from the early middle Eocene of the North Sea (Ioakim, 1979; Herit ier, et al,., 1979) and England (Eaton, 1976) and Rhombodinium condylos makes i ts last stratigraphic appearance in the 46 early Eocene of England (Downie, Hussain and Williams, 1971; Eaton, 1976) , the North Sea (Ioakim, 1979) and the middle to early Eocene of the Grand Banks and Scotian Shelf (Williams and Brideaux, 1975; Williams and Bujak, 1977; Barss et a l . , 1979). The range top of P i s t i l l i p o l l e n i t e s mcgregorii is well-defined in the early middle Eocene of the Canadian Arctic (Staplin, 1976; Rouse, 1977; Norris, 1986), Br it ish Columbia (Rouse et a l . , 1971, Rouse, 1977) and the western United States (Newman, 1981, 1983; Cushman, 1983; Reiswig, 1983; Wingate, 1983). Leopold and McGinitie (1972), Newman (1980, 1981, 1983), Cushman (1983) and Wingate (1983) report the range top of Platycarya from the western United States as early to middle Eocene and Frederiksen and Cristopher (1978) and Frederiksen (1980) report a middle Eocene range top from the southeastern United States. 7. T r i c o l p i t e s sp. A Interval Zone The top of this zone is tentatively defined by the range top of T r i c o l p i t e s sp. A (sensu Rouse 1977) and the base by the range top of Paraalnipollenites alterniporus. However, because of the rare and sporadic occurrence of Tricolpites sp. A, this zone would be more ap- propriately considered an assemblage zone characterized by the concur- rent association of Pistillipollenites mcgregorii, Tricolpites spp. 47 (including T. cf. T. hians, T. densus and T. reticulatus), Rhoipites cryptoporus, Intratriporopollenites sp. A. and Carya spp., which i n - cludes a pre-Carya form (PI. 4, Fig. 13) that has at least one of i ts three pores located on the equator. Bladdered conifer and taxodiaceous pollen and pteridophyte fern spores are generally the main ter res t r i a l l y derived component of the palynoflora. Triporopollenites mullensis and tlomipites rotundus have their range tops within the zone and several occurrences of Insulapollenites rugulatus (PI. 4, Fig. 12) were also noted. In a sidewall core sample from Herjolf M-92 and cuttings samples from Karlsefni A-13, several Paleocene tlomipites spp., e.g., M. ventifluminis (PI. 4, Fig. 10), M. wyomingensis (PI. 4, Figs. 8-9), ti. amplus (PI. 4, Fig. 15) and tt. anellus (PI. 4, Fig. 14), were recorded. The assemblage of pollen and spores in this zone d i f fers from the overlying P i s t i l l i p o l l e n i t e s mcgregorii zone in that there is a s ig- nif icant increase in the number of tricolpate pollen. Also, tricolporate species tend to have generally smaller and less well-defined pores. Araliaceoipollenites and Verrutricolporites are absent from the assemblage. Another observed trend is the tendency for a reduction in the number of gemmae on the Paleocene forms of P. mcgregorii. 48 Dinoflagellates are abundant but less diverse than in the previous zone. The most diagnostic feature of the dinoflagellate assemblage is a peak abundance of Apectodinium spp. at the top of the zone. Other abundant forms are Areoligera spp. and Adnatosphaeridium spp. Among the dinoflagellates that have their range tops within the zone are Deflandrea speciosa and D. cf. D. dartmooria. The age of this zone is being interpreted as late Paleocene (possibly even latest Paleocene to ear l iest Eocene). The last stratigraphic ap- pearance of Deflandrea speciosa is reported from the late Paleocene of the North Sea (Ioakim, 1979), Herit ier et a l . , 1979) and the Grand Banks and Scotian Shelf (Williams and Bujak, 1977; Barss et a l . , 1979). Peak abundances of Apectodinium spp. are recorded from the latest Paleocene and/or ear l iest Eocene of the North Sea (Knox et a l . , 1981), England (Dowm'e et a l . , 1971; Costa and Downie, 1976) and Denmark (Heilman-Clausen, 1985). A late Paleocene range top is reported for T r i c o l p i t e s sp. A from the Canadian Arctic (Rouse, 1977). tlomipites ventifluminis, M. wyomingensis, M. anellus and M. amplus also have their range tops in the late Paleocene of the Wind River Basin (Nichols and Ott, 1978) and li. s t r i c t u s becomes extinct in the latest Paleocene of South Carolina (Frederiksen and Christopher, 1978). The range top of M. rotundus and M. coryloides is in the late middle Paleocene of the Canadian Arct ic (Rouse, 1977) and Alberta (this author, unpublished technical report), 49 and late Paleocene of the Powder River Basin (Leffingwell, 1971). The range base of Tilia in the Canadian Arct ic and Br i t i sh Columbia is placed at the base of the Eocene. In sidewall core samples from Herjolf M-92, Kangamiut 1 and Karlsefni A-13 from both above and below the interpreted Pal eocene/Eocene boundary, Tilia is found only above the boundary. 8. Paraalnipollenites altemiporus Interval Zone The top of the zone is defined by the range top of Paraalnipollenites altemiporus ( P I . 4, Figs. 16-17). The base of the zone is a r t i - f i c i a l l y defined by the f i r s t appearance downhole of Cretaceous dinoflagellates (e.g., Phelodinium sp., Isabel idinium sp. and Amphidiadema nucula). The Paraalnipollenites altemiporus interval is comprised of a low diversity pollen and spore assemblage characterized by abundant bladdered conifer (predominantly Picea ( P I . 4, Fig. 26) and Pinus) and taxodiaceous pollen ( P I . 4, Fig. 20) as well as monolete ( P I . 4, Fig. 25) and t r i l e te fern spores. Paraalnipollenites altemiporus, the Betulaceae-Myricaceae pollen complex ( P I . 4, Figs. 21-22), Casuarinidites spp. ( P I . 4, Fig. 24) and reticulate ( P I . 4, Figs. 19-23), scabrate and psilate tricolpate grains are present but never abundant. With the exception of several rare occurrences of Momipites (e.g., Momipites actinus, P I . 4, Fig. 18), this zone is es- sential ly devoid of juglandaceous pollen. 50 Dinoflagellates are a common constituent of the palynomorph assemblage. Just above the top of the zone, there is a well-defined dinoflagellate interval marked by the last stratigraphic appearance of Alisocysta margarita, and the range top of Palaeoperidinium pyrophorum is usually found near the middle of the zone. Dinoflagellates having their range tops within the zone are Alisocysta circumtabulata, Deflandrea diebeli and D. striata. An early to middle Paleocene age is assigned to this zone based upon the range top of Alisocysta circumtabulata in the middle Paleocene (lower Thanetian) of the North Sea (Herit ier et a l . , 1979; Knox et a l . , 1981) the Grand Banks and Scotian Shelf (Williams and Bujak, 1977) and the Atlantic coastal plain sediments of Virginia (Witmer, personal communication). In addition, Palaeoperidinium pyrophorum makes i t s last stratigraphic appearance at the top of the Danian in the North Sea (Herit ier et a l . , 1979; Ioakim, 1979; Knox et a l , 1981), the Grand Banks and Scotian shelf (Williams and Bujak, 1977; Barss et a l . , 1979) and the Atlantic coastal plain (Witmer, personal communi- cation) and near the middle Selandian in Denmark (Heilman-Clausen, 1985). The range top of Paaralnipollenites altemiporus is reported from the middle Paleocene of the Canadian Arct ic (Rouse, 1977) and Alberta 51 (this author, unpublished technical report; Sweet, personal communi- cation). Also, the low divers ity pollen and spore assemblage of the P. altemiporus interval is very typical of early to middle Paleocene floras reported from the Canadian Arct ic (Rouse, 1977), the western inter ior of the United States and Canada (Leffingwell, 1971; Sweet, 1978; Hotton, 1983) and Alabama (Srivastava, 1972). DISTRIBUTION OF PROVISIONAL ZONES IN STUDY WELLS The distr ibution of the eight preliminary pollen and spore zones among the six study wells is shown in Figure 4. As previously mentioned, the ages assigned to the various zones are only relat ive and are based for the most part on the well documented range tops of certain dinoflagellate species. Range charts of pollen and spores with spe- cies arranged in descending order by last stratigraphic occurrence for each well can be found in the APPENDIX. The depths between which zonal boundaries are drawn are also indicated. The charts for Kangamiut 1, Karlsefni A-13, Herjolf M-92 and Cartier D-70 plot only the ranges of the most common and/or zonally diagnostic species; whereas, the range charts for Hekja 0-71 and Roberval K-92 show a more detailed representation of the Tertiary suite of pollen and spores re- covered from the continental shelf sediments of the Labrador Sea. The Tsuga igniculus and Fagus granulata zones are f a i r l y wel1-documented 52 AGE PALYNOZONE KANGAMIUT 1 HEKJA 0-71 KARLSEFNI A-13 HERJOLF M-92 ROBERVAL K-92 CARTIER D-70 • GE NE  MIDDLE TO LATE MIOCENE Tsuga igniculus X X O Hi Z EARLY MIOCENE Fagus granulata X X X >• EARLY OLIGOCENE Parviprojectus sp. A X X X X QC < UJ EARLY OLIGOCENE TO LATE EOCENE A raliaceoipollenites megaporifer X X X X rr O G E N  LATE EOCENE Rhoipites latus X X X X X X I r k LU H P A LE  MIDDLE TO EARLY EOCENE Pistillipollenites mcgregorii X X X X X X LATE PALEOCENE Tricolpites sp. A X X X X X MIDDLE TO EARLY PALEOCENE Paraalnipollenites altemiporus X X X X X igure 4. Distribution of provisional pollen and spore interval zones in the six study wells. in Hekja 0-71 and Roberval K-92. Their apparent absence from the other wells is interpreted as an art i fact of not having representative samples from these intervals available for study. Although a set of samples between 950 and 2500 m. from Kangamiut 1 were provided, they were overmacerated and contained a considerable amount of mineral mat- ter and, therefore, were not studied in deta i l . Nevertheless, some in-s i tu pollen, primarily Picea and Pinus with minor occurrences of Tsuga igniculus, Ilex, Alnus, Osmunda, Laevigatosporites and ericaceous tetrads, were noted. Because these grains are long-ranging, i t is d i f f i c u l t to assign them to any one zone. How- ever, the general lack of diversity and the predominance of conifers (including Tsuga igniculus) suggests that at least part of this inter- val belongs to the T. igniculus zone. One sidewall core sample (6374 f t . ) from Karlsefni A-13 has been ten- tat ively assigned to the Fagus granulata zone. Present in the assemblage are not only Picea, Tsuga igniculus and Gramineae pollen, but also pollen belonging to the juglandaceous group (e.g., Juglans, Carya and Pterocarya) as well as Ulmus and CorylusfCarpinus. Although only one questionable occurrence of Fagus granulata was recorded, the presence of Gramineae pollen and the diversity of the assemblage ind i - cates the sample should be assigned to the F. granulata zone. The F. granulata zone is interpreted as probable early Miocene, how- ever, i t should be noted that the majority of pollen (e.g., 54 Corylus/Carpinus, Fagus, Quercus and Betula) recorded from the inter- val range down section into the Oligocene and, in some cases, even lower. In Roberval K-92 between 790 and 1400 m., the recovery of in-s i tu palynomorphs is relat ively poor. Because of the absence of Gramineae pollen in these samples, i t is possible that they represent, at least in part, the middle to late Oligocene.' Unfortunately, with the exception of a couple of recorded occurrences of Paralecaniella and Form sp. A, the samples in question are essential ly barren of dinoflagellates. Dinoflagellates can often be helpful in dist inguish- ing Miocene and Oligocene palynofloral assemblages from one another (Helby et. a l . , 1984). Because pre-Eocene samples from nearby Cartier D-70 were not available for study, i t can not be determined i f a simi- lar undiagnostic zone is present in that well. Whether or not there is a middle to late Oligocene hiatus in the continental shelf sediments of the Labrador Sea remains to be seen. Hopefully, the re- cent ODP, Leg 105 cruise to the Labrador Sea and Baffin Bay wi l l shed some light on this problem (Gradstein, personal communication). The Parviprojectus sp. A zone is found in Kangamiut 1, Hekja 0-71, Herjolf M-92 and Roberval K-92. Many of the pollen (e.g., Boisduvalia, Jussiaea, Araliaceoipollenites granulatus and Rousea spp.) found associated with Parviprojectus in this zone are not found in Kangamiut 1. However, because only one rather s i l t y sample (2600 m.) was examined, the absence of the missing forms may be due to both the poor sample control and the lithology. In Roberval K-92, the top 55 of the zone has been drawn just above 1420 m., based upon the range tops of Boisduvalia and Jussiaea. The last stratigraphic occurrence of Parviprojectus is found 50 meters below that sample at 1470 m. The top of the interval is d i f f i c u l t to define because of the abundance of recycled Carboniferous spores which overwhelmingly di lute the in-s i tu taxa in this zone, as well as in the underlying Araliaceoipollenites megaporifer zone. The absence of the Parviprojectus sp. A zone in Karlsefni A-13 is very l ike ly due to the approximate 400 f t . gap be- tween samples. The Araliaceoipollenites megaporifer zone can be recognized in Hekja 0-71, Karlsefni A-13, Herjolf M-92 and Roberval K-92. Because the zone can be quite narrow, i t s apparent absence in Kangamiut 1 may be due to the 100 meter spacing between samples 2600 and 2700 m. Whether or not the zone is present in Cartier D-70 is questionable and i s , therefore, not shown in Figure 4. The pollen and spore f lora from two sidewall core samples (4240 and 4270 feet) is not very diagnostic and is characterized by an abundance of bladdered conifers. The pres- ence of several species of Araliaceoipollenites and a single specimen of Jussiaea suggests the samples may belong to either the Parviprojectus sp. A or Araliaceoipollenites megaporifer zones. How- ever, the presence of' Araneosphaera araneosa (range top in the late Eocene) in sample 4270 feet suggests instead that the interval belongs to the Rhoipites latus zone. 56 Samples collected from s i l ty to shaly intervals within and in close proximity to sand bodies are often characterized by a depauperate in-s i tu palynomorph assemblage consisting mainly of poorly preserved and oxidized bladdered conifers, spores and dinoflagellates. In these intervals recycled palynomorphs, in addition to degraded and non-degraded v i t r i n i t e are commonly a major component of the overall assemblage of organic matter. Another factor affecting the concentration of pollen and spores, espe- c i a l l y in Eocene and older Tertiary and Late Cretaceous shales and mudstones, is an increase in the abundance of marine derived dinoflagellates and other marine algae, as well as f lu f fy appearing amorphinite. In some samples within these intervals, the dominant pollen and spore type consists of bisaccate pollen. This situation corresponds with the observation by Mudie (1982) that in the recent offshore sediments of eastern Canada, bladdered conifer pollen is gen- eral ly transported further offshore than other pollen types via wind and/or water transport. The Rhoipites latus and Pistillipollenites mcgregorii zones are found in a l l six study wells. Both zones are fa i r l y easy to recognize in spite of a problem with uneven recovery of pollen and spores in sam- ples within these intervals. In some of these samples the number and 57 diversity of the ter res t r i a l l y derived palynomorphs in very low, espe- c i a l l y in Karlsefni A-13. This problem with spotty recovery of pollen and spores continues down section into the T r i c o l p i t e s sp. A and Paraalnipollenites altemiporus zones. The T r i c o l p i t e s sp A zone was identif ied in Karlsefni A-13, Herjolf M-92 and Roberval K-92 and, tentatively, in Kangamiut 1 and Cartier D-70. Because of the rar i ty of the zonally nominate species, the top of the T r i c o l p i t e s sp. A zone can be d i f f i c u l t to identify. In Kangamiut 1 the top of the zone is tentatively placed between samples 3099 and 3201 meters. The positioning of the boundary in this well is based in part upon the recorded range tops of Momipites rotundus and Triporopollenites mullensis, as well as the relative abundance of tr icolpate pollen in relation to tricolporates and the absence of T i l i a , Araliaceoipollenites and Verrutricolporites from sample 3201 meters. Using absence data is questionable though when working with cuttings samples. The pollen and spore data is supported, however, by associated dinoflagellate assemblages which are very useful for help- ing to interpret the upper l imits of the zone. The range tops of Deflandrea speciosa and Apectodinium hypercanthum coincide with or very closely approximate the boundary between the P i s t i l l i p o l l e n i t e s mcgregorii and the Tricolpites sp. A zones. In Cartier D-70 the top of the T r i c o l p i t e s sp. A zone l ies within a broad interval between 5500 and 5810 feet. It is very d i f f i c u l t to 58 determine i t s position more precisely because the samples examined from this interval (5600 and 5720 feet) are from sandy units within or near the Upper Cartier Sandstone. The recovery of palynomorphs is f a i r l y poor and there is some contamination by cavings. Sample 5810 feet is interpreted to l i e within the T r i c o l p i t e s sp. A zone based on the combined occurrence of Momipites rotundus, Triporopollenites mullensis and Insulapollenites rugulatus. The range tops of these species l i e within the zone. Deflandrea speciosa and Apectodinium hypercanthum are also associated with the assemblage. The Paraalnipollenites altemiporus zone is found in the same wells as is the T r i c o l p i t e s sp. A zone. The zone is f a i r l y easy to identify, but i t s stratigraphic relationship to the range tops of Alisocysta margarita and Palaeoperidinium pyrophorum can vary. Although the r e l - ative positioning of the range tops of Paraalnipollenites altemiporus and these two dinoflagellates appears to be mainly dependent upon the sampling interval , the last consistent stratigraphic occurrence of Alisocysta margarita tends to l i e just above the range top of Paraalnipollenites altemiporus In Hekja 0-71 the Tricolpites sp. A and Paraalnipollenites altemiporus zones were not ident i f ied. Samples below 2600 meters were not examined because of the d i f f i cu l t y in picking rel iable range tops. The problem was due to the ubiquitous presence of Paleocene pollen and spores throughout the well. 59 The boundaries between provisional zones in Hekja 0-71 are f a i r l y nar- row and occur anomalously high in the section. For example, the boundary between the Fagus granulata and Parviprojectus sp. A zones l ies between 935 and 970 meters; and the transitional Eocene/01igocene Araliaceoipollenites megaporifer zone l ies between 1400 and 1605 me- ters. These data are contradictory to the relative ages reported by Klose et a l . (1982) in their description of the general l ithology of the well. Based on foraminifera fauna, they place the 01igocene-Miocene boundary at approximately 1830 meters and the Eocene-01igocene boundary at 2600 meters. In addition, they describe the l ithology of the sediments as predominantly sandy down to a depth of approximately 1300 meters. However, most of the raw samples re- ceived from Aquitaine for study did not appear sandy or s i l t y . The rather gross discrepancies between the relative ages of boundaries presented herein and the data from Klose et a l . (1982) could possibly be due to several different factors, namely, sample contamination via d r i l l i n g additives or cavings and/or redeposition of palynomorphs. Mud additives the same age as rock units being d r i l l ed can greatly bias palynological studies. One very common additive is l ignite from the Paleocene Ft. Union Formation from North Dakota. Many of the Paleocene species of pollen and spores found in Hekja 0-71 are similar in composition to palynological assemblages from the Ft. Union. How- 60 ever, according to McMillan (personal communication), Tertiary d r i l l - ing muds and/or l ignite additives were not used in d r i l l i n g Hekja 0-71. In Hekja 0-71 , Paleocene pollen and spores (e.g., Momipites spp. and Insulapollenites rugulatus) are f a i r l y common constituents throughout the well. If mud contamination can be ruled out, the Paleocene palynomorphs must be considered redeposited. The problem is to deter- mine i f they are in place or i f they have caved down section from younger sediments along with other pollen and spores that were inter- preted as in - s i tu . During the Pliocene-Pleistocene in the Labrador Sea region, there was considerable erosion of land surfaces, resulting in the offshore deposition of abundant recycled material of different ages. Because cuttings samples were used in studying Hekja 0-71, the pollen and spore assemblages examined from the well could represent cavings of recycled palynomorphs that dominate Pliocene-Pleistocene assemblages. If the palynomorphs were derived from recycling, an unroofing effect would be expected, whereby the age of the sequence while working stratigraphical ly down section would be inverted from oldest to young- est. This is not the case, however. Although there are abundant Paleocene pollen and spores found throughout the well, the range tops of species considered in-s i tu progress successively from youngest to oldest. Furthermore, this pattern would not be expected i f the 61 palynomorphs just represented cavings. Even though contamination by cavings can not be ruled out, the apparent youngest to oldest stratigraphic succession of range tops of pollen and spores downhole can not be dismissed. For this reason, therefore, zonal boundaries are presented as discussed, until such time that new data and/or bet- ter sample control is provided. A detailed study of the assemblages in fluorescent l ight might help to resolve the problem of identifying in situ palynomorphs from caved and redeposited grains (Bujak, peronal communication). As an aside, i t should be noted that other palynological workers, e.g., Mclntyre (personal communication) and Rouse (personal communication) have also found Hekja 0-71 a biostratigraphical ly confusing well to work. 62 COMPARISON OF LABRADOR SEA PALYNOLOGICAL ZONATIONS Two palynological zonations of the Tertiary sediments of the Labrador Sea were previously established by G. L. Williams (Williams and Bujak, 1977; Barss et a l . , 1979) and Ioakim (1979) Both zonations are based essential ly on just dinoflagellate assemblages. How these zonal schemes correlate with the pollen and spore zonation proposed herein is i l lustrated in Figure 5. The G. L. Williams zonation covers the complete Tertiary section, whereas the Ioakim scheme involves just the Paleocene and Eocene. The relative ages shown in Figure 5 are only approximations. A single zone, Tsuga igniculus was established by G. L. Williams for the Pliocene. No correlative pollen and spore zone could be estab- lished because material of known Pliocene age was not examined in any of the six study wells. The Miocene section, on the other hand, shows two zones for each zonal scheme. The T. igniculus and Fagus granulata zones correspond to the Operculodinium centrocarpum and Paralecaniella indentata zones, respectively. Because the range top of T. igniculus is a r t i f i c i a l l y defined in this study due to the lack of stratigraphical ly higher samples, i t is possible that the upper l imits of this zone may extend into the T. igniculus zone of G. L. Williams. 63 LATE PL IOCENE EARLY PL IOCENE LATE M I O C E N E MIDDLE M I O C E N E EARLY M IOCENE LATE OL IGOCENE EARLY OL IGOCENE LATE E O C E N E MIDDLE E O C E N E EARLY E O C E N E LATE P A L E O C E N E EARLY P A L E O C E N E M A A G E 2.0 •5.1 14.4 24.6 32.8 38.0 42.0 50.5 54.9 60.2 65.0 BARSS . B U J A K A N D WILLIAMS. 1979 Tsugaepollenites igniculus Assemblage Operculodinium centrocarpum Assemblage Paralecaniella indentata Assemblage Cordosphaeridium fibrospinosum- Deflandrea sp. C Assemblage Wetzeliella ovalis Assemblage Wetzeliella lunaris Assemblage Areoligera senonensis Assemblage Ceratiopsis speciosa Assemblage Alisocysta circumtabulata Assemblage Palaeoperidinium pyrophorum Assemblage IOAKIM, 1979 Rhombodinium intermedium Zone Wetzeliella articulata Zone Kisselovia edwardsii Zone Rhombodinium condylos Zone Wetzeliella verielongitudina Zone Wetzeliella similis Zone Wetzeliella mecklefeldensis Zone Apectodinium hyperacanthum Zone Deflandrea speciosa Zone Palaeoperidinium pryrophorum — Deflandrea striata Zone WILLIAMS (HEREIN) Tsuga igniculus Zone Fagus granulata Zone (no data) -?- Parviprojectus sp. A Zone Araliaceoipollenites megaporifer Zone Rhoipites latus Zone Pistillipollenites mcgregorii Zone Tricolpites sp. A Zone Paraalnipollenites alterniporus Zone •Harland et al.. 1982 Figure 5. Comparison of previously established Tertiary palynological and the provisional pollen and spore zones . zonations of the Labrador A late Oligocene Cordosphaeridium fibrospinosum - Deflandrea sp. C zonal assemblage is reported by G. L. Williams. No corresponding pollen and spore zone was found in the study wells.. The pollen and spores indicate a hiatus in the depositional record during this inter- val. The uppermost early Oligocene dinoflagellate Wetzeliella ovalis zone tends to correspond with the Parviprojectus sp. A.zone. Whereas pollen and spores indicate a transition zone (Araliaceoipollenites megaporifer) across the Eocene/01igocene boundary, the boundary is marked by the tops of the Wetzeliella lunaris and Rhombodinium inter- medium zones. The top of the Pistillipollenites mcgregorii zone appears to be a good zonal marker for the upper middle Eocene for which there are no zonally diagnostic dinoflagellate range tops or assemblages indicated. P. mcgregorii was found in a l l of the study wells and, though not com- mon, i t s occurrence is consistent and i t is associated with a charac- te r i s t i c assemblage. Ioakim's zonal resolution for the Eocene of the Labrador Sea sediments is the. most detailed of the three zonations. This is particularly true of the early Eocene, which she has divided into five zones. The early Eocene of the Labrador Sea region was a time during which the diversity and relative abundance of dinoflagellates were highest. Un- fortunately, her zonation was somewhat d i f f i c u l t to apply because not a l l of the zonally nominate species were present in the wells invest i - 65 gated and, in some instances, their stratigraphic occurrences not a l - ways consistent. This problem may possibly be due in part, however, to the wide intervals between samples, palynomorph preservation and contamination by cavings and/or redeposition. Dinoflagellates are more useful for establishing zonal boundaries in the Paleocene than are the pollen and spores. Three zones were recog- nized by both Ioakim and G. L. Williams whereas only two have been ident i f ied using pollen and spores. The character ist ica l ly low diver- sity and reduced numbers of pollen and spores in this part of the sec- tion are a major d i f f i cu l t y with regards to further refining the zonal resolution of the Tricolpites sp. A and Paraalnipollenites altemiporus zones. The zone comparisons i l lustrated in Figure 5 demonstrate that pollen and spores can be useful in the Tertiary marine sections of the Labrador Sea for helping to establish biostratigraphic control, par- t i cu lar ly when used in conjunction with dinoflagellate assemblages. The provisional zonation proposed herein is especially important in sections where terrestr ia l palynomorphs predominate, e.g., Eocene through Miocene of Hekja 0-71 and upper Eocene and younger sections of the remaining study wells. There is an excellent potential for i n - creasing the biostratigraphic zonal resolution in these intervals by taking a combined detailed taxonomic and s tat i s t ica l approach to the study of the pollen and spore assemblages. The maintenance of careful 66 control over sample spacing and quality would be essential, however, for such analyses. DISCUSSION The proposed provisional pollen and spore zonation may be applicable to other northern latitude regions. Many of the zonally diagnostic f lora l elements found in the Tertiary sediments of the Labrador Sea are also known to extend across the Canadian Arct ic and into north- western North America. Pollen and spore assemblages of Paleocene age have been described from the Canadian Arct ic (Rouse and Srivastava, 1972; Doerenkamp et a l . , 1976; Rouse, 1977; Ioannides and Mclntyre, 1980). Although many of the same species are common to the two areas, on the Labrador Shelf there is a f a i r l y strong marine influence and the pollen and spores do not show as great a diversity as in the largely terrestr ia l assemblages from the Arct ic . Rouse was able to divide the early and middle Paleocene into three zones (P- l to P-3) which correspond to the single Paraalnipollenites alterniporus zone from the Labrador Sea. Almost a l l of the pollen and spores (including the zonally nominate species, T r i c o l p i t e s sp. A) from the late Paleocene of the Labrador Sea is also present in Rouse's late Paleocene P-4 assemblage. Many of 67 the same elements are also reported by Ioannides and Mclntyre (1980) from the Caribou H i l l s section of the Mackenzie delta. The Eocene pollen and spore assemblages of the Labrador Sea, Canadian Arct ic , Br i t i sh Columbia and northwestern Washington State are remark- ably similar. Over this extensive area, the Eocene assemblages are very diverse, with a large number of species making their f i r s t stratigraphic appearance during this time interval. Pollen and spore assemblages comparable to the P i s t i l l i p o l l e n i t e s mcgregorii zone (this paper) are reported from the early to middle Eocene of the Caribou H i l l s section in the Mackenzie delta (Ioannides and Mclntyre, 1980), the southern Beaufort Sea (Norris, 1986), the Eureka Sound Formation and equivalent beds in the Canadian Arctic and south central Br it ish Columbia (Rouse, 1977), the Burrard Formation in coastal Br it ish Columbia (Rouse et a l . , 1971) and the Chuckanut Formation just south of the Canadian-United States border in northwestern Washington State (Reiswig, 1983). The f lora represented by the late-middle to late Eocene Rhoipites latus zone is equivalent to the E-2 assemblage described by Rouse (1977) from the Canadian Arctic and south central Br i t i sh Columbia. Similar assemblages have also been described from the Kitsilano Forma- tion in coastal Br i t i sh Columbia (Hopkins, 1969; Rouse et a l . , 1971) and the Chuckanut Formation in northwestern Washington (Reiswig, 1983). Rouse (personal communication) has also noted 68 Araliaceoipollenites megaporifer, Verrutricolporites and other pollen associated with the Araliaceoipollenites megaporifer zone from the Beaufort Sea. The early Oligocene Parviprojectus sp. A zonal assemblage from the Labrador Sea is similar to that described from the Caribou H i l l s sec- tion of the Mackenzie delta (Interval D of Ioannides and Mclntyre, 1980), from central Br i t i sh Columbia (P ie l , 1971 and 1977) and from the Northern Rocky Mountain Trench in Br i t i sh Columbia (Hopkins et a l . , 1972). An early to middle Miocene pollen and spore assemblage similar to that used to characterize the Labrador Sea Fagus granulata zone is reported from the Whatcom Basin of southwestern Br i t i sh Columbia and northwest- ern Washington (Hopkins, 1968), south central Br i t i sh Columbia (P ie l , 1977) and Alaska (Wolfe and Leopold, 1967). The lower Miocene pollen and spore f lora reported by Norris (1986) for the southern Beaufort Sea is less diverse than the F. granulata zonal assemblage from the Labrador Sea. The Tsuga igniculus zone in the Labrador Sea is very similar to the late middle-upper Miocene assemblages of the Canadian Arct ic (Rouse, personal communication) and, though less diverse, to the Upper Skonun Formation of the Queen Charlotte Islands (Martin and Rouse, 1966), estimated between 11-13 Ma (Champigny et a l . , 1981). 69 The general s imilar ity of pollen and spore assemblages across northern and western Canada raises some interesting speculation with regards to the provenance of the grains. Because Tertiary outcrops in the circum-Labrador Sea area are almost non-existent, i t is not possible to determine i f in-s i tu terrestr ia l palynomorphs represent the " l oca l " f lora of the area or i f they were transported for long distances via a combination of wind and running water. Although some of the palynofloral elements were undoubtedly indigenous to the surrounding area, the species composition of redeposited Paleogene palynomorphs along with clay mineralogy data (Hiscott, 1984) indicate that at least some portion of the palynoflora was derived from the western inter ior and Arct ic regions of Canada (see CHAPTER 4 for deta i l ) . Pollen and spore assemblages from the offshore areas of Newfoundland, Nova Scotia and the northeastern United States seem to share fewer f lora l components with the Labrador Sea region than do northern and western Canada. A number of the zonally diagnostic pollen and spores used to characterize the eight provisional zones proposed for the con- tinental shelf sediments of the Labrador Sea are not reported by Williams and Brideaux (1975) from the Grand Banks or by Bebout (1980) from the Baltimore Canyon COST No. B-2 well. Some form of provincialism between the Labrador Sea and the Grand Banks/Scotian Shelf areas is also suggested by dinoflagellate assemblages (Bujak, personal communication). There are apparently some differences in dinoflagellate species composition between the two geographical re- 70 gions (Williams and Brideaux, 1975; Williams and Bujak, 1977; and Barss et a l . , 1970). With the exception of a greater abundance and diversity of extratriporate pollen, the Paleocene pollen and spore assemblage from the Grand Banks is quite similar to that from the Labrador Sea region. It is generally characterized by long-ranging species of low diversity and abundance. In the Baltimore Canyon well the Paleocene is absent. The Eocene and early Oligocene pollen and spore assemblages from the Grand Banks and Baltimore Canyon are very similar to one another and share many of the same elements found in the more northerly assemblages. However, some of the important zonally diagnostic pollen (e.g., onagraceous pollen, Parviprojectus, P i s t i l l i p o l l e n i t e s mcgregorii, and Rhoipites latus) and fungal spores (e.g., Striadiporitesy Fusiformisporites and Pesavis) common to the Labrador Sea, Canadian Arctic and Br i t i sh Columbia were not reported by Williams and Brideaux or Bebout. The Miocene of the Labrador Sea, Grand Banks and Baltimore Canyon is generally characterized by an abundance of conifer pollen (e.g., Picea, Pinus and Tsuga) and the last consistent stratigraphic appear- ance of a number of arboreal pollen species (e.g., Fagus, T i l i a , Juglans and Liquidambar). The ranges of several of these taxa extend stratigraphical ly higher in the Grand Banks and Baltimore Canyon than 71 they appear to farther north in the Labrador Sea and Canadian Arct ic, where climatic cooling associated with the onset of glaciation was more pronounced. Based upon the recorded distribution of Tertiary pollen and spore assemblages from northern North America, the provisional zonation pro- posed herein may successfully be applied across a broad regional zone that extends westward and northward from the Labrador Sea to include at least portions of the Canadian Arctic and Br i t i sh Columbia. The application of the zonation to the south into the Grand Banks, Scotian Shelf and Atlantic coastal plain areas of the northeastern United States is questionable, however, because of the apparent absence and/or differences in the stratigraphic ranges of many of the zonally diagnostic species used to characterize the zones. CONCLUSIONS 1. The diversity and abundance of pollen and spores in the Tertiary marine sediments of the Labrador Sea, provide suff ic ient material to use as a basis for establishing biostratigraphic control in the re- gion. Using range tops, eight preliminary pollen and spore interval zones are proposed. 72 2. A comparison between the Tertiary pollen and spore zonation pro- posed herein with previously published dinoflagellate zonations from the Labrador Sea demonstrates the u t i l i t y of pollen and spores for helping to establish stratigraphic control in marine sediments. A l - though dinoflagellates lend themselves part icular ly well to high-resolution biostratigraphy (as evidenced by Ioakim1s rigorous zonation of the Eocene), the stratigraphic ranges of pollen and spores when integrated with those of dinoflagellates, maximizes the total amount of information that can be derived from a palynological study of marine sediments. This is especially true in intervals where there is a strong terrestr ia l influence (e.g., Eocene through Miocene sections in Hekja 0-71 and Roberval K-92). The use of both pollen/spores and dinoflagellates not only helps to refine the zonation of the stratigraphic sections in these two wells, but also helps to distinguish and correlate facies. 3. The proposed pollen and spore zonation for the Tertiary of the Labrador Sea can be extended regionally across the Canadian Arct ic and inter ior Br i t i sh Columbia. Although some ranges may shift s l ight ly due to local climatic or physiographic factors, the general succession and content of the terrestr ia l palynoflora appears to be continuous across northern Canada. South of the Labrador Sea in the Grand Banks and Scotian Shelf area, however, most of the zonally nominate species have not been recorded. This apparent provincial i ty between the two areas may also be observed in the dinocyst palynoassemblages. 73 4. The proposed provisional pollen and spore zonation represents a good palynostratigraphic framework for future studies. There is a strong potential for refinement of this zonation especially for the Eocene and younger sediments. Before this can be done, however, i t wil l be necessary to establish better sidewall core control and to tighten the intervals between samples. 74 REFERENCES CITED Barss, M. S., J . P. Bujak and G. L. Williams, 1979. Palynological zonation and correlation of sixty-seven wells, eastern Canada. Geol. Surv. Can., Paper 78-24, 118 pp. Bebout, J . W., 1980. Observed stratigraphic distribution of spores, pollen and Incertae sedis palynomorphs in the Tertiary section of the Cost No.B-2 well, Baltimore Canyon, Atlantic outer cont i - nental Shelf. Palynology, 4, 181-196. Berggren, W. A. and J . A. Van Couvering, 1974. The late Neogene: biostratigraphy, geochronology and paleoclimatology of the last 15 mil l ion years in marine and continental sequences. Palaeogeogr., Palaeoclimatol., Palaeoecol., 16, 1-216. Champigny, N., C. M. Henderson and G. E. Rouse, 1981. New evidence for the age of the Skonun Formation, Queen Charlotte Islands, Br i t i sh Columbia. Can. J . 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Elsik (ed.), Contributions of stratigraphic palynology (with emphasis on North America), 1, Cenozoic palynology. Am. Assoc. Stratigraphic Palynologists Contr. Ser., 5A, 48-65. Rouse, G. E, W. S. Hopkins, J r . and K. M. P ie l , 1971. Palynology of some Late Cretaceous and Early Tertiary deposits in Br i t i sh Columbia and adjacent Alberta. Geol. Soc. Am., Spec. Paper 127, 213-246. Rouse, G. E. and W. H. Mathews, 1979. Tertiary geology and palynology of the Quesnel area, Br i t i sh Columbia. Bul l . Can. Petrol. Geol., 5, 418-445. Rouse, G. E. and S. K. Srivastava, 1972. Palynological zonation of Cretaceous and early Tertiary rocks of the Bonnet Plume Forma- t ion, northeastern Yukon, Canada. Can. J . Earth Sc i . , 9, 1163-1179. Srivastava, S. K., 1972. Some spores and pollen from the Paleocene Oak H i l l Member of the Naheola Formation, Alabama (U.S.A.). Rev. Palaeobotany and Palynology, 14, 217-285. Staplin, F. (ed.), 1976. Tertiary biostratigraphy, Mackenzie delta region, Canada. Bul l . Can. Petrol. Geol., 24:1, 117-136. Stover, L., 1977. Oligocene and early Miocene dinoflagellates from Atlantic core hole 5/5B, Blake Plateau. in W. C. Elsik (ed.), Contributions of stratigraphic palynology (with emphasis on North America), 1, Cenozoic palynology. Am. Assoc. Stratigrphic Palynologists Contr. Ser., 5A, 66-89. Sweet, A. R. 1978. Palynology of the Ravenscrag and Frenchman Formations, in Coal resources of southern Saskatchewan: a model for evaluation methodology. Geol. Surv. Can., Economic Geology Report 30, 29-39. Thomas, F. C. and F. M. Gradstein, 1981. Tertiary subsurface correlations using pyrit ized diatoms, offshore Eastern Canada. Geol. Surv. Can., Current Research Part B, Paper 81-1B, 17-23. Umpleby, D. C , 1979. Geology of the Labrador Shelf. Geol. Surv. Can., Paper 79-13, 34 pp. Williams, G. L. and W. W. Brideaux, 1975. Palynologic analyses of Upper Mesozoic and Cenozoic rocks of the Grand Banks, Atlantic continental margin. Geol. Surv. Can., Bul l . 236, 1-163. 80 Wil l iams, G. L. and J . P. Bujak, 1977. Cenozoic palynostratigraphy of offshore Eastern Canada, in W. C. El s i k (ed.) , Contributions of s t rat ig raph ic palynology (with emphasis on North America), 1, Cenozoic palynology. Am. Assoc. St rat ig raph ic Palynologists Contr. Ser., 5A, 14-47. Wingate, F. H., 1983. Palynology and age of the Elko Formation (Eocene) near Elko, Nevada. Palynology, 7, 93-132. Wolfe, J . A. and E. B. Leopold, 1967. Neogene and ear ly Quaternary vegetation of northwestern North America and northeastern As ia. in D. M. Hopkins (ed.), the Bering Land Bridge. Stanford Univer- s i t y Press, Stanford, C a l i f . , 193-206. 81 EXPLANATION OF PLATES Al l specimens were recovered from offshore Tertiary sediments from the Labrador Sea. The taxa i l lustrated are generally arranged according to the sequence in which they are discussed in the text. A l l photomicrographs were photo- graphed in transmitted l ight under Nomarski d i f ferent ia l i n - terference contrast. Figure captions contain information on the well, sample depth and type of sample ( i . e . , cuttings or sidewall core) from which specimens came. The orien- tation and focus level of specimens, magnification and photo numbers ( i . e . , negative number, year and frame number) of the photomicrographs are also included. 82 PLATE 1 FIGURE 1: Tsuga igniculus (Potonie) Potonie and Venitz 1934. Monosaccate pollen with loosely convoluted velum surrounding saucer-shaped body. Zonally nominate species. Range top = T. igniculus Zone. Roberval K-92; 710 m. (cuttings); mid-focus; 800x; ROB B:81:7. FIGURE 2: Osmunda sp. Tr i le te spore exhibiting irregular rugulo-baculate ornamentation. Genus long-ranging with greatest abun- dance in Miocene. Range top = T. igniculus Zone. Hekja 0-71; 935-965 m. (cuttings); polar view, mid-focus; lOOOx; TH 1:84:9. FIGURE 3: Betula c l a r i p i t e s Wodehouse 1933. Triporate pollen with protruding aspidate pores. Range top = T. igniculus Zone. Hekja 0-71; 740-830 m. (cuttings); polar view, mid-focus; 800x; TH 1:84:1. FIGURE 4: Chenopodipollis sp. Multiporate pollen. Range top = T. igniculus Zone. Hekja 0-71; 740-830 m. (cuttings); mid-focus; 800x; TH 1:84:2. FIGURE 5: Gramineae sp. Monoporate pollen with pore surrounded by annulus. Range top = T. igniculus Zone. Hekja 0-71; 740-830 m. (cut- tings); high-focus; 800x; TH 2:84:20. FIGURES 6 and 7: Fagus granulata Martin and Rouse 1966. Broadly e l - l i p t i c a l tricolporate pollen with narrow colpi and large e l l i p t i c a l pores. Fine (Fig. 7) to coarsely (Fig. 6) granulate ornamentation. Zonally nominate species. Range top = F. granulata Zone. Fig. 6: Hekja 0-71; 935-965 m. (cuttings); equatorial view, mid-focus; lOOOx; TH 1:84:7. Fig. 7: Hekja 0-71; 935-965 m. (cuttings); equatorial •view, mid-focus; lOOOx; TH 1:84:13. FIGURE 8: Quercus form A. Tricol pate, fine to moderately granulate form. Range top = F. granulata Zone. Hekja 0-71; 935-965 m. (cut- tings); equatorial view, mid-focus; 900x; TH 1/2:84:7. FIGURE 9: Quercus form B. Tricolpate, coarsely granulate form. Range top = T. igniculus Zone. Hekja 0-71; 935-965 m. (cuttings); equatorial view, mid-focus; 900x; TH 1:84:4. FIGURE 10: Liquidambar form A. Polyporate pollen with large rounded e l l i p t i c a l pores. Differs from form B by larger size (29 ûm to 40/um) and fewer but larger pores. Range top = F. granulata Zone. Hekja 0-71; 1205-1250 m. (cuttings); mid-focus; lOOOx; TH 2:84:4. 83 FIGURE 11: Liquidambar form B. Polyporate pollen with numerous, small rounded pores. Differs from form A by size (22 /jm to 27 ^m) as well as number and shape of pores. Hekja 0-71; 935-965 m. (cuttings); mid-focus; lOOOx; TH 1:84:5. FIGURE 12: Sequoia sp. Pollen grain with coarsely scabrate ornamentation and pronounced papi l la. Range top = F. granulata Zone. Hekja 0-71; 910-930 m. (cuttings); mid-focus; lOOOx; TH 4:84:21. FIGURE 13: Tsuga v i r i d i f l u m i n i p i t e s Wodehouse 1933. Monosaccate pollen with low, t ight ly convoluted velum. Fine spinae attached to velum (v is ib le along outer margin of saccus). Range top -F. granulata Zone. Hekja 0-71; 935-965 m. (cuttings); mid-focus; 800x; TH 4:84:35. FIGURE 14: Parviprojectus sp. A sensu Rouse 1977. Retistr iate isopolar pollen with three thin equatorial projections (4 yum to 6 /um) that narrow to a point at their free end. Col pi nar-row and extend only about one third to one half the distance to the poles (Fig. 14b). Zonally nominate species. Range top = Parviprojectus sp. A Zone. Hekja 0-71; 970-1010 m. (cuttings); equatorial view, mid-focus; '900x (Fig. 14a) and 1500x (Fig. 14b); HEK 2:82:9. FIGURES 15 and 16: CorylusfCarpinus spp. Triporate pol len. Group long-ranging but most abundant in early Oligocene sections of study- wells. Range top = T. igniculus Zone. Hekja 0-71; 1205-1250 m. (cut- t ings); polar view, mid-focus; lOOOx; TH 4:84:5 (Fig. 15) and TH 4:84:7 (Fig. 16). FIGURE 17: Myrica sp. Triporate pollen with pronounced annulus. Enlargement of pore area (Fig. 17b) shows coarse granular " teeth- l ike" texture on the inner wall. Range top = T. igniculus Zone. Hekja 0-71; 970-1010 m. (cuttings); polar view, mid-focus; 900x (Fig. 17a) and 1200x (Fig. 17b); HEK 2:82:30. FIGURES 18-21: Ilex spp. E l l i p t i c a l to round tricolporate pollen showing wide variation in size and arrangement of clavate ornamentation. Col pi extend to poles (Fig. 20) and pores indist inct. Range top = F. granulata Zone. Fig. 18: Hekja 0-71; 1205-1250 m. (cuttings); euqatorial view, mid-focus; lOOOx; TH 1/2:84:3. Fig. 19: Kangamiut 1; 2700 m. (cuttings); equatorial view, mid-focus; lOOOx; KANG G:79:27. Fig. 20: Hekja 0-71; 1905-1945 m. (cuttings); polar view, mid-focus; lOOOx; TH 4:84:17. Fig. 21: Hekja 0-71; 2305-2330 m. (cuttings); equatorial view, mid-focus; lOOOx; TH 3:84:7. 84 PLATE 1 PLATE 2 FIGURE 1: Tilia crassipites Wodehouse 1933. Large rounded, ret iculate tricolporate pollen with short colpi obscured by thick pad-like thickenings surrounding the pores. Specimen shows reticulum f iner on one pole (Fig. l b ) and coarser on the other ( F i g . l a ) . Range top = Fagus granulata Zone. Hekja 0-71; 970-1010 m. (cuttings); polar view, low-focus (Fig. l a ) and high-focus (Fig. l b ) ; lOOOx; TH 1:84:26 and 27. FIGURES 2 and 6: Ulmus spp. Triporate to pentaporate pollen with characterist ic but variable rugulate to rugo-verrucate sculpture. Commonly tetraporate and quadrangular (Fig. 2) to rounded (Fig. 6) in outline. Range top = Fagus granulata Zone. Fig. 2: Karlsefni A-13; 8600 f t . (cuttings); polar view, mid-focus; lOOOx; KARL A:80:13. Fig. 6: Hekja 0-71; 970-1010 m. (cuttings); polar view, mid-focus; lOOOx; TH 1:84:17. FIGURE 3: Alnus sp. Porate pollen with variable number of pores ( typica l ly 5). Pores annular and connected by thickened arc i . Range top = Tsuga igniculus Zone. Karlsefni A-13; 6720 f t . (cuttings); po- lar view, mid-focus; lOOOx; KARLA:80:19. FIGURES 4 and 5: Carya spp. Rounded to subtriangular triporate pollen. Pores located equidistantly apart on one hemisphere. Range top = Fagus granulata Zone. Fig. 4: Hekja 0-71; 1905-1945 m. (cut- tings); polar view, mid-focus; lOOOx; TH 3/4:84:30. Fig. 5: Hekja 0-71; 1205-1250 m. (cuttings); polar view, mid-focus; lOOOx; TH 3/4:84:5. FIGURE 7: Juglans sp. Rounded periporate pollen. Range top = Fagus granulata Zone. Hekja 0-71; 1405-1450 m. (cuttings); polar view, mid-focus; lOOOx; TH 1:84:3. FIGURE 8: Jussiaea sp. Psilate triporate pollen with thick "doughnut-like" annulus surrounding pores. Range top = Parviprojectus sp. A Zone. Herjolf M-92; 4500-4510 f t . (cuttings); polar view, mid-focus; 1100x; HERJ 2:81:20. FIGURE 9: Boisduvalia clavatites Piel 1971. Onagraceous triporate pollen with protruding pores that have dissected r idge-l ike appear- ance. Rounded verrucae/gemmae suclptural elements sparsely arranged on outer exine surface. Range top = Parviprojectus sp. A Zone. Herjolf M-92; 4500-4510 f t . (cuttings); polar view, mid-focus; lOOOx; HERJ 2:81:0. 86 FIGURE 10: Rousea araneosa (Frederiksen) Frederiksen 1980. Reticulate tr icolpate pollen. Reticulum characterized by narrow muri and wide lumina which become smaller along the colpus. Range top = Parviprojectus sp. A Zone. Hekja 0-71; 1605-1645 m. (cuttings); equatorial view, mid-focus; lOOOx; TH 1/2:84:14. FIGURES 11 and 12: Araliaceoipollenites granulatus (Potonie) Frederiksen 1980. Granulate tr icolporate pollen. Pores lalongate. Range top = Parviprojectus sp. A Zone. Fig. 11: Hekja 0-71; 1290-1345 m (cuttings); equatorial view, mid-focus; lOOOx; HEK 3:83:7. Fig. 12: Herjolf M-92; 5600 f t . (cuttings); equatorial view, mid-focus; lOOOx; HERJ 2:81:35. FIGURE 13: Acanthaceae sp. Psilate tricolporate pollen with large granules located in the region of the colpus. Range top = Parviprojectus sp. A Zone. Hekja 0-71; 1205-1250 m. (cuttings); equatorial view, mid-focus; lOOOx; TH 1:84:25. FIGURE 14: Rousea monilifera Frederiksen 1980. Coarsely reticulate tr icolpate pollen with coarsely beaded muri. Range top = Parviprojectus sp. A Zone. Hekja 0-71; 1205-1250 m. (cuttings); equatorial view, mid-focus; lOOOx; TH 2:84:35. FIGURE 15: Nyssapollenites sp. Finely reticulate tricolporate pollen with exinal thickenings around pores. Outline subtriangular and sides straight to s l ight ly convex. Range top = Parviprojectus sp. A Zone. Hekja 0-71; 2305-2330 m. (cuttings); polar view, mid-focus; lOOOx; TH 2:84:21. FIGURE 16: Ephedra c l a r i c r i s t a t a Shakhmundes 1965. Range top = Parviprojectus sp. A Zone. Herjolf M-92; 4610-4620 f t . (cuttings); equatorial view, mid-focus; 700x; HERJ 3:81:13. FIGURE 17: Araliaceoipollenites profundus Frederiksen 1980. Large granulate tricolporate pollen with deeply invaginated colpi extending length of grain. Range top = Parviprojectus sp. A Zone. Hekja 0-71; 1205-1250 m. (cuttings); equatorial view, mid-focus; 1200x; TH 1/2:84:9. 87  PLATE 3 FIGURES 1 and 2: Araliaceoipollenites megaporifer Frederiksen 1980. Granulate tricolporate pollen. Oval with rounded ends. Pores large and rounded. Col pi narrow and extending almost the fu l l length of grain. Zonally nominate species. Range top = A. megaporifer Zone. Fig. 1: Hekja 0-71; 1605-1650 m. (cuttings); equatorial view, mid-focus; lOOOx; TH 1/2:84:13. Fig. 2: Herjolf M-92; 5200 f t . (cut- tings); equatorial view, mid-focus; lOOOx; HERJ 2:84:19. FIGURE 3: Tetracolporites cf. T. brevis. Tetracolporate pollen. Psilate to fa int ly punctate ornamentation and lalongate pores. Col pi extend nearly to poles. Range top = Araliaceoipollenites megaporifer Zone. Hekja 0-71; 1405-1450 m. (cuttings); equatorial view, mid-focus; lOOOx; TH 4:84:32. FIGURE 4: Gothanipollis cockfieldensis Engelhardt 1964. Syncolporate pollen. In equatorial view has triangular shape with narrowly rounded, somewhat flared appearance at apertures. Range top = Araliaceoipollenites megaporifer Zone. Herjolf M~92; 4610 f t . (cuttings); polar view, mid-focus; 1200x; HERJ 3:81:28A. FIGURES 5 and 6: Verrutricolporites cruciatus Frederiksen 1980. Verrucate tricolporate pollen. Pores lalongate. Col pi show l i t t l e thickening and extend approx. 4/5 the length of grain. Range top Araliaceoipollenites megaporifer Zone. Fig. 5: Hekja 0-71; 1405-1450 m. (cuttings); equatorial view, mid-focus; lOOOx; TH 1/2:84:22. Fig. 6: Hekja 0-71; 1605-1650 m. (cuttings); equatorial view, mid-focus; lOOOx; TH 4:84:25. FIGURES 7 and 8: tlomipites microfoveolatus (Stanley) Nichols 1973. Triporate pollen. Small (12 yum to 20 /jm) with s l ight ly convex (Fig. 7) to concave (Fig. 8) sides. Range top = Araliaceoipollenites megaporifer Zone. Fig. 7: Hekja 0-71; 1905-1945 m. (cuttings); po- lar view, mid-focus; 1000x; TH 4:84:34. Fig. 8: Kangamiut 1; 2750 m. (cuttings); polar view, mid-focus; lOOOx; KANG E:79:37. FIGURES 9 and 10: Ericaceae tetrads. Tetrads of tr icolpate pollen. Shape of outline varies from triangular (Fig. 9) to rounded (Fig. 10). Rounded forms generally larger than triangular ones. Range top = Fagus granulata Zone. Fig. 9: Hekja 0-71; 1205-1250 m. (cuttings); mid-focus; lOOOx; TH 1:84:16. Fig. 10: Hekja 0-71; 2305-2330 m. (cut- t ings); mid-focus; 800x; TH 3:84:19. 89 FIGURE 11: Rhoipites latus Frederiksen 1980. Tricolporate pollen with rounded to s l ight ly lalongate pores. Ornamentation reticulate with lumina polygonal to longitudinally elongate. Zonally nominate species. Range top = R. latus Zone. Herjolf M-92; 5400 f t . (cut- t ings); equatorial view, mid-focus; 900x HERJ 3:81:17. FIGURE 12: C a p r i f o l i i p i t e s sp. A sensu Rouse 1977. Reticulate tricolporate pollen. Reticulum even and width of muri nearly equal to width of lumina. Pores lolongate. Range top = Rhoipites latus Zone. Herjolf M-92; 5400 f t . (cuttings); equatorial view, mid-focus; 800x; HERJ 2:81:29. FIGURE 13-15: Cupuliferoipollenites spp. Psilate tricolporate pollen. Pores lalongate. Col pi extend 2/3 to nearly fu l l length of grain. Range top = Parviprojectus sp. A Zone.- Fig. 13: Hekja 0-71; 2305-2330 m. (cuttings); equatorial view, mid-focus; lOOOx; TH 3/4:84:15. Fig. 14: Hekja 0-71; 1805-1850 m. (cuttings); equatorial view, mid-focus; lOOOx; HEK 3:83:33. . Fig. 15: Kangamiut 1; 2901 m. (cuttings); equatorial view, mid-focus; KANG 1:81:16. FIGURE 16: Symplocoipollenites sp B. Tricolporate pollen. Granulate. Col pi wide, extend to pole and bordered by exinal thickenings. Pores poorly defined. Range top: Rhoipites latus Zo.ne. Kangamiut 1; 2700 m. (cuttings); polar view, mid-focus; lOOOx; KANG G:79:26. FIGURE 17: Symplocoipollenites sp. A. Reticulate tricolporate pollen. Col pi extend approx. 1/2 to 2/3 the distance to poles and bordered only by slight thickening. Exine thickened at pores. Range top = Rhoipites latus Zone. Hekja 0-71; 1605-1645 m. (cuttings); po- lar view, mid-focus; lOOOx; TH 1/2:84:23. FIGURE 18: Tricolporopollenites kruschii sensu Rouse 1977. Reticulate tricolporate pollen. Reticulum f iner at poles and along co lp i . Col pi show slight marginal thickening and extend nearly to poles. Range top = Rhoipites latus Zone. Hekja 0-71; 1905-1945 m. (cuttings); polar view; mid-focus; lOOOx; TH 4:84:9. FIGURE 19: Verrutricolporites sp. A. Verrucate tricolporate pollen with pronounced lalongate pores and thickenings along co lp i . Colpi extend approx. 4/5 the length of grain. Range top = Roipites latus Zone. Hekja 0-71; 1605-1650 m. (cuttings); equatorial view, mid-focus; lOOOx; HEK 3:83:19. 90 FIGURE 20: Verrutricolporites sp. B.. Verrucate tricolporate pollen with c i rcu lar to lolongate pores. Col pi extend 3/4 the distance to poles. Verrucae large and irregular in design. Exine thicker at poles than at equator. Range top = Rhoipites latus Zone. Hekja 0-71; 1905-1945 m. (cuttings); equatorial view, mid-focus; lOOOx; TH 4:84:23. FIGURE 21: Verrutricolporites sp. C. Verrucate tricolporate pollen with indist inct pores. Col pi without thickenings and extend nearly to poles. Range top = Araliaceoipollenites megaporifer Zone. Hekja 0-71; 1605-1645 m. (cuttings); equatorial view, mid-focus; lOOOx; TH 1/2:84:17. FIGURE 22: Verrutricolporites sp. D. Rounded, verrucate tricolporate pollen with lolongate pores. Col pi with pronounced marginal thickenings extend 4/5 the length of grain. Verrucae large. Range top = Rhoipites latus Zone. Hekja 0-71; 1710-1745 m. (cuttings); equatorial view, mid-focus; lOOOx; HEK 3:83:30. FIGURE 23: Ailanthipites sp. B. sensu Rouse 1977. Retistriate tricolporate pollen with lalongate pores. Range top = Rhoipites latus Zone. Hekja 0-71; 2305-2330 m. (cuttings); equatorial view, mid-focus; lOOOx; TH 4:84:11. FIGURE 24: Bombacacidites bombaxoides Couper 1960. Subtriangular shaped tricolporate pollen with reticulate ornamentation. Reticulum coarser at poles and f iner along equator. Range top = lower Rhoipites latus Zone. Hekja 0-71; 1905-1945 m. (cuttings); 900x; TH 4:84:3. FIGURE 25: Puctodiporites sp. Diporate fungal spore with punctate ornamentation. Distinct co l lar surrounds pores. Range top = Araliaceoipollenites megaporifer Zone. Hekja 0-71; 1905-1945 m. (cut- tings); mid-focus; lOOOx; TH 4:84:12. FIGURES 26 and 27: Pusiformisporites spp. Two-celled fungal spores with longitudinal grooves. Range top = Rhoipites latus Zone. Fig. 26: Roberval K-92; 1900 m. (cuttings); mid-focus; lOOOx; ROB B:81:11. Fig. 27: Hekja 0-71; 1905-1945 m. (cuttings); mid-focus; lOOOx; TH 4:84:7. FIGURES 28 and 29: Striadiporites spp. Diporate fungal spore with ribbed ornmentation. Range top = Rhoipites latus Zone. Fig. 28: Kangamiut 1; 3090 m. (cuttings); mid-focus; lOOOx; KANG 1:79:0. Fig. 29: Hekja 0-71; 1905-1945 m. (cuttings); mid-focus; lOOOx; TH 4:84:10.' 91 PLATE 3 PLATE 4 FIGURES 1, 6 and 11: P i s t i l l i p o l l e n i t e s mcgregorii Rouse 1962. Triporate pollen with variable number of gemmae. Older specimens typ- i ca l l y have fewer gemmae, usually situated near pores (Fig. 11), and younger grains tend to have numerous gemmae (Figs. 1 and 6) that may cover the entire surface of the grain. Range top = P. mcgregorii Zone. Fig. 1: Hekja 0-71; 2020-2030 m. (cuttings); mid-focus; lOOOx; TH 3:84:33. Fig. 6: Karlsefni A-13; 10,500 f t . (cuttings); mid-focus; lOOOx; KARL 1:82:11. Fig. 11: Herjolf M-92; 7200 f t . (cuttings); mid-focus; lOOOx; HERJ 1:81:5. FIGURE 2: Rhoipites angustus Frederiksen 1980. Microreticulate tricolporate pollen with oval to diamond shaped outline. Pores rounded. Colpi appear thickened and extend nearly to poles. Range top = Rhoipites latus Zone. Herjolf M-92; 4610-4620 f t . (cuttings); equatorial view, mid-focus; 800x; HERJ 1:81:30. FIGURES 3 and 4: Platycarya sp. Triporate pollen with 3 equatorial, atriate pores and thin narrow troughs or pseudocolpi on each hemi- sphere. Range top = base Rhoipites latus Zone. Karlsefni A-13; 10,500 f t . (cuttings); mid-focus; lOOOx; KARL 1:82:16 and 17. FIGURE 4: Pesavis tagluensis Els ik and Jansonius 1974. Circular, mult icel lular fungal spore. Stalked central ce l l with two curved l a t - eral arms and centripetal hyphae originating from each primary c e l l . Range top = Rhoipites latus Zone. Kangamiut 1; 2949 m. (cuttings); mid-focus; lOOOx; KANG D:79:23. FIGURE 5: Azolla glochidia. Range top = P i s t i l l i p o l l e n i t e s mcgregorii Zone. Hekja 0-71; 2305-2330 m. (cuttings); mid-focus; 900x; TH 2:84:15. FIGURES 8 and 9: Momipites wyomingensis Nichols and Ott 1978. Small (19 /jm to 27 um), straight to convex sided, triporate pollen with atriate pores. Lacks polar island and tr iradiate scar. Range top = T r i c o l p i t e s sp. A Zone. Herjolf M-92; 7200 m. (cuttings); mid-focus; 900x; HERJ 1:81:15 and 16. FIGURE 10: Momipites ventifluminis Nichols and Ott 1978. Atriate triporate pollen with convex sides. Exine thickening on one hemi- sphere evidenced by three thin, c ircular spots around pole. Range top = T r i c o l p i t e s sp. A Zone. Herjolf M-92; 7022 m. (sidewall core); po- lar view, mid-focus; 900x; HERJ 4:81:15. 93 FIGURE 12: Insulapollenites rugulatus Leffingwel1 1971. Parasyncolpate pollen with coarsely rugulate sculpture in interapical areas. Ornamentation becomes reticulate to f inely reticulate along col p i . Range top = T r i c o l p i t e s sp. A Zone. Herjolf M-92; 7200 f t . (cuttings); polar view, mid-focus; 800x; HERJ 1:82:14. FIGURE 13: pre-Carya. Carya-like triporate pollen in which one or two pores have migrated from one hemisphere to the equator. Range top = T r i c o l p i t e s sp. A Zone. Herjolf M-92; 7022 f t . (sidewall core); polar view, mid-focus; HOOx; HERJ 1:81:17. FIGURE 14: Momipites anellus Nichols and Ott 1978. Conves sides triporate pollen with atriate pores. Thin exine forming a circumpolar ring surround polar area. Similar to M. amplus but smaller in size (18 /um to 27 jum). Range top = T r i c o l p i t e s sp. A Zone. Herjolf M-92; 7300 f t . (cuttings); polar view, mid-focus; 800x; HERJ 3:81:5. FIGURE 15: Momipites amplus (Leffingwell) Nichols 1973. Convex sided triporate pollen with atriate pores situated on the equator. Circumpolar ring of thin exine surrounds pole (very faint in i l l u s - trated specimen). Differs from M. anellus by i t s larger size (29 /um to 37 /um). Range top = T r i c o l p i t e s sp. A Zone. Herjolf M-92; 7100 f t . (cuttings); polar view, mid-focus; lOOOx; HERJ 1:81:3. FIGURES 16 and 17: Paraalnipollenites alterniporus (Simpson) Srivastava 1975. Triporate pollen with pseudopores developed along ridges of exinal thickening (arci) connecting pores. Zonally nominate species. Range top = P. alterniporus Zone. Fig. 16: Herjolf M-92; 7600 f t . (cuttings); polar view, mid-focus; lOOOx; HERJ 2:81:18. Fig. 17: Kangamiut 1; 3447 m. (cuttings); polar view, mid-focus; lOOOx; KANG E:79:26. FIGURE 18: Momipites actinus Nichols and Ott 1978. Straight to con- cave sided triporate pollen with atriate pores and tr iradiate thinning at one pole. Range top = Paraanipollenites alterniporus Zone. Herjolf M-92; 7400 f t . (cuttings); polar view, mid-focus; 800x; HERJ 2:81:21. FIGURE 19: T r i c o l p i t e s parvus Stanley 1965. Reticulate tr icolpate pollen. Range top = T r i c o l p i t e s sp. A Zone. Kangamiut 1; 3600 m. (cuttings); polar view, mid-focus; 900x; KANG G:79:29. FIGURE 20: Taxodiaceaepollenites sp. Range top = Tsuga igniculus Zone. Kangamiut 1; 3600 m. (cuttings); mid-focus; lOOOx; KANG G:79:32. 94 FIGURES 21 and 22: Betulaceoipollenites spp. Triporate pollen with aspidate pores. Range top = P i s t i l l i p o l l e n i t e s mcgregorii Zone. Karlsefni A-13; 13,140 f t . (cuttings); polar view, mid-focus; lOOOx; KARL A:80: l l and 12. FIGURE 23: T r i c o l p i t e s cf. T. hians Stanley 1965. Reticulate tr icolpate pollen. Range top = P i s t i l l i p o l l e n i t e s mcgregorii Zone. Kangamiut 1; 3399 m. (cuttings); polar view, mid-focus; 900x; KANG G:79:19. FIGURE 24: Casuarinidites sp. Triporate, atriate pollen. I l lus - trated specimen appears more coarsely granulate than others repres- ented in this group. Range top = P i s t i l l i p o l l e n i t e s mcgregorii Zone. Herjolf M-92; 7500 f t . (cuttings); polar view, mid-focus; 900x; HERJ A:80:12. FIGURE 25: Laevigatosporites sp. Psilate monolete spore. Range top = Tsuga igniculus Zone. Roberval K-92; 2690 m. (cuttings); mid-focus; lOOOx; ROB C:80:5. FIGURE 26: Piceapollenites sp. Bisaccate pollen. Range top = Parviprojectus sp. A Zone. Herjolf M-92; 7500 f t . (cuttings); mid-focus; 800x; HERJ A:80:5. 95  CHAPTER 3. THE IDENTIFICATION AND DISTRIBUTION OF RECYCLED PALYNOMORPHS IN THE CONTINENTAL SHELF SEDIMENTS OF THE LABRADOR SEA INTRODUCTION The general distr ibution and relative abundances of recycled - pre-Tertiary palynomorphs were determined from selected stratigraphic intervals in seven Labrador Sea wells. The purpose of the study was to find out i f concentrations of certain age-groups of recyclants would reveal any information concerning sediment sources in the Labrador Sea area during a given time. The value of using redeposited palynomorphs as provenance indicators has been demonstrated by a num- ber of workers, including Richardson and Rasul (1978), Askin and E l l i o t t (1982), Legault and Norris (1982), Turner (1982) and Scott and Srivastava (1984). The project was funded by Aquitaine Company of Canada Ltd., (now Canterra Energy Ltd.) on behalf of the Baffin-Labrador Group, a consortium of o i l companies involved in the exploration of hydrocarbons in the Labrador Sea. From north to south, the study wells are Kangamiut 1, Karlsefni A-13, Skolp E-07, Snorri J-90, Herjolf M-92, Roberval K-92 and Cartier D-70. Their location is shown in Figure 1. Paleocene and Eocene sediments are represented in each of the wells with middle and Upper Cretaceous 97 Figure 1 . Location map of the Labrador Sea and the seven offshore wells used in this study. 98 sediments present in Skolp E-07, Herjolf M-92 and Roberval K-92. The oldest penetrated sediments represented in this study were Carboniferous, found at the base of Roberval K-92 between 3550 and 3850 meters. The ages of the sediments are based upon this author's detailed palynological study of the wells. Prepared palynological slides of predominantly cuttings samples from Kangamiut 1, Karlsefni A-13, Skolp E-07, Herjolf M-92 and Cartier D-70 were provided on loan from Total-Eastcan, courtesy of Dr. N. J . McMillan, then of Aquitaine (Canterra Energy Ltd.) and now with the Geological Survey of Canada in Calgary, Alberta. Washed cuttings sam- ples from Roberval K-92 were supplied by Aquitaine (now Canterra). The samples from Snorri J-90 were examined at the Atlantic Geoscience Center in Dartmouth, Nova Scotia, where the palynological slides are on f i l e . CRETACEOUS AND LOWER TERTIARY STRATIGRAPHY OF THE LABRADOR SEA With the exception of small pockets of Cretaceous and Paleogene-aged sediments outcropping on West Greenland and central Baffin Island, land masses adjacent to the Labrador Sea were essential ly stripped of their sediments by continental ice sheets during the Pleistocene (McMillan, 1973; Henderson et a l . , 1981). Our stratigraphic under- standing of the Labrador Sea, therefore, is mainly dependent upon the 99 offshore wells d r i l l ed along the continental margins of the Labrador Sea. In places, total thickness of the Cretaceous and Tertiary sediments is greater than ten kilometers (McMillan, 1980, 1982). The general stratigraphy of the Labrador and West Greenland continental shelves is i l lustrated in Figure 2. Lithostratigraphic nomenclature for offshore Labrador is based on work by Umpleby (1979), McWhae et a l . , (1980) and McMillan (1980, 1982) and for offshore West Greenland by Rolle (1985). The offshore Labrador wells were d r i l l ed into graben structures asso- ciated with the Saglek (Karlsefni A-13 and Skolp E-07) and Hopedale (Snorri J-90, Herjolf M-92, Roberval K-92 and Cartier D-70) basins, which are separated from one another by the Okak Arch. The Okak Arch represents a remnant structural feature related to fractures formed when Greenland and Labrador separated (McMillan, 1980; 1982). The thickness of sediments in the wells is dependent upon the control of basement highs. Cretaceous sediments are generally restricted to the central portions of the basins, whereas Tertiary sediments tend to drape over the Okak and Cartwright arches (Hiscott, 1984). Kangamiut 1 was d r i l l ed on a horst structure located offshore West Greenland (Rolle, 1985). 100 LABRADOR SHELF* WEST GREENLAND SHELF* PLEISTOCENE O O N O z u i U LU z LU CD O LU z LU z LU C3 O LU - J £ PLIOCENE MIOCENE ? OLIGOCENE EOCENE PALEOCENE GLACIAL DEPOSITS UPPER SAGLEK MUDSTONE LOWER SAGLEK MUDSTONE 2 LEIF MEMBER MUDSTONE (KENAMU FORMATION^ CARTWRIGHT^ GUDRID' FM ^ — ^ FM GLACIAL DEPOSITS MANITSOQ FM ATANEQ FM KANGAMIUT FM HELLIFISK FM IKERMIUT FM Figure 2. Generalized l i thostrat igraphic columns of offshore Labrador and West Greenland (not to scale). Based on Umpleby (1979)*, McWhae et a l . (1980)* and Rolle (1985)**. The Labrador Sea represents a fa i led r i f t basin that formed during the breakup of Labrador and Greenland from Early Cretaceous to latest Eocene/earliest Oligocene time (Gradstein and Srivastava, 1980). Dur- ing the i n i t i a l phase of crustal extension, local ly derived, nonmarine f luv ia l sediments of Early Cretaceous age were deposited into the newly developed graben basins. On the Labrador Shelf, the Lower Cretaceous Bjarni Formation is mainly comprised of variable thick- nesses of arkosic sandstones, gray s i l t y shale and thin coal beds (Umpleby, 1979). It was penetrated in Skolp E-07, Herjolf M-92 and Roberval K-92. Commencement of actual sea-floor spreading is marked by deposition of. the dark marine, ner i t ic to upper bathyal shales of- the Markland For- mation, which unconformably overlies the Bjarni Formation (Avalon Un- conformity, McWhae et a l . , 1980). In some wells (e.g:, Skolp E-07), the marine shales are intertongued with nearshore sands of the Freydis Member. Based upon the presence of marine dinoflagellates with re- str icted range tops in some of the Labrador Sea wells (Barss et a l . , 1979; this author's observation), the f i r s t incursion of marine waters into the newly developing Labrador Sea may have occurred as early as late Turonian to Coniacian time. Gradstein and Berggren (1981) report the f i r s t open-marine foraminiferal assemblages in the Labrador Sea to be Campanian to Maastrichtian in age. 102 Sedimentation along the continental margins of the Labrador Sea was interrupted near the Maastrichtian-Danian boundary. The unconformity (Bylot Unconformity) is not everywhere recognizable but is probably early Danian in age (McWhae et a l . , 1980; Rolle, 1985). This hiatus corresponds to the worldwide, f i r s t order marine regression of Vail et a l . (1977). During the Paleocene and early Eocene, large volumes of brown to gray shales and mudstones of the Cartwright Formation were being deposited into rapidly subsiding basins. McWhae et a l . (1980) interprets most of these sediments to represent turbidite deposits. Coarse-grained turb id i t i c deep-sea fan deposits of the Gudrid Formation are found in association with the Cartwright in some of the wells, including Cartier D-70. Agglutinated "f lysch-type" foraminiferal assemblages indicate increasing bathyal depths along the Labrador Shelf at this time, with maximum transgression during the early Eocene (Gradstein and Srivastava, 1980). This was followed by a phase of marine regression characterized by a shallowing of sea level and deposition of the coarsening upward se- quence of shales, si ltstones and sandstones of the unnamed Mudstone unit of Umpleby (1979), i . e . , Kenamu Formation of McWhae et a l . (1980). It coincides with the cessation of sea-floor spreading in the Labrador Sea, just prior to Anomaly 13 (Gradstein and Srivastava, 1980). The Cartwright and Kenamu formations are roughly equivalent to 103 the Ikermiut and Kangamiut formations, respectively, from offshore West Greenland (Rolle, 1985). The middle and late Oligocene is poorly understood in the Labrador Sea and according to this study and the foraminiferal studies of Gradstein (Gradstein and Srivastava, 1981), may be absent along much of the Labrador Shelf. It marks a period of time characterized by erosion and/or lack of sedimentation. IDENTIFICATION OF RECYCLED PALYNOMORPHS The recognition of redeposited palynomorphs is important for helping to determine the sources from which sediments are derived, as well as for helping to solve stratigraphic problems. In sediments where recy- cled palynomorphs comprise the bulk of an assemblage, problems with dating and correlating the sediments can often result from the misin- terpretation of the age of the redeposited grains. For example, in an unpublished study by this author concerning the dating and correlation of coal and shale units in south central Alberta, the age of the sediments appeared to be Maastrichtian. The palynomorph assemblage was characterized by such well preserved and abundant diagnostic pollen as Aquilapollenites conatus, A. reticulatus, Wodehouseia spinata, Proteacidites thalmanii and Gunnera microreticulata . An ex- amination of interbedded ex in i t i c - r i ch coal seams in the area, how- ever, yielded good lower to middle Paleocene palynofloral assemblages characterized in part by the presence of Wodehouseia fimbriata, 104 Insulapollenites rugulatus and Maceopolipollenites amplus. The re- sults demonstrated that the numerous Maastrichtian palynomorphs were recycled and that the age of the sediments was actually Paleocene. The ident i f icat ion of palynomorphs as recycled is not always easy, however, and can be complicated by a combination of factors, including the age and state of preservation of the recyclants, the type of sam- ple collected (e.g., cuttings, sidewall core or outcrop) and the ther- mal history of the region. Aranova (1960), Wilson (1964) and Stanley (1966) discuss different methods that can be used to identify recyclants under br ight - f ie ld i l lumination. These c r i t e r i a include taxonomic ident i f icat ion, d i f fer ing degrees of preservation, accept- ance of stain and palynomorph color. Bujak and Davies (1982, 1983), on the other hand, discuss the use of fluorescent l ight microscopy to distinguish reworked palynomorphs from indigenous ones, in Neogene strata from the Beaufort Sea and Upper Jurassic to Lower Tertiary sediments from offshore eastern Canada. By far the most rel iable method of determining redeposited palynomorphs is taxonomic identi f icat ion of species. Unfortunately, morphological detai ls necessary for determining species are often ob- scured due to oxidation, maturation and both biological and physical degradation. Also, many species have such long ranges that i t is pos- sible for them to belong to more than one group of recycled palynomorphs, e.g., s imilarly appearing bladdered conifer and 105 taxodiaceous pollen have ranges extending from the Jurassic to Recent and the monolete fern spore, Laevigatosporites appears to range from the Paleozoic to Recent. Although older recycled palynomorphs often cannot be identi f ied down to species leve l , i t is usually possible to assign the redeposited grains to a particular genus. If the stratigraphic range of the genus is of f a i r l y short duration, i t s identif icat ion can be suff ic ient enough to allow i t to be assigned to a particular group of recyclants. However, i f a palynomorph cannot be identif ied taxonomically or i f i t is long-ranging, i t is necessary to use more subjective methods of ident i f icat ion. The color of pollen and spores is often useful for distinguising the relative age of a recylant. Pollen and spores undergo a systematic change in color from l ight yellow-green, to yellow to yellow-orange to brown to black with increasing thermal maturation (Correia, 1967; Staplin, 1969; Raynaud and Robert, 1976). Usually, the older palynomorphs have undergone a more intensive thermal history than younger ones and are, therefore, darker. Because the samples in the study slides were subjected to oxidation (e.g., n i t r i c acid) in the laboratory during sample preparation, the actual thermal alteration of these samples could not be determined. However, because the older pollen and spores generally retain the same relative differences in color as those in the kerogen preparation, palynomorph color can be 106 used with some qual i f icat ion. When using color for ident i f icat ion, however, i t is necessary to take into consideration wall thickness and ornamentation. Thick-walled and heavily ornamented specimens are i n - variably darker than grains of the same age and thermal history, but with thinner walls and l i t t l e to no ornamentation. Unlike pollen and spores, dinoflagellates and other marine algae do not show a systematic change in color through time and increasing thermal maturation. Although there have been some attempts made to use color changes in acritarchs to monitor thermal maturation, the re- sults to date are too variable to use with any certainty. The unpre- dictable response of marine palynomorphs to changes in thermal maturation are very l ike ly the result of differences in wall composi- t ion. For that reason, color is not a part icular ly useful parameter for distinguishing recycled dinoflagellates, acritarchs and other ma- rine algae from those that are in place. Another useful technique for identifying recyclants is the ab i l i t y of the various wall layers of palynomorphs to accept organic stains such as Safranin-O. Wall composition and thickness, relative state of preservation and, especial ly, the degree of thermal maturation a l l help to determine the staining characteristics of the grains (Stanley, 1966). 107 In the Labrador Sea wells, staining characteristics are most useful for distinguishing recycled Tertiary pollen and spores. Contemporaneous early and middle Paleocene pollen and spores pick up only a s l ight, f a i r l y even stain and late Paleocene and Eocene ones pick up an even, red stain. In contrast, Paleocene and/or early Eocene pollen and spores recycled into younger sediments character- i s t i c a l l y have an uneven stain. Caved modern pollen and spores usu- a l l y pick up a purplish red stain. Older pollen and spores (Paleozoic to Cretaceous) either do not or only part ia l ly pick up stain, which is probably due to changes in exine composition brought on by their higher degree of thermal maturation. It is considerably more d i f f i c u l t to use staining characterist ics to identify recycled and caved dinoflagellates and other marine algae. Some dinoflagellates, regardless of age, tend to be resistant to staining and others, of the same age, wi l l often exhibit di f ferent i n - tensit ies of color. In general, however, older, more thermally mature recycled dinoflagellates do not stain and, therefore, can be used to help spot recyclants, especially in thermally immature sediments. In some circumstances, the state of preservation of the palynomorphs can be useful for determining redeposited grains.. Older reworked palynomorphs are often less well preserved than younger recycled and/or contemporaneous grains. Depending upon the depositional his- tory and number of orders of recycl ing, redeposited grains tend to 108 show a greater degree of chemical, biological and/or mechanical break- down. This particular property, however, is probably the least r e l i - able method to use for identifying recycled palynomorphs and should, therefore, be used only in conjunction with other c r i t e r i a . Under certain conditions, the recyclants can actually be better preserved than in-s i tu grains. This is especially true in situations where the contemporaneous palynomorphs have been subjected to extensive oxidation or bacterial decay. If the recyclants have been protected from degradation, e.g., by rapid deposition and bur ia l , they may be well-preserved. Thermally immature to mature ex in i t ic (hydrogen-rich) organic matter (including pollen, spores and dinoflagellates) fluoresces when excited with ultravio let or blue l ight (Bostick, 1979; van G i j ze l , 1979; Teichmuller and Durand, 1983). Whether biochemical, as suggested by Bujak and Davies (1982, 1983), or thermochemically induced, younger, thermally immature palynomorphs ( v i t r i n i te reflectance of approxi- mately .2 to .3) emit blue to green wavelengths and older, more thermally mature ones emit yellow to orange to red wavelengths un t i l , at a v i t r i n i t e reflectance of between 1.1 and 1.3, fluorescence be- comes extinct (Senftle, personal communication). The intensity and color of fluorescing palynomorphs can sometimes be very useful for identifying redeposited grains. It is a qualitative technique and, although i t is best to use kerogen preparations, this 109 type of non-quantitative fluorescence can be measured on slides of macerated samples that have undergone chemical oxidation in the labo- ratory (Senftle, personal communication; Bujak, personal communi- cation). This technique was used with limited success in the Roberval K-92 well (samples from the remaining study wells were not available for examination in fluorescent l i ght ) . Unfortunately, the mounting medium used during slide preparation was too fluorescent to provide real ly good results. Nevertheless, two different populations of Carboniferous recyclants as well as redeposited Cretaceous grains could be distinguished. Older Tertiary palynomorphs redeposited into younger strata were more d i f f i c u l t to identify, however, because there was less contrast in the color and intensity of fluorescence. In spite of th is , Paleocene and Eocene recyclants found in the Neogene sections of the well tended to fluoresce less intensely and appeared a deeper, more orange-red color than palynomorphs indigenous to the sediment. It should also be noted that the dinoflagellates in these samples often emitted not only a brighter fluorescence than pollen and spores of the same age, but also appeared to exhibit less variation in fluorescence intensity and color between Neogene and Paleogene forms than did the pollen and spores. The use of fluorescence to identify populations of recycled palynomorphs needs further study but i t ap- pears to be a promising technique. In general, there are no sure methods to actually identify and accu- rately date every recyclant in a sample. However, by using the above 110 described techniques, i t is possible to determine different general "age" populations of recyclants and their relat ive abundances through time. Usually, the older the recyclants, the easier i t is to recog- nize them as being redeposited and, hence separate them into different groups. CATEGORIES OF RECYCLED PALYNOMORPHS The recycled pollen, spores and dinoflagellates found in the Cretaceous and Tertiary shelf sediments of the Labrador Sea are d iv i s - ible into four major groups, categorized on the basis of relative age. Only three of these groups of recyclants ( i . e . , Paleozoic, Upper Jurassic/Lower Cretaceous and Upper Cretaceous) wi l l be considered. The fourth group, which, is comprised of Paleogene recyclants, is dicussed in CHAPTER 4. A brief summary of the parameters used to help identify these different populations of redeposited palynomorphs is given in Figure 3. Paleozoic Group Recycled Paleozoic assemblages include: Calamospora sp. Convolutisporites sp. Densosporites spp. I l l POLLEN AND SPORES DINOFLAGELLATES AND OTHER MARINE ALGAE G R O U P S O F  R E C Y C LA N T S UPPER CRETACEOUS USUALLY ASSIGNABLE TO GENUS AND SPECIES USUALLY LIGHT BROWN OR MEDIUM YELLOW- BROWN CAN PICK UP SOME STAIN USUALLY WELL-PRESERVED LOW FLUORESCENCE USUALLY ASSIGNABLE TO GENUS AND SPECIES COLOR UNDIAGNOSTIC— USUALLY CLEAR STAIN ACCEPTANCE VARIABLE USUALLY WELL PRESERVED LOW TO MEDIUM FLUORESCENCE G R O U P S O F  R E C Y C LA N T S UPPER JURASSIC/ LOWER CRETACEOUS USUALLY ASSIGNABLE TO GENERA, BUT MANY LONG-RANGING VARIOUS SHADES OF BROWN. DEPENDING UPON THICKNESS AND ORNAMENTATION DO NOT ACCEPT STAIN ORNAMENTATION SOMEWHAT REDUCED NON FLUORESCING USUALLY ASSIGNABLE TO GENUS COLOR UNDIAGNOSTIC DO NOT ACCEPT STAIN PRESERVATION FAIR NON-FLUORESCING? G R O U P S O F  R E C Y C LA N T S PALEOZOIC USUALLY ASSIGNABLE TO GENERA WITH RESTRICTED PALEOZOIC RANGES DARK BROWN TO RED-BROWN COLOR VERY DIAGNOSTIC DO NOT ACCEPT STAIN ORNAMENTATION REDUCED OR ABSENT NON-FLUORESCING (EXCEPT SUB-GROUP OF PZ SPORES IN ROBERVAL K-92) . (NO DATA) Figure 3. Summary of methods used to help identify different groups of redeposited palynomorphs in the Cretaceous and Tertiary shelf sediments of the Labrador Sea. Florinites spp. Lycospora spp. Lycospora cf. L. pusilla Knoxisporites sp. Murospora spp. Punctatisporites minutus Kosanke Triquitrites spp. T. additus Wilson & Hoffmeister T. crassus Kosanke The Paleozoic recyclants are comprised of non-marine monolete and t r i l e t e spores that can be divided into two general populations, based upon their physical appearance. One of these is characterized by f a i r l y well preserved spores that are medium yellow-brown in color un- der br ight - f ie ld i l lumination. They are very abundant in' Roberval K-92 and consist almost exclusively of species belonging to the genera Lycospora, Triquitrites and Punctatisporites. The other group of Paleozoic recyclants is more diverse and considerably less abundant and tends to be more poorly preserved (ornamentation is either reduced or missing), as well as darker brown to amber in color. Both sets of redeposited Paleozoic spores are f a i r l y easy to. distinguish from the younger recyclants, because of their d i s t inct morphology. Also, nei - ther group accepts stain. Although there was no attempt to divide this rather broad group of re- deposited grains into f iner "age" categories, many of the recyclants are probably Devonian and/or Carboniferous. The stratigraphic ranges of the genera Calamospora, Densosporites, Lycospora, Knoxisporites and Punctatisporites, are generally thought to be restr icted to the 113 Devonian and/or Carboniferous (Tschudy and Scott, 1965; Barss, 1967; Felix and Burbridge, 1967). Murospora peaked in the Mississippian, although several species have been described from the Mesozoic, and F l o r i n i t e s ranges from the Pennsylvanian (peak abundance) to the Permian (Tschudy and Scott, 1965). Upper Jurassic/Lower Cretaceous Group Recycled Upper Jurassic/Lower Cretaceous assemblages include: Alisporites bilateralis Rouse Appendicisporites spp. Callialasporites dampieri (Balme) Dev Cerebropollenites mesozoicus (Couper) Nilsson Cicatricosisporites august us Singh C. h a l l e i Del court & Sprumont C. mohroides Del court & Sprumont Classopollis classoides (Pflug) Pocock & Jansonius Concavissimisporites sp. Exesipollenites tumulus Blame Foveotriletes sp. Hamulatisporites sp. Leptolepidites verrucatus Couper Matonisporites sp. Osmundacidites wellmanii Couper Podocarpidites biformis Rouse Many of the species represented in this category are generally long-ranging, with ranges extending from the Upper Jurassic to the Lower Cretaceous (Couper, 1958; Brenner, 1963; Dettmann, 1963; Singh, 1971; Brideaux and Mclntyre, 1975; and Srivastava, 1977). Even though a few species have ranges that reportedly extend up into the Cenomanian, they were placed within this group. The recyclants are, for the most part, non-marine and f a i r l y easy to distinguish 114 taxonomically from Paleozoic and Upper Cretaceous redeposited palynomorphs. Their preservation is generally f a i r , they are medium to dark brown in color and they do not accept stain. Although the age of this group of redeposited grains must be consid- ered to range from the Late Jurassic to Early Cretaceous, i t is very l ike ly Early Cretaceous. None of the taxa in this category are re- str icted to the Jurassic. Also, Jurassic sediments have not been found during d r i l l i n g along the continental shelves of the Labrador Sea. The oldest Mesozoic sediments reported to date belong to the f luv ia l -de l ta i c , Lower Cretaceous Bjarni Formation. Upper Cretaceous Group Recycled Upper Cretaceous assemblages include: Aquilapollenites spp. A. quadrilobus Rouse BalmeisporitesIGhoshispora sp. Cyathidites minor Couper Gleicheniidites senonicus Ross Proteacidites thalmanii Anderson Wodehouseia spinata Stanley Alterbia spp. Chatangiella spp. Cyclonephelium distinctum Deflandre & Cookson Dinogymnium spp. Odontochitina operculata (0. Wetzel) Deflandre Oligosphaeridium complex (White) Davey & Williams 115 The Upper Cretaceous recyclants are comprised of both marine and non-marine palynomorphs. They are generally well preserved and can usually be ident i f ied down to species level . The pollen and spores may accept some stain and are generally medium yellow-brown in color. The dinoflagellates and acritarchs, on the other hand, are usually clear and may or may not pick, up stain. A Late Cretaceous age has been assigned to this group based upon the well documented age ranges of many of i t s constituents from North America (Srivastava, 1969 and 1972; Harland, 1973; Mclntyre, 1974; May, 1980; and Nichols and Jacobson, 1982. Those species (e.g., Cyclonephelium distinctum, Oligosphaeridium complex and Odontochitina operculata) that have range bases that extend down into the mid and/or Early Cretaceous and that show no. variation in color, preservation or stain acceptance were as- signed to the younger category. RESULTS AND DISCUSSION The relat ive abundance of the Paleozoic, Upper Jurassic/Lower Cretaceous and Upper Cretaceous groups of recyclants, and their d i s - tr ibution in selected intervals from the seven study wells, are shown in Figure 4. For most samples, counts of 200 in-s i tu and recycled palynomorphs (including pollen, spores and dinoflagellates) were made. An attempt was made to identify the " re la t ive" age of a l l specimens. 116 KANGA- MIUT 1 KARL- SEFNI A-13 SKOLP E-07 SNORRI J-90 HERJOLF M-92 ROBER- VAL K-92 CARTIER D-70 1 2 3 1 2 3 1 2 3 1 2 3 1 2 3 1 2 3 1 2 3 LATE-MIDDLE MIOCENE • • O EARLY MIOCENE • • O • • • EARLY OLIGOCENE • O • — • • • • O A A R Y  EARLY OLIGOCENE/ LATE EOCENE • • • • • O • • A E R T I LATE EOCENE • • O • • o • • • • • O • • A • • O t— EARLY EOCENE • • O • • o • O — • • • • • o • • • • • O LATE-MIDDLE PALEOCENE • • o • • o • • O • • O • O o • • • • • o EARLY PALEOCENE • A • o • • o • • O • o A • A • • — CO - i MAASTRICHTIAN • • • • • o • • A • O — C E O I CAMPANIAN- TURONIAN • • • • • —' • A C R E T A  ALBIAN- CENOMANIAN • • • • • A C R E T A  NEOCOMIAN • o • • Figure 4. Distribution of relative abundances of recycled Paleozoic ( 3 ) , Upper Jurassic/Lower Creta- ceous (2) and Upper Cretaceous (l) palynomorphs in seven Labrador Sea wells. Symbols repre- sent the following relative abundances: - absent; O r a r e ; © s p a r s e ; •uncommon; • common; A very common; and A abundant. When in doubt about certain long-ranging species, however, the younger age was assigned. Because of the uncertainties involved with ident i - fying and determining the age of recyclants, relat ive frequencies ( i . e . , rare = 1, scarce = <5, uncommon = 4-9, common = 10-20, very common = 21-30 and abundant = >30) are used in the following d i s - cussion . The greatest overall concentration of redeposited palynomorphs is found in the Eocene sections of the wells. There is no apparent lat itudinal control over the distr ibution and species composition of the recyclants from north to south. Cartier D-70, the most ' southerly well, and Skolp E-07 both have f a i r l y low numbers of recycled grains, whereas Roberval K-92, and Herjolf M-92 have the greatest concen- trations. The dark brown to amber, f a i r l y poorly preserved population of recy- cled Paleozoic spores previously described were generally sparse to rare. In the Albian-Cenomanian sections of Skolp E-07 and Herjolf M-92, however, they do show a sl ight increase in number. Reworked Carboniferous spores were also reported in four other offshore West Greenland wells (Rolle, 1985) in addition to Kangamiut 1. The species composition of the redeposited Carboniferous grains is comprised of taxa that are found represented in in-s i tu Carboniferous spore assemblages recovered from Roberval K-92 and Gudrid H-55 (also located along the southern edge of the Labrador shelf). Although many of the 118 spores have broad geographical ranges, the s imilar ity in taxa may i n - dicate that the recycled Paleozoic grains were derived from local Carboniferous-aged strata. Another possible source of Paleozoic recyclants might have been highlands associated with the Appalachian system, located south to southwest of the Labrador Sea. According to McMillan (personal communication) the Paleozoic sediments penetrated in Roberval K-92 and Gudrid H-55 along the southern Labrador shelf could possibly represent Appalachian outl iers. In Roberval K-92, there is an anomalous occurrence of a group of very abundant, medium yellow-brown Paleozoic (Carboniferous?) recyclants, dominated almost exclusively by the three genera Lycospora, T r i q u i t r i t e s and Punctatisporites. The origin and distr ibution of this set of redeposited grains is very d i f f i c u l t to interpret. A l - though i t is possible that they were introduced into Roberval K-92 as contaminants during d r i l l i n g , Paleozoic mud and other palynomorph en- riched additives were reportedly not used (McMillan, personal communi- cation). Also, the cuttings samples were thoroughly washed and, in some instances, carefully picked. This group of recyclants has a bimodal distribution in Roberval K-92, with peaks of abundance in the Late Cretaceous and in the latest Eocene to early Oligocene. They reach their greatest concentration in the lower Oligocene section of the well. At f i r s t glance, i t would appear as though a Lycospora-Triquitrites-Punctatisporites spore-rich 119 rock of probable Carboniferous age was extensively eroded over a very substantial period of time. Temporary physical changes in the source area or shifts in paleocurrent directions, could help account for fluctuations in relative abundances. The sediments from the well, however, do not show any signif icant breaks or changes in the relative frequency of other recyclants or in clay mineral composition (Hiscott, 1984) during the late Paleocene and early Eocene, a period of time during which the anomalous Paleozoic spores are greatly reduced in number. Another possible explanation for the distr ibution of this anomalous assemblage in the Roberval K-92 well is that the Upper Cretaceous sediments in which the spores were i n i t i a l l y redeposited, were subse- quently eroded and redeposited into the younger sediments by multiple, recycling events. Perhaps even more l ike ly is that the spores found in the Cretaceous sections of the well represent cavings contamination from the upper Eocene to lower Oligocene portions of the well. Sidewall cores and the cal iper curve (useful for helping to identify severely caved sections in a borehole) from the well would have been useful for resolving this problem, but neither were available for study. If concentrations of the Lycospora-Triquitrites-Punctatisporites dominated assemblage are rea l , they l ike ly represent a very local phenomenon, because of their re- str ict ion to the Roberval K-92 well. However, i t is d i f f i c u l t to rec- oncile the abundance of this group of recyclants in Roberval K-92 with 120 i t s absence (and the overall low number of recyclants in general) in nearby Cartier D-70. As in the other wells, only sparse to rare occurrences of the other group of Paleozoic recyclants were noted in Roberval K-92. These recyclants are not only darker and more degraded than the anomalous, three genera dominated group, but also they have no fluorescent prop- ert ies. The Lycospora-Triquitrites-Punctatisporites assemblage, on the other hand, is characterized by a very low, dark reddish-brown fluorescence, indicating different thermal histories for the two groups and, therefore, separate sources. Upper Jurassic/Lower Cretaceous recyclants are f a i r l y uncommon throughout the studied intervals. They reach their peak abundance in the mid-Cretaceous sections of Skolp E-07 and Herjolf M-92 and are un- common to rare in the younger sediments. Because most of the grains in this group of recyclants found in the Cretaceous sections of the wells are non-marine and resemble the Lower and mid-Cretaceous pollen and spore assemblages found in the Bjarni Formation, many of the recyclants may have been derived local ly from the erosion of the Bjarni Formation. Although they are never abundant, the greatest concentration of Upper Cretaceous recyclants is found in the lower Paleocene in Snorri J-90 and Roberval K-92 and in the Eocene in Herjolf M-92. Karlsefni A-13 121 has increased numbers of Upper Cretaceous recyclants in both the lower Paleocene and Eocene. In Skolp E-07 and Cartier D-70, Upper Cretaceous grains redeposited into Tertiary strata are not very com- mon . Some of the taxa (e.g., Aquilapollenites spp., Wodehouseia spinata and Balmeisporites) represented in the group of Upper Cretaceous recyclants were not found as part of the in-s i tu Late Cretaceous pollen and spore assemblages from the Labrador Sea. They are, how- ever, common palynofloral constituents with well-documented occur- rences in the western inter ior and Arct ic regions of Canada. Their presence in the Tertiary Labrador Sea sediments suggests the poss ib i l - i ty that these recyclants were transported for long distances from sources located in the Canadian western inter ior and Arct ic . In addition to the presence of the pre-Tertiary groups of recyclants, recycled Paleogene palynomorphs were also noted throughout the T e r t i - ary sections of the wells (see CHAPTER 4). The Paleogene recyclants are comprised primarily of pollen and spores and reach peak abundance in the late Eocene and up into the early Oligocene. In Karlsefni A-13, the most northerly of the study wells, the relative number of Paleogene recyclants increases upwards from the late Paleocene to the Miocene, where i t reaches i t s greatest abundance. In Roberval K-92, Herjolf M-92 and Snorri J-90, Paleogene recyclants are most numerous in the middle to late Eocene. In the Eocene sections of Cartier D-70 122 and Skolp E-07, Paleogene recyclants are f a i r l y common but never abun- dant. Petrologic studies by Higgs (1977) and Hiscott (1984) indicate that the provenance of sediments in the Labrador Sea during the Cretaceous was local . Higgs examined Cretaceous and lower Paleocene sands from the continental shelf of the Labrador Sea and onshore western Greenland. The mineralogical and textural immaturity of the grains indicated local sources that underwent rapid erosion and short trans- portation. The sediment source rocks were comprised predominantly of acidic plutonics and amphibolite-facies metamorphics. These results were supported by Hiscott, who studied the clay mineralogy of fine-grained Cretaceous and Tertiary sediments from six Labrador Sea wells (including Roberval K-92). He found that the middle and Upper Cretaceous marine shales of the Labrador Sea were characterized by a predominance of local ly sourced smectite. Palynological evidence for determining the provanance of sediments for the Cretaceous is not very conclusive, because many of the species in question are rather common forms that have f a i r l y broad geographical distr ibutions. However, the general s imi lar ity in composition, pres- ervation and color of many of the recycled Carboniferous and Cretaceous taxa in the Cretaceous Bjarni and Markland formations to in -s i tu Carboniferous (in the Roberval K-92 and Gudrid H-44 wells) and 123 Cretaceous palynomorph assemblages suggest that the source of the recyclants may have been relat ively local . The great thickness of Tertiary sediments, i f derived from s t r i c t l y local sources, would require adjacent highlands and a high rate of up- l i f t to keep pace with sediment i n f i l l i n g the offshore basins. To the south along the Atlantic coastal plain of eastern North America, there are also thick sequences of sediments, however, their source can be traced to the Appalachians (Mathews, 1975). Unfortunately, the almost virtual absence of Mesozoic and Tertiary outcrops in the circum-Labrador Sea region makes i t d i f f i c u l t to determine i f re la - t ively local strata provided the preponderance of sediment delivered offshore. The apparent random distribution and mixed composition of recyclants in the Lower Tertiary Cartwright and Kenamu formations (as well as Ikermiut and Nukik formations from offshore West Greenland) also makes i t d i f f i c u l t to determine provenance. Provenance interpretations for these strata are further complicated by the redistribution and mixing of recyclants on the ocean floor by turbidity currents. Nevertheless, the detailed palynological study of in-s i tu and redeposited Paleogene pollen and spores from the Labrador Sea by this author suggests that the sediment (including the palynomorphs) source area may have encom- passed parts of the western interior and Arctic regions of Canada (see CHAPTER 4). 124 Hiscott (1984) found that the Lower Tertiary sediments were character- ized by a mixed smectite-i11ite-kaolinite assemblage of clay minerals. The composition and homogeneity of this polycyclic clay suite is also indicative of a multiple source, such as would be expected from a large, intercontinental drainage basin, encompassing thousands of square kilometers. The existence of such a large r iver drainage sys- tem covering much of inter ior Canada and parts of the Canadian Arct ic during the Tertiary was suggested by McMillan (1973), in order to ac- count for the great volume of sediment accumulated along the cont i - nental margins of the Labrador Sea. This r iver system would be akin to the modern Mississippi and Mackenzie rivers in that in each of these regimes not only is the volume of sediment considerable but also the percentage of redeposited palynomorphs is very high. If the drainage basin of the proposed Tertiary r iver system carrying sediment to the Labrador Sea is as vast as postulated by McMillan, then i t is d i f f i c u l t to determine the actual sources from which the recycled palynomorphs were eroded. In addition, the different re la - tive age populations of recyclants could represent mixtures of either f i r s t - cyc le and/or multiple cycles of redeposition. 125 SUMMARY 1. The relat ive abundances of Paleozoic, Upper Jurassic/Lower Cretaceous and Upper Cretaceous recycled palynomorphs were determined for Tertiary and Cretaceous aged sediments from seven Labrador Sea wells. Recyclants were identi f ied and categorized whenever possible on the basis of their taxonomic ident i f icat ion, otherwise, the degree of maturation, state of preservation and acceptance of stain were used for ident i f icat ion. 2. With the exception of Roberval K-92, Paleozoic recyclants are low in number and f a i r l y evenly distributed among each of the wells. In Roberval K-92, however, there are anomalously high percentages of a three genera-dominated group of Carboniferous? spores in the Upper Cretaceous and upper Eocene to lower Oligocene sections of the well. The number of Upper Jurassic/Lower Cretaceous recyclants is f a i r l y low except for a s l ight increase in Kangamiut 1 at the top of the upper Paleocene. Skolp E-07, Herjolf M-92 and Roberval K-92 also have s l ight ly higher proportions of Upper Jurassic/Lower Cretaceous rede- posited grains in the mid and lower Cretaceous sections of the wells. Moderate to re lat ively high frequencies of Upper Cretaceous reworks are f a i r l y common throughout the Upper Cretaceous and Tertiary 126 sections of the wells, but generally show no particular overall pat- tern of concentration when compared between wells. 3. Within the Upper Jurassic/Lower Cretaceous population of reworked palynomorphs, some of the redeposited taxa can be ident i f ied as Lower Cretaceous rather than Jurassic. The remaining recyclants within this group have ranges that extend across the Upper Jurassic and Lower Cretaceous boundary and can not be def in i t ive ly c la s s i f ied. Due to certain physical characteristics (e.g., color and preservation), how- ever, they are considered of probable Early Cretaceous age. Because of the lack of recycled palynomorphs with restr icted Jurassic ranges and the absence of reported Jurassic sediments in any of the Labrador Sea wells d r i l l ed to date, i t appears unlikely that Jurassic aged strata are present in the offshore Labrador and West Greenland subsur- face. 4. Recycled palynomorphs recovered from Cretaceous sediments in Skolp E-07, Herjolf M-92 and Roberval K-92 were probably derived from local sources. There is a s imilar ity in species composition between the re- cycled Upper Jurassic/Lower Cretaceous palynomorph assemblages in the middle and Upper Cretaceous strata in these wells and the taxa indigenous to the Lower Cretaceous Bjarni Formation. Mineralogical studies by Higgs (1977) and Hiscott (1984) also indicate local sources for the Cretaceous sediments. 127 5. 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Congress, Bucharest, 1979, P r o c , 2, 165-175. , 1982. Canada's east coast: the new super petroleum province. J . Can. Pe t ro l . Technology, 21:2, 1-15. . McWhae, J . R. H., R. E l i e , K. C. Laughton and P. R. Gunther, 1980. Stratigraphy and petroleum prospects of the Labrador shelf. B u l l . Can Pe t r o l . Geol. , 28, 460-488. Nichols, D. J . and S. R. Jacobson, 1982. Palynostrat igraphic framework for the Cretaceous (Albian-Maestr icht ian) of the over- thrust be l t of Utah and Wyoming. Palynology, 6, 119-147. Raynaud, J . F. and P. Robert, 1976. Optical methods of studying organic matter. Soc. Nat l . Pe t ro l . Aqui. Ctr . Res. B u l l e t i n , 10, 109-127. Richardson, J . B. and S. M. Rasul, 1978. Palynological evidence for the age and provenance of the Lower Old Red Sandstone from the Apley Barn Borehole, Witney, Oxfordshire. Proc. Geol. Assoc., 90, 27-42. Ro l le , F., 1985. Late Cretaceous-Tertiary sediments offshore central West Greenland: 1 ithostrat igraphy, sedimentary evolut ion, and petroleum potent i a l . Can. J . Earth S c i . , 22, 1001-1019. Scott, L. and S. K. Sr ivastava, 1984. Reworked Cretaceous palynomorphs in Late Quaternary deposits from central Colorado, U. S. A. Pollen et Spores, 26, 227-240. Singh, C , 1971. Lower Cretaceous microf loras of the Peace River area, northeastern A lberta. Res. Counci l , A lber ta , 28, 542 pp. Sr ivastava, S. K. 1969. Assorted angiosperm pollen from the Edmonton Formation (Maestr icht ian), A lberta, Canada. Can. J . Bot., 47, 975-989. 131 , 1972. Systematic description of some spores from the Edmonton Formation (Maestrichtian), Alberta, Canada. Palaeontographica Abt. B, 139, 1-46. . 1977. Microspores from the Fredericksburg Group (Albian) of the southern United States. Paleobiologie Cont inenta l , 6:2, 119 pp. Stanley, E. A., 1966. The problem of reworked pollen and spores in marine sediments. Marine Geology, 4, 397-408. Staplin, F., 1969. Sedimentary organic matter, organic metamorphism and o i l and gas occurrence. Can. Petrol. Geol. Bu l l . , 17, 47-66. Teichmuller, M. and B. Durand, 1983. Fluorescence microscopical rank studies on l ip t in i tes and v i t r in i tes in peat and coals, and com- parisons with results of the Rock-Eval pyrolysis. Int. J . Coal Geology, 2, 197-230. Tschudy, R. H. and R. A. Scott (eds.), 1965. Aspects of Palynology. New York: John Wiley & Sons, Inc., 193-269. Turner, R. E., 1982. Reworked acritarchs from the type section of the Ordovician Caradoc Series, Shropshire. Palaeontology, 25, 119-143. Umpleby, D. C , 1979. Geology of the Labrador Shelf. Geol. Surv. Can., Paper 79-13, 34 pp. Va i l , P. R., R. M. Mitchum, J r . and S. Thompson III, 1977. Seismic stratigraphy and global changes of sea level. Part 4: Global cycles of relative changes of sea level, in C. E. Payton (ed.), Seismic stratigraphy—applications to hydrocarbon exploration. Am. Assoc. Petrol. Geol., Memoir 26, 83-97. van G i j ze l , P., 1979. Manual of the techniques and some geological applications of fluorescence microscopy. Workshop sponsored by Am. Assoc. of Strat. Palynologists, Core Laboratories Inc., Dallas. Wilson, L. R., 1964. Recycling, stratigraphic leakage, and faulty techniques in palynology. Grana Palynologica, 5, 426-436. 132 EXPLANATION OF PLATES A l l specimens were recovered from offshore Tertiary sediments from the Labrador Sea. The photomicrographs were photographed in transmitted l ight under Nomarski d i f ferent ia l interference con- trast. Figure captions contain information of the wel l , sample depth and type of sample ( i . e . , cuttings or sidewall core) from which specimens were recovered. The magnification and photo num- ber ( i . e . , negative number, year and frame number) of the photomicrographs are also included. 133 PLATE 1 FIGURE 1: Wodehouseia spinata. Recycled Upper Cretaceous pollen re- covered from late Eocene strata. Karlsefni A-13; 7482 f t . (cuttings); lOOOx; KARL A:80:18. FIGURE 2: Aquilapollenites amplus. Recycled Upper Cretaceous pollen recovered from late Eocene strata. Cartier D-70; 4500 f t . (cuttings); 800x; CAR C:81:9. FIGURE 3: Balmeisporites sp. Recycled Upper Cretaceous spore recov- ered from middle-late Eocene strata. Cartier D-70; 4590-4600 f t . (cuttings); 800x; CAR C:81:10. FIGURE 4: Gleicheniidites senonicus. Recycled t r i l e t e spore assigned to Upper Cretaceous group of recyclants. Recovered from middle-late Paleocene strata. Kangamiut 1; 3447 m. (cuttings); 800x; KANG E:79:32. FIGURE 5: C i c a t r i c o s i s p o r i t e s cf. C. hughesii. Recycled Lower Cretaceous spore recovered from late Eocene strata. Kangamiut 1; 2700 m. (cuttings); 800x; KANG E:79:20. FIGURE 6: Eamulatisporites sp." Recycled Lower Cretaceous spore re- covered from late Paleocene strata. Kangamiut 1; 3099 m. (cuttings); 800x; KANG E:79:28. FIGURE 7: Podocarpidites biformis. Recycled Lower Cretaceous spore recovered from middle-late Paleocene strata. Kangamiut 1; 3447 m. (cuttings); 800x; KANG E:79:33. FIGURE 8: Leptolepidites cf. L. verrucatus. Recycled Lower Cretaceous spore recovered from late Paleocene strata. Kangamiut 1; 3099 m. (cuttings); 800x; KANG E:79:22. FIGURE 9: F l o r i n i t e s sp. Recycled Paleozoic (Carboniferous?) spore recovered from late Eocene strata. Herjolf M-92; 5400 f t . (cuttings); 800x; HERJ A:81:27. FIGURE 10: Densosporites cf. D. subtriangularis. Recycled Paleozoic (Carboniferous?) spore recovered from middle-late Paleocene strata. Kangamiut 1; 3201 m. (cuttings); 800x; KANG E:79:14. FIGURE 11: T r i q u i t r i t e s sp. Recycled Paleozoic (Carboniferous?) spore recovered from late Eocene/early Oligocene strata. Roberval K-92; 1870 m. (cuttings); lOOOx; ROB E:81:8. 134 FIGURE 12: Triquitrites sp. Recycled Paleozoic (Carboniferous?) spore recovered from late Eocene/early Oligocene strata. Roberval K-92; 1930 m. (cuttings); lOOOx; ROB E:81:2. 135 PLATE 1 I36 CHAPTER 4. PROVENANCE OF IN_SITU AND RECYCLED PALEOGENE PALYNOMORPHS OF THE LABRADOR SHELF INTRODUCTION The Paleogene continental shelf sediments of seven Labrador Sea wells were studied in detail for the purpose of relating the composition and relative abundances of recycled and in-s i tu Paleogene palynomorphs to their sediment source. The wells used in the study are: Kangamiut-1, from offshore Western Greenland; Hekja 0-71, from offshore southern Baffin Island; and Karlsefni A-13, Snorri J-90, Herjolf M-92', Roberval K-92 and Cartier D-70, from offshore Labrador. Their location is shown in Figure 1. This study is an outgrowth of a project, sponsored by Aquitaine of Canada (now Canterra), to determine the distribution of Cretaceous and older recycled palynomorphs in the shelf sediments of the Labrador Sea. During that study, a relat ively large number of recycled Paleogene palynomorphs were found in association with the other recyclants. In two of the wells (Hekja 0-71 and Roberval K-92), they actually dominate the total late Eocene palynomorph assemblage. A l - though a few dinoflagellates are represented, almost a l l of the Paleogene recyclants are pollen and spores. They are also very simi- lar in species composition to the in-s i tu or contemporaneous Tertiary pollen and spore assemblages recovered from the wells. 137 Figure 1. Location map of the Labrador Sea and the seven offshore wells used in this study. 138 The Paleocene and Eocene depositional history of the Labrador Sea was influenced by a major marine transgression that began in latest Cretaceous time and came to an end during the late Eocene. The shelf sediments are characterized by thick sequences of predominantly brown mudstones with s i l t y and sandy partings and rare, thin dolomitic limestone beds, which generally represent distal turbidites that were reworked downslope by turbidity currents (McWhae, 1981). Sediment ac- cumulation curves for the Labrador Sea (uncorrected for compaction) indicate that shelf sedimentation rates during this time period were in excess of 10 cm/1000 years (Gradstein and Srivastava, 1980). Kerogen analyses show that much of the sediment was te r res t r i a l l y de- rived (Bujak and Williams, 1977a and 1977b) and, in places, is charac- terized by a maximum organic carbon content of from 2-4 percent (Rashid et a l . , 1979). Foraminiferal assemblages also indicate bathyal to ner i t ic water depths throughout much of the Paleocene and Eocene with a shallowing towards the end of the Eocene (Gradstein and Berggren, 1981). With the onset of marine regression, l i t t l e or no deposition took place for much of the Oligocene and, perhaps, the early Miocene (Gradstein and Srivastava, 1980). Based primarily upon deep seismic reflection prof i les , McWhae and Michel (1975) and Cutt and Laving (1977) suggested that considerable d i f ferent ia l re l i e f existed over the Labrador and Newfoundland shelves 139 during late Cretaceous and early Paleogene time. Erosion of these topographic highs was suggested as the main source of the terrigenous sediments deposited into the subsiding offshore grabens. In contrast, McMillan (1973) proposed that, in addition to some input of sediments from local sources, large portions of the Tertiary marine sediments were derived from the erosion of outcrops in the southern Arct ic and central and western inter ior of Canada by a large "super r iver" system, which entered the Labrador Sea through what is now Hudson Stra i t . Hiscott (1984) also suggested an Arct ic and western Canadian source for the Paleogene sediments of the Labrador Sea, based upon the presence and abundance of a homogeneous, polycyclic suite of clay minerals. The palynofloral.. composition of the Paleogene contemporaneous and recycled pollen and spore assemblages from the Labrador Sea continental shelf sediments help support both McMillan's and Hiscott 's model of a distant source for much of the sediment de- livered to the Labrador Sea during the Early Tertiary. RECYCLED PALYNOMORPHS AS INDICATORS OF PROVENANCE Palynomorphs and other organic matter are an integral part of the sedimentary environment and are carried as part of the suspended sedimentary load along with inorganic clay and s i l t sized part ic les. As such, they can be very useful for helping to determine the 140 provenance of sediments. Stanley (1966) suggested that recycled pollen and spores and other organic matter in marine sediments could be used to help determine sediment source areas. Groot and other workers also made the'same observation based upon their investigation of Quaternary sediments in the Argentine Basin (Groot, 1966). Askin and E l l i o t (1982) examined recycled Permian and Triass ic palynomorphs in the Tertiary Seymour Island Group of the Antarctic Peninsula, and concluded that a non-marine, topographic high in the forearc terrain of the late Paleozoic-early Mesozoic Gondwana plate margin was the source of the sediment. The pattern of distr ibution of recycled Paleozoic, Late Cretaceous and Early Tertiary palynomorphs in surf ic ia l glacio-marine sediments of the Ross Sea, Antarctica, led Truswell and Drewry (1984) to suggest that separate inputs of ice into the Ross Sea came from West and East Antarctica. An abundance of recycled Tremadocian (Early Ordovician) acritarchs led Richardson and Rasul (1978) to recognize four different Paleozoic sediment source areas for the Lower Devonian Old Red Sandstone of southern England. Turner (1982) also used redeposited acritarchs to determine sediment source in the type Caradoc Series (Late Ordovician) in Shropshire, England, which was interpreted to have been derived from Tremadoc and Arenig/Llanvirn-aged sediments (Early Ordovician) from the Midland Platform. 141 Based upon the presence of recycled Jurassic and Lower Cretaceous palynomorphs, McLean (1968) proposed that the sediment source for the upper Paleocene Naheola Formation of Wilcox County, Alabama, was lo - cated in central Alabama. Multiple recycling events and a local Late Devonian source of sediment to Lower Cretaceous rocks of the Moose River Basin in Ontario were identi f ied by Legault and Norris (1982). Scott and Srivastava (1984) showed that the Upper Cretaceous Mancos Shale was-an important source of sediment to the Late Quaternary de- posits in the Alkal i Basin of central Colorado in the western inter ior of the United States. There are some problems associated with using contemporaneous and, part icular ly, recycled palynomorphs to determine sediment sources. For example, multiple recycling events can often obscure the primary source of the sediment. Also, sampling and the state of preservation of the organic matter can bias the sample and misrepresent palynomorph concentration. Furthermore, i t is often very d i f f i c u l t to identify as recycled, those palynomorphs that have been redeposited in sediments of nearly the same age. Many of the forms are long-ranging and are similar in color and morphology. By understanding these problems and making careful observations, however, i t is possible to recognize re- cycling trends that can be used to help determine the provenance of sediments. Relative abundances of the redeposited grains, especially in intervals where there is good stratigraphic control, can be deter- mined. Also, there are a number of methods that can be used in con- 142 junction with one another to help identify the recyclants (see CHAPTER 4). These include the taxonomic identi f icat ion of key diagnostic spe- cies with limited ranges, as well as the monitoring of color and stain acceptance characteristics of the grains. It is also useful to qual itat ively measure the dif ferent fluorescing properties of the palynomorphs. RESULTS The palynofloral composition and relat ive abundance of redeposited (as well as contemporaneous) Paleogene palynomorphs from the Labrador Sea were determined for the purpose of helping to- identify their l ike ly provenance. Sample depths and the Lower Tertiary sections from each of the seven study wells are i l lustrated in Figure 2. Lithostratigraphic nomenclature is based on the work by Umpleby (1979), McWhae et a l . (1980) and Rolle (1985), and the relat ive ages of the sediments are based on palynological work by this author. The relat ive abundances were determined by counting 300 palynomorphs ( in -s i tu and recycled) per sample. Only those palynomorphs that could be reasonably identif ied as recycled were counted as such. Other age groups ( i . e . , Late Cretaceous, Early Cretaceous-Late Jurassic and Paleozoic) of recycled palynomorphs found within the study wells, with the exception of Hekja 0-71, were also included in the counts (see CHAPTER 3). 143 DEPTH IN METERS -1000 KANGAMIUT 1 * ' HEKJA 0-71 ' 2 KARLSEFNI A-13* 3 SNORRI J-90 .4 HERJOLF M-92" ROBERVAL K-92 • UKm FM -4000 — to lUOSTOHE MBB, • = s 3 UPPER MOST LEIF SS LOWER MOST C A R T W R F M . L A B R A D O R ~ S H . HORIZONTAL BARS TO THE RIGHT OF EACH COLUMN REPRESENT SAMPLE LOCATIONS. •'STRATIGRAPHY AFTER ROLLE. 1985 ^STRATIGRAPHY AFTER KLOSE ET AL. 1982 "3STRATIGRAPHY AETER TOTAL-EASTCAN •'STRATIGRAPHY AFTER MCMILLAN Figure 2. Generalized l ithostratigraphic columns of the Tertiary sections of the seven study wells. The distr ibution and relat ive abundances of recyclants in each of the study wells for the middle to late Paleocene, early Eocene, late Eocene, and late Eocene-early Oligocene strata are i l lustrated in Fig- ure 3. Although Upper Cretaceous dinoflagellate and pollen and spores were found redeposited in the lower Paleocene samples, early Paleocene aged recycled grains could not be ident i f ied. A combination of fac- tors made them impossible to recognize. For example, the age d i f f e r - ence between the redeposited and in-s i tu material was too close to be able to distinguish them apart from one another. Also, the diversity of pollen and spores is generally low and, of those species present, many are f a i r l y long-ranging. During the middle to late Paleocene, the number of recognizable older Paleocene-aged recyclants is moderately low (Figure 3a), whereas Upper Cretaceous redeposited grains are a f a i r l y common component of the total number of recyclants. By early Eocene time, however, the number of Paleocene recyclants increases (Figure 3b), but the percentage of recycled Late Cretaceous palynomorphs remains approximately the same. Data on the relative abundance of recycled Paleocene palynomorphs for the northern part of the study area was not determined. The Paleocene interval in Hekja 0-71 was not studied because of the d i f f i cu l t y of determining rel iable range tops. In Kangamiut 1, i t was not possible to separate Paleocene assemblages into different populations. 145 Figure 3. Distribution of relat ive abundances of Paleogene recycled palynomorphs in the Paleogene sediments of the Labrador Sea. Key to numbers: 1 - Kangamiut 1; 2 - Hekja 0-71; 3 - Karlsefni A-13; 4 - Snorri J-90; 5 - Herjolf M-92; 6 - Roberval K-92; and 7 - Cartier D-70. Symbols represent the following relat ive abundances: - no data; • sparse; • uncommon; •common; A very common; and • abundant. 146 The Paleogene recyclants reach their greatest abundance in the late Eocene, where they are very common components of the overall palynomorph assemblage (Figure 3c). Similar abundances are found in the late Eocene/early Oligocene sediments from offshore Labrador and Southern Baffin Island. In the northeastern corner of the Labrador Sea basin off West Greenland, however, the number of Paleogene recyclants decreases s l ight ly (Figure 3d). The most common constituents found within the Paleogene group of recyclants appear to be middle to late Paleocene and early Eocene in age. They include the following species: Insulapollenites rugulatus, tlaceopolipollenites amplus, Momipites spp. Paraalnipollenites altemiporus, Pistillipollenites mcgregorii, Plicatopollenites sp. There are also large numbers of Paleocene tricolporate and tricolpate pollen with uneven staining characterist ics, that are especially com- mon in the late Eocene and late Eocene/early Oligocene strata. In Roberval K-92, interpreted Paleocene recyclants generally exhibited a more medium to darker orange color of fluorescence than did palynomorphs considered indigenous to the sediments. 147 There is a poss ib i l i ty that some of the Paleocene pollen and spores identi f ied as recycled represent mud contamination. One of the more common types of mud additives used in d r i l l i n g is a pol len-rich Paleocene l ignite from North Dakota. Interpretations of the Paleogene stratigraphy in some of the Beaufort Sea and offshore eastern Canada wells have been complicated by these d r i l l i n g mud contaminants (Bujak, personal communication). However, the physical appearance and species composition of the Paleocene pollen and spores (indigenous and rede- posited grains), as well as limited sidewall core control in Kangamiut 1, Karlsefni A-13 and Herjolf M-92 indicate that the majority were not introduced during d r i l l i n g . Furthermore, an inquiry made into the types of d r i l l i n g additives used in the offshore study wells suggested that Tertiary muds were not l ike ly used (McMillan, personal communi- cation). DISCUSSION In order to help account for the high rate of sedimentation and re- sulting thick sequences of predominantly Tertiary sediment found along the continental margins of the Labrador Sea, McMillan (1973) proposed the existence of a large river system that drained much of the Canadian inter ior during latest Cretaceous and Tertiary time. This 148 "super r iver" entered the Labrador Sea through the graben structure of what is now the Hudson Strait (see Figure 4). Included within i t s drainage basin were parts of the Northwest Terr i tor ies , Alberta, Saskatchewan, Manitoba and the northwestern edge of Quebec. Such great volumes of sediment were being deposited into the Labrador Sea, that in some places, sediment thickness exceeds 3 to 4 kilometers. The up l i f t and erosion of the Canadian Cordi l lera helped control the amount and type of sediment being discharged into this ancestral r iver system. McMillan also discusses the probable locations of other im- portant r iver systems in the region. One of these probably brought sediment to offshore Labrador through the the Stra it of Belle Isle, and another through the Churchill River drainage, which enters Lake Melvi l le at Goose Bay, Labrador. Along the west coast of Greenland (including Disko Island), the Tertiary sand and shale sequences were probably derived from the deposition of sediments carried by rivers draining the Greenland landmass. The almost complete absence of Cretaceous and Tertiary outcrops on ad- jacent land masses makes i t d i f f i c u l t to determine, however, i f the local palynoflora in the area was actually representative of that found in the offshore sediments. A number of studies have shown that pollen and spore assemblages found incorporated into marine sediments do tend to represent the regional f lora of the entire drainage basin of the r iver system responsible for transporting the grains offshore 149 Figure 4. Schematic diagram showing possible drainage patterns of r iver systems supplying sediments to the Labrador Sea during the Tertiary as proposed by McMillan, 1973. 150 (Muller, 1959; Koroneva, 1968 and 1971; Heusser and Florer, 1973; Heusser and Balsam, 1977). Therefore, i f McMillan's "super r iver" did exist, a s imi lar ity in palynofloral composition between western and inter ior Canada and the Canadian Arct ic and the Labrador Sea would be expected. A large number of pollen and spore species recovered from the Labrador Sea Paleogene sediments also have well documented occurrences in simi- lar ly aged sediments from a broad area encompassing parts of the Canadian Arct ic and western Canada. Shared components include Gothanipollis cockfieldensis, Momipites spp., Maceopolipollenites spp., Pistillipollenites mcgregorii, Parviprojectus sp., Boisduvalia clavatites, Jussiaea sp. and Insulapollenites rugulatus. Araliaceoipollenites, Cupuliferoipollenites, Rhoipites and Verrutricolporites pollen species and fungal spores (e.g., Fusiformisporites, Pesavis and Ctenosporites) are also common elements among the several regions. Although many of these palynomorphs have broad geographical ranges on the North American continent, some appear restr icted to the Canadian Arct ic and the western and inter ior regions of Canada and the United States. Parviprojectus is found in late Eocene to early Oligocene sediments from the Canadian Arct ic (Staplin, 1976, Rouse, 1977) and Br i t i sh Columbia (Rouse, 1977). Similar pollen is also reported from Alaska (Wiggins, personal communication). P i s t i l l i p o l l e n i t e s 151 mcgregorii is reported from late Paleocene to middle Eocene strata from Br i t i sh Columbia (Rouse et a l . , 1971; Rouse, 1977; Rouse and Mathews, 1979; Mathews and Rouse, 1984), the Canadian Arct ic (Staplin, 1976; Rouse, 1977; Ioannides and Mclntyre, 1980; Norris, 1986) and the northwestern United States (Newman, 1981; and Wingate, 1983). Insulapollenites rugulatus occurs in Paleocene sediments from the western inter ior of the United States (Leffingwel1, 1971) and Canada (Sweet, 1978; this author, unpublished technical report). Some of these elements are conspicuously absent from published palynological reports from immediately south of the Labrador Sea in the Grand Banks, the Scotian Shelf and the northeastern Atlantic coast of the United States (Williams and Brideaxix, 1975; Barss et a l . , 1979; Bebout, 1980). See CHAPTER 2 for a more detailed discussion of the geographic distribution of taxa. Although the contemporaneous Paleogene assemblages show greater diver- s i ty, the species composition of both the recycled and in-s i tu palynofloral assemblages is very similar. For example, key diagnostic pollen used to identify late Paleocene and early Eocene sediments, such as Pistillipollenites mcgregorii and Momipites coryloides, are found recycled in late Eocene and younger sediments. This homogeneity of composition suggests that the Paleogene recycled and contemporaneous pollen and spore floras were both derived from similar sources. 152 That a r iver system, such as the one proposed by McMillan, is capable of carrying great volumes of sediments, including palynomorphs and other organic debris, for such long distances and then depositing the material into offshore marine environments, is well documented. Muller (1959) examined the distr ibution of detr i ta l organic matter (e.g., pollen, spores, cut ic le and woody material) in the deltaic and shelf sediments of the Orinoco River in northeastern Venezuela. He found that the pollen and spore assemblages associated with these sediments were representative of the regional mountain and plains veg- etation growing within the r iver ' s drainage basin (an area of over 900,000 square kilometers). Recycled Cretaceous and Tertiary pollen and spores and tracheal fragments from the headwaters of the Orinoco in the Andean footh i l l s were also noted. His results show that swamp and marsh palynofacies of the Orinoco are characterized by local sources whereas the offshore and prodelta palynofacies are composed of mixed assemblages of not only marine but also ter res t r i a l l y derived contemporaneous and reworked organic matter. There is also a general overall decrease in the amount of land-derived organic matter with i n - creasing distance offshore. The hydrodynamic properties of the or- ganic debris as well as the marine currents are responsible for their di stribution. 153 Contemporaneous and recycled ter res t r i a l l y derived organic matter, i n - cluding pollen and spores, were also found in the Amazon submarine fan (Tissot and Pelet, 1981). The organic debris, representing the r i ver ' s vast drainage basin, was carried by the river and offshore currents out onto the continental shelf and slope. One of the best analogues of McMillan's proposed "super r i ver " , with regards to volume of sediment transported, is the Mississippi River, which has a large drainage basin than spans more than 3 mil l ion square kilometers. It deposits, on the average, 500,000,000 tons of sediments per year into the Gulf of Mexico. Its suspended sediment load includes a high percentage of contemporaneous and recycled or- ganic matter-(Hart, personal communication). In order to determine the effective distance of transport of certain pollen and spore types by water in deltaic environments, Piel (1965) examined the pollen and spore f lora in six shallow cores of Recent pond and marsh sediments from the Mississippi River Delta. His re- sults show not only a broad spectrum of contemporaneous pollen and spores representing the Miss iss ippi 's vast drainage basin, but also a re lat ively high percentage of Tertiary and Quaternary recycled arboreal pollen and bryophyte and fern spores deposited rather uni- formly in each of the six study cores. In addition, he found fa i r l y abundant occurrences of Aquilapollenites, which were probably derived from the erosion of Late Cretaceous sediments in the Rocky Mountain 154 western inter ior region of North America. Similar Campanian and Maastrichtian pollen (e.g., Aquilapollenites spp., Wodehouseia spinata and Balmeisporites sp.), with well documented occurrences in the Canadian western inter ior, were also found in the Labrador Sea T e r t i - ary sediments. The importance of the Mississippi River with regards to sediment d i s - tribution offshore is documented by Urban and Newport (1975), who re- port recycled Devonian through Tertiary aged palynomorphs in Recent sediments approximately 100 miles offshore in the Gulf of Mexico. The broad dispersal of f luv ia l sediments discharged into marine'waters is further demonstrated by the fact that the offshore portions of the modern Mississippi River form a sediment platform out into the Gulf of Mexico covering an area of approximately 700 square miles (Smith, 1978). In a study of palynomorph distr ibution in the Gulf of Cal ifornia (Cross et a l . , 1966; and Cross, 1975), i t was found that accumulations of pollen and spores and other land derived plant matter were d i s t r ib - uted in banded gradients near the mouths of the larger r ivers. The hydrodynamic properties of the different grains tends to cause them to be selectively concentrated in bands. In addition, recycled palynomorphs were associated with bottom sediments in the northern third of the Gulf. These redeposited grains were eroded from older 155 sediments by the ancestral Colorado River and discharged into the Gulf of Cal i fornia where they underwent later submarine reworking. Heusser and Balsam (1977), in their study of the distribution of pollen and spores in the Recent offshore sediments off the mouth of the Columbia River and off San Francisco Bay, conclude that f luv ia l transport is the predominant factor controll ing contemporaneous pollen influx in the northeastern Pacif ic Ocean. They found high concen- trations of pollen and spores from 50 to 100 kilometers offshore in water depths ranging from 50 to 3000 meters. In contrast, Mudie (1982) reports that wind transport is the major mechanism of dispersal of Recent pollen and spores in offshore eastern Canada. She found that f luv ia l transport is subordinate in this region where river run- off volumes are presently small and winds are predominantly offshore. Although wind transport can be an important factor in pollen and spore transport, the large number of recyclants mixed in with in situ assemblages suggests that the primary controll ing mechanism of trans- port was f1uvial. The aforementioned studies a l l emphasize the importance of marine cur- rents for distr ibuting sedimentary organic matter offshore. Although the paleocirculation of surface waters in the Labrador Sea from Campanian to early Oligocene time may have been poleward (Gradstein and Srivastava, 1980), i ts northward movement does not appear to have s ignif icant ly affected the distr ibution pattern of the recycled and 156 contemporaneous palynomorphs. In spite of minor differences in re la - t ive abundance, the composition and frequency of the two assemblages appear to be f a i r l y evenly distributed at any one time. Another factor controll ing the distr ibution of the organic matter is the movement and reworking downslope of the sediments by turbidity currents. The Cartwright Formation from offshore Labrador and the Nukik Formation from offshore West Greenland represent, for the most part, turbidite deposits. Recycled grains are a common constituent in turbidites, where they may represent multiple cyc l ic events (Whitman, 1985). Although the reworking by turbidity currents has undoubtedly affected the overall distr ibution as well as mixing of assemblages, a detailed examination of the palynomorphs indicates that the species composition of the palynoflora has not been overly biased. The mineralogical composition of the Cretaceous and early Paleocene continental shelf strata of the Labrador Sea was studied by Higgs (1977) for the purpose of determining the provenance of the sediments. Higgs examined the mineral and 1ithic fragments of 44 Cretaceous and early Paleocene sand samples from offshore Labrador and onshore West Greenland. Based on his findings, he concluded that the Cretaceous and early Paleocene sediments of the Labrador Sea were derived from local sources. Palynological results from these same intervals do not contradict this conclusion, because of the relat ively low percentage 157 of recycled palynomorphs and the low diversity and abundance of in-s i tu pollen and spores in the early Paleocene. Although Hiscott (1984) also supports a local source for Cretaceous and possibly early Paleocene Labrador Sea sediments, his detailed study of the clay mineralogy of both the Cretaceous and Tertiary sediments, from five offshore Labrador wells (including Roberval K-92) and Hekja 0-71 from offshore southern Baffin Island, indicates a Canadian Arctic-western North American source for a large portion of the Paleogene sediments. Data from other wells (including Karlsefni H-13, Snorri J-90 and Cartier D-70) were also incorporated into his results. He found that, although the pre-Tertiary marine shales were characterized by an abundance of local ly derived smectite, the Paleogene sediments were characterized by a predominately mixed smect i te- i l l i te -kao l in i te clay assemblage. The homogeneity of this polycyclic clay suite indicates a multiple source such as would be ex- pected from a large, intercontinental drainage basin encompassing thousands of square kilometers. In fact, the volume of the long-distance transported material was so great that i t diluted clays derived from local sources. 158 CONCLUSIONS 1. The s imi lar ity of Paleogene in-s i tu and recycled palynomorphs (primarily pollen and spores) between the shelf sediments of the Labrador Sea and the Canadian Arct ic and western interior of Canada indicate that a least a portion of the assemblages may have been transported from distant sources. The method of transport, as pro- posed by McMillan (1973), was probably via a "super r iver" system that drained much of the Canadian inter ior during the Tertiary. The re- sults of Hiscott 1 s (1984) clay mineralogical study supports this con- clusion. 2. A Canadian Arct ic and western inter ior sediment source to the Labrador Sea during the Tertiary has important implications regarding the interpretation of not only the sedimentology of the region but also the paleoclimatology. 159 REFERENCES Askin, R. A. and D. H. E l l i o t , 1982. Geologic implications of recycled Permian and Triass ic palynomorphs in Tertiary rocks of Seymour Island, Antarctic Peninsula. Geology, 10, 547-551. Barss, M. S., J . P. Bujak and G. L. Williams, 1979. Palynological zonation and correlation of sixty-seven wells, eastern Canada. Geol. Surv. Can., Paper, 78:24, 118 pp. Bebout, J . W., 1980. Observed stratigraphic distr ibution of spores, pollen and Incertae sedis palynomorphs in the Tertiary section of the Cost No. B-2 well, Baltimore Canyon, Atlantic outer cont i - nental shelf. Palynology, 4, 181-196. Bujak, J . P., M. S. Barss and G. L. Williams, 1977a. Offshore east Canada's organic type and color and hydrocarbon potential, Part I. Oil Gas J . , April 4, 198-202. , 1977b. Offshore East Canada's organic type and color and hydrocarbon potential, Part II. Oil Gas J . , Apri l 11, 96-100. Cross, A. T., 1975. Source and distr ibution of palynomorphs of the Gulf of Cal i fornia. Abstr., Geoscience and Man, 11, p. 156. Cross, A. T., G. G. Thompson and J . B. Zaitzeff, 1966. Source and distr ibution of palynomorphs in bottom sediments, southern part of Gulf of Cal i fornia. Marine Geology, 4, 467-524. Cutt, B. J . and J . G. Laving, 1977. Tectonic elements and geologic history of the South Labrador and Newfoundland continental shelf, Eastern Canada. Bul l . Can. Pet. Geol., 25:5, 1037-1058. Gradstein, F. M. and W. A. Berggren, 1981. Flysch-type agglutinated foraminifera and the Maestrichtian to Paleogene history of the Labrador and North Seas. Marine Micropaleontology, 6, 211-268. Gradstein, F. M. and S. P. Srivastava, 1980. Aspects of Cenozoic stratigraphy and paleoceanography of the Labrador Sea and Baffin Bay. Palaeogeogr., Palaeoclim., Palaeoecol., 30, 261-295. Groot, J . J . , 1966. Some observations on pollen grains in suspension in the estuary of the Delaware River. Marine Geology, 4, 409-416. 160 Heusser, C. J . and L. E. Florer, 1973. Correlation of marine and continental Quaternary pollen records from the northeast Pacif ic and western Washington. Quaternary Research 3, 661-670. Heusser, L. and W. L. Balsam, 1977. Pollen distr ibution in the Northeast Pacif ic Ocean. Quaternary Research, 7, 45-62. Higgs, R. Y., 1977. Provenance of Mesozoic and Cenozoic si 1 ic ic las t i c sediments of the Labrador and West Greenland continental margins. M. Sc. Thesis, U. of Calgary, Calgary A l ta . , 169 pp. Hiscott, R. N., 1984. Clay mineralogy and clay-mineral provenance of Cretaceous and Paleogene strata, Labrador and Baffin shelves. Bul l . Can. Petrol. Geol., 32:3, 272-280. Ioannides, N. S. and D. J . Mclntyre, 1980. A preliminary palynological study of the Caribou H i l l s outcrop section along the Mackenzie River, D i s t r i c t of Mackenzie, in Current Research, Part A, Geol. Survey of Canada, Paper 80-IA, 197-208. Koroneva, E. V., 1968. Distribution and rpreservation of pollen in sediments in the western part of the Pacif ic Ocean. Geological Bul let in, 2, 1-17. , 1971. Spores and pollen in Mediterranean bottom sediments. in B. M. Funnel and W. B. Reidel (eds.), The Micropaleontology of Oceans. University Press, Cambridge, 361-371. Leffingwell, H. A., 1971. Palynology of the Lance (Late Cretaceous) and Ft. Union (Paleocene) Formations of the type Lance area, Wyoming. Geol. Soc. Am., Spec. Paper 127, 1-64. Legault, J . A. and G. Norris, 1982. Palynological evidence for recycling of Upper Devonian into Lower Cretaceous of the Moose River Basin, James Bay Lowland, Ontario. Can. J . Earth Sc i . , 19, 1-7. Mathews, W. H. and G. E. Rouse, 1984. The Gang Ranch-Big Bar area, south-central Br i t i sh Columbia: stratigraphy, geochronology, and palynology of the Tertiary beds and their relationship to the Fraser Fault. Can. J . Earth Sc i . , 21, 1132-1144. McLean, D. M., 1968. Reworked palynomorphs in the Paleocene Naheola Formation of southwest Alabama. J . Paleontology, 42:6, 1478-1485. 161 McMillan, N. J . , 1973. Shelves of Labrador Sea and Baffin Bay, Canada, in R. 6. McCrossan (ed.), The Future Petroleum Provinces of Canada. Calgary, Alberta, Can. Soc. Petrol. Geol., Memoir 1, 473-517. McWhae, J . R. H., 1981. Structure and spreading history of the Northwestern Atlantic from the Scotian Shelf to Baffin Bay. in J . W. Kerr and A. J . Fergusson (eds.), Geology of the North Atlantic Borderlands. Can. Soc. Petrol. Geol., Memoir 7, 299-332. McWhae, J . R. H., R. E l ie , K. C. Laughton and P. R. Gunther, 1980. Stratigraphy and petroleum prospects of the Labrador shelf. Bul l . Can. Petrol. Geol., 28, 460-488. McWhae, J . R. H. and W. F. E. Michel, 1975. Stratigraphy of Bjarni H-81 and Leif M-48, Labrador Shelf. Bul l . Can. Petrol. Geol., 23, 361-382. Mudie, P. J . , 1982. Pollen distribution in Recent marine sediments, eastern Canada. Can. J . Earth Sc i . , 19, 729-747. Muller, J . , 1959. Palynology of Recent Orinoco delta and shelf sediments. Micropaleonto.logy, 5, 1-32. Newman, K. R., 1981. Palynologic biostratigraphy of some early Tertiary nonmarine formations in central and western Washington. Geol. Soc. Am., Spec. Paper 184, 49-65. Norris, G., 1986. Systematic and stratigraphic palynology of Eocene to Pliocene strata in the Imperial Nuktak C-22 well, Mackenzie Delta region, D is tr ict of Mackenzie, N.W.T. Geol. Sur. Can., Bul l . 340, 89 pp. P ie l , K. M., 1965. Palynology of some Recent sediments from the Mississippi Delta. M.Sc. Thesis: New Orleans, Tulane Univer- s ity, 74 pp. Rashid, M. A., L. P. Purcell and I. A. Hardy, 1979. Source rock potential for o i l and gas of the East Newfoundland and Labrador Shelf areas, in A. D. Mi al1 (ed.), Facts and Principles of the World's Petroleum Occurrence. Can. Soc. Petrol. Geol., Memoir 6, 589-608. Richardson, J . B. and S. M. Rasul, 1978. Palynological evidence for the age and provenance of the Lower Old Red Sandstone from the Apley Barn Borehole, Witney, Oxfordshire. Proc. Geol. Assoc., 90, 27-42. 162 Rouse, G. E., 1977. Paleogene palynomorph ranges in western and northern Canada. in W. C. Elsik (ed.), Contributions of stratigraphic palynology (with emphasis on North America), Vol. 1, Cenozoic palynology. Am. Assoc. Stratigraphic Palynologists Contr. Ser., 5A, 48-65. Rouse, G. E., W. S. Hopkins, J r . and K. M. P ie l , 1971. Palynology of some Late Cretaceous and Early Tertiary deposits in Br i t i sh Columbia and adjacent Alberta. Geol. Soc. Am., Spec. Paper 127, 213-246. Rouse, G. E. and W. H. Mathews, 1979. Tertiary geology and palynology of the Quesnel area, Br i t i sh Columbia. Bul l . Can. Petrol. Geol., 27, 418-445. Scott, L. and S. K. Srivastava, 1984. Reworked Cretaceous palynomorphs in Late Quaternary deposits from central Colorado, U. S. A. Pollen et Spores, 26, 227-240. Smith, G. A., 1978. Evaluation of palynomorph and maceral distr ibution in sedimentary environments of the modern Mississippi and St. Bernard deltas. M.Sc. Thesis, Baton Rouge, Louisiana State Univ., 53 pp. Stanley, E. A., 1966. The problem of reworked pollen and spores in marine sediments. Marine Geology, 4, 397-408. Staplin, F. L. (ed.), 1976. Tertiary biostratigraphy, Mackenzie Delta region, Canada. Bul l . Can. Petrol. Geol., 24:1, 117-136. Sweet, A. R., 1978. Palynology of the Ravenscrag and Frenchman Formations, in Coal Resources of Southern Saskatchewan: A Model for Evaluation Methodology. Geol. Surv. Can. Economic Geol. Re- port 30, 29-39. Tissot, B. and R. Pelet, 1981. Sources and fate of organic matter in ocean sediments. Oceanologica Acta, 97-103. Truswell, E. M. and D. J . Drewry, 1984. Distribution and provenance of recycled palynomorphs in surf ic ia l sediments of the Ross Sea, Antarctica. Marine Geology, 59, 187-214. Turner, R. E., 1982. Reworked acritarchs from the type section of the Ordovician Caradoc Series, Shropshire. Palaeontology, 25, 119-143. Umpleby, D. C , 1979. Geology of the Labrador Shelf. Geol. Surv. Can., Paper 79-13, 34 pp. 163 Urban, J . B. and R. L. Newport, 1975. Palynomorphs from sediments of the Flower Garden reef area of the Gulf of Mexico. Abst., Geoscience and Man, 11, p. 160. Whitman, J . , 1985. Turbidite sedimentation in the Mariana Basin and the Cenomanian-Turonian Boundary. Abst., Scripps Industrial Asso- ciates Seminar, May 1985. Williams, G. L. and W. W. Brideaux, 1975. Palynologic analyses of Upper Mesozoic and Cenozoic rocks of the Grand Banks, Atlantic continental margin. Bul l . Geol. Surv. Can., 236, 163 pp. Wingate, F. H., 1983. Palynology and age of the Elko Formation (Eocene) near Elko, Nevada. Palynology, 7, 93-132. 164 CHAPTER 5. PALEOGENE PALEOCLIMATIC TRENDS OF THE LABRADOR SEA REGION INTRODUCTION Pollen and spore assemblages recovered from six wells d r i l l ed along the continental shelves of the Labrador Sea (Figure 1) help support a large body of data indicating that warm temperatures were prevalent at high latitudes during the Paleogene. During parts of the Early T e r t i - ary, tropical to subtropical conditions extended into Arct ic and Antarctic latitudes (Rouse, 1977; Wolfe, 1978). Paleomagnetic studies and paleogeographic reconstructions indicate that paleopole positions in the Tertiary were not s ignif icant ly different from their present positions (Donn and Shaw, 1977). Although paleontological and isotope geochemical studies (including Rouse, 1977; Savin, 1977; Wolfe, 1978, 1980; Gradstein and Berggren, 1981) from around the world document a general decline in global temperatures since late Cretaceous times, there were several important temperature fluctuations superimposed on the overall cooling trend. Savin (1977) plotted oxygen isotopic paleotemperature data for North Pacif ic planktic and benthic foraminifera through the Cenozoic. The isotope data from the benthic foraminifera represents surface water temperatures at high latitudes where cool bottom waters are formed. 165 Figure 1 . Location map of the Labrador Sea and the six offshore wells used in this study. 166 The benthic isotopic paleotemperature curve shows a period of climatic cooling at the Cretaceous/Tertiary boundary and early Paleocene, which was followed by a warming phase that reached optimum conditions in the early Eocene. The middle and late Eocene saw gradual cooling until at the end of the Eocene and early Oligocene, there was a dra- matic decline in temperature. With the exception of several warming events in the late Oligocene and middle Miocene, there was a deter i - oration of climate through the Neogene and an increased development of lat itudinal temperature gradients. STUDY AREA Paleogene sediments were studied in wells from offshore West Greenland (Kangamiut 1), offshore southern Baffin Island (Hekja 0-71) and of f - shore Labrador (Karlsefni A-13; Herjolf M-92, Roberval K-92 and Cartier D-70). Their location is shown in Figure 1. The ages of the sediments are based upon work by this author and the 1ithostratigraphy for offshore Labrador is after McWhae et a l . (1980) and for offshore Greenland after Rolle (1985). The generalized 1ithostratigraphy of the Paleogene sections of each of the study wells is i l lustrated in Figure 2. Sample depths are indicated by horizontal l ines to the right of each column. 167 DEPTH IN METERS KANGAMIUT 1 * ' HEKJA 0-71 . 2 KARLSEFNI A-13 . 3 HERJOLF M-92* 3 - 3 0 0 0 NUKIK FH. AAAA/ 2 = ~ tn UJ tn UPPER MDST LEIF SS LOWER MDST CARTWR FU. LABRADOR SH. ROBERVAL K-92 . 3 CARTIER D-70* AGLER FM 15 IARKLAND FM AAA7V1 CARTIER SS, CARTWR. FM I. CARTIER' SS LEIF SS : X - T u j o LAB SH HORIZONTAL BARS TO THE RIGHT OF EACH COLUMN REPRESENT SAMPLE LOCATIONS. •'STRATIGRAPHY AFTER ROLLE. 1985 •'STRATIGRAPHY AFTER KLOSE ET AL.. 1982 ^STRATIGRAPHY AFTER TOTAL EASTCAN Figure 2. Generalized 1ithostratigraphic columns of the Tertiary sections of the six study wells. cn oo The Labrador Sea was formed by the breakup of Labrador and Greenland. Based upon dinoflagellate occurrences, the incursion of marine waters into the newly forming basin probably began during the early Senonian (Barss et a l . , 1979). The modern configuration of the Labrador Sea was established by the latest Eocene/earliest Oligocene with the ces- sation of sea-floor spreading just prior to Anomaly 13 time (Gradstein and Srivastava, 1980). During the Paleogene great volumes of sediment, which in places reach up to ten kilometers in thickness (McMillan, 1980 and 1982), were de- posited along the continental margins of the Labrador Sea. The sediments are characterized by thick sequences of shales, mudstones, si ltstones and sandstones. McWhae et a l . (1980) interpret the brown to gray shales and mudstones of the Carwright Formation to represent turbidite deposits. Based upon foraminiferal studies from six of f - shore Labrador wells (including Karlsefni A-13, Herjolf M-92 and Cartier D-70), Gradstein and Williams (1981) interpret both the Cartwright and Kenamu Formations (roughly equivalent to the Ikermiut and Kangamiut Formations, respectively, from offshore West Greenland) to have been deposited under bathyal to deep ner i t ic conditions. Max- imum transgression in the Labrador Sea occurred during the early Eocene (Gradstein and Srivastava, 1980). 169 RESULTS AND DISCUSSION The pollen and spores found in the marine sediments of the Labrador Sea represent allochthonous ter res t r i a l l y derived assemblages, which were selectively delivered offshore mainly by f luv ia l transport. A l - though wind transport of palynomorphs can be an important mechanism of delivery of contemporaneous pollen and spores into marine depositional basins, as demonstrated by Mudie (1980 and 1982) in Recent offshore eastern Canada, f luv ia l transport tends to be the major contributor of pollen and spores and other terrestr ia l organic matter in marine sediments of warmer climatic regions where f luv ia l sediments by-pass i n f i l l e d coastal basins or where rivers are extraordinarily large (Muller, 1959; Cross et a l . , 1966; Frederiksen, 1969; McAndrews and Powers, 1973; Heusser and Balsam, 1977). The clay mineralogy of Lower Tertiary Labrador Sea sediments is pre- dominantly characterized by a mixed smectite, i l l i t e and kaolinite assemblage which is interpreted by Hiscott (1984) to indicate long distance f luv ia l transport of the sediments into the Labrador Sea. In order to account for the great thicknesses of sediment, McMillan (1973) proposed the possible existence of several rivers that drained into the Tertiary Labrador Sea basin. One of these was a major r iver that drained much of the Canadian interior and southern Arct ic re- gions. The composition and distribution of in-s i tu and recycled Paleogene pollen and spores in the Labrador Sea are also compatible 170 with a Canadian trans-continental and Arct ic provenance (see CHAPTER 4). F luvia l ly transported grains tend to ref lect the general regional veg- etation represented in the drainage basins of the rivers carrying sediments to the sea (Muller, 1959; Cross et a l . , 1966; Balsam and Heusser, 1976). Therefore, the Labrador Sea pollen and spore assemblage is very l ike ly representative of the gross regional f lora of not only the general area surrounding the Labrador Sea but also much of the Canadian inter ior and parts of the Canadian Arct ic . The general geographic distr ibution of modern vegetation is climat- i ca l l y controlled. A knowledge of the regional vegetation, therefore, can be used to help interpret paleoclimatic trends, by determining the probable a f f i n i t i e s of foss i l palynomorphs to modern plants. It is often d i f f i c u l t , however, to relate foss i l pollen and spores to their modern antecedents. The further back in time the more d i f f i c u l t i t is to rel iably determine relationships. A number of workers have made comparisons between foss i l pollen and spores and Recent palynofloras (Frederiksen, 1969; Rouse, 1977). The most up to date treatment is by Frederiksen (1985) who discusses in some detail the botanical a f f i n - i t ie s between various foss i l and modern taxa in his review of the paleoecology of Early Tertiary pollen and spores. 171 Other problems associated with using foss i l pollen and spores in ma- rine sediments to interpret paleoclimates include 1) biased assemblages resulting from selective transport of palynomorphs, 2) types of samples used (e.g., cuttings or sidewall cores) and 3) stratigraphic spacing of samples through a section. The diversity and relat ive abundance of pollen and spore taxa in the Labrador Sea samples varies considerably from the lower Paleocene sediments where they are at their lowest, to the Eocene and early Oligocene where they are generally high. Another factor controll ing the overall composition and distr ibution of the palynomorphs is the effect of turbidity currents. In-situ and recycled te r res t r i a l l y de- rived palynomorphs and other organic matter in the Cartwright Forma- tion were carried and redeposited downslope, where they became mixed with marine assemblages. In addition, mostly cuttings samples were used in the study, thereby, introducing possible downhole contam- ination by cavings. Paleoecological interpretations are further ham- pered by the use of f a i r l y wide sampling intervals in Kangamiut 1, Karlsefni A-13, Herjolf M-92 and Cartier D-70. Because of these problems, therefore, i t is not possible to provide a detailed paleoecological analyses of the Labrador Sea Paleogene pollen and spore assemblages. However, i t is possible to identify some very broad, general cl imatic trends that existed in the Labrador Sea and 172 very l ike ly the Canadian inter ior and Arct ic regions during the Early Tertiary. Early to Middle Paleocene Early to middle Paleocene sections were studied in a l l the wells with the exception of Hekja 0-71. The pollen and spore assemblage recov- ered from this interval has a low diversity and is characterized by abundant bisaccate and taxodiaceous conifer pollen, as well as monolete and t r i l e t e fern spores. Triporate pollen of the Betulaceae-Myricaceae-Casuarinaceae complex and reticulate," scabrate and psi late tr icolpate pollen are also present but never abundant. Similar assemblages are also reported from Saskatchewan (Sweet, 1978), Alberta (Sweet, 1983; this author, unpublished technical report) and further to the south in the western inter ior of the United States (Leffingwell, 1971; Nichols et a l . , 1985). Rouse (1977), who reports the same type of assemblage from the Canadian Arct ic , interprets i t to be indicative of cool and probably wet climatic conditions. Early to middle Paleocene foraminifera assemblages from the Labrador Sea and West Greenland also indicate temperate climatic conditions (Gradstein and Srivastava, 1980). Schweitzer (1980) interprets a lower Paleocene coastal mixed conifer and broad-leaved deciduous megafloral assemblage from Spitsbergen to 173 represent a warm temperate environment with occasional l ight frosts, corresponding to the lowlands of southern China and Taiwan. Based upon physiognomic data and comparisons between foss i l and extant f loras, Wolfe (1980) considers the early Paleocene Spitsbergen megafloral assemblages, as well as those from West Greenland, Alaska and Siberia, to be indicative of a mesothermal climate with mean annual temper- atures of around 14-15°C. The evolution of terrestr ia l vertebrates from the Rocky Mountain west- ern inter ior of the United States indicates climatic cooling across the Cretaceous/Tertiary boundary. The transitional composition of en- vironmentally restr icted faunas corresponds to gradual changes in the physical environment as a result of declining continental paleotemperatures (Clemens, 1982). Frederiksen (1985) indicates that pteridophyte fern spores are found in a variety of climates today and that a fern-dominated assemblage does not necessarily have to indicate climatic deterioration so much as an ecologically disruptive event. One such event, as proposed by Alvarez and others (1977, 1980), invokes a catastrophic asteroid im- pact at the end of the Cretaceous. They base their theory on the presence of a geographically widespread, iridium enriched clay layer found at the Cretaceous/Tertiary boundary. The terminal Cretaceous mass extinction and climatic cooling events are interpreted by many (including Alvarez et a l . , 1980, 1984; Smit and Hertogen, 1980; Hsu, 174 1981; Smit, 1982; and Pollack et a l . , 1983) to have resulted from a major impact of an extraterrestr ia l body. Early Paleocene fern-dominated palynomorph assemblages have been re- ported from Colorado, New Mexico and Montana just above the anomalous iridium enriched clay layer. (Tschudy et a l . , 1984; Nichols et a l . , 1985). The dominance of fern spores gives way to an increase in angiosperm pollen approximately 15 centimeters above the clay layer. The composition of the new f lora is much different from that of the late Maastricht!'an. Other theories to explain the iridium anomaly at the Cretaceous/Tertiary boundary and the decline in global temperatures include excessive volcanism over a prolonged period of time, such as the Deccan traps in India (McLean, 1984; Off icer and Drake, 1985) and physio-chemical and paleocirculation changes in the world's oceans (Gartner and Keany, 1978; Tappan, 1982). Late Paleocene Continued climatic warming in the middle to late Paleocene is i nd i - cated by an increase in diversity and relative abundance of angiosperm pollen in a l l of the study wells. Tricolporate and juglandaceous pollen are important constituents of the assemblage. The Momipites complex (Juglandaceae family) is similar morphologically to the modern 175 genus Englehardtia which is now found in the wet tropical mountains and lowland forests of Southeast Asia (Frederiksen, 1985), Mexico and Central America (Leopold and MacGinitie, 1972). Climatic warming in the late Paleocene at high latitudes is also ind i - cated by foss i l leaf assemblages from Alaska, which are characterized by a dominance of broad-leaved evergreens including palms and cycads (Wolfe, 1971, 1980). Fol iar physiognomic characterist ics of the f lora suggest a mean annual temperature of 17° to 18° C (Wolfe, 1978). Early to Early-Middle Eocene Climatic warming reached its maximum during the early to early middle Eocene as evidenced by the high diversity and composition of the pollen and spore palynoflora from offshore Labrador and West Greenland. Similar palynological assemblages are reported from simi- lar ly aged sediments from Brit ish Columbia (Rouse, 1977; Rouse and Mathews, 1979; Mathews and Rouse, 1984) and the Canadian Arct ic (Staplin, 1976; Rouse, 1977; Norris, 1986). Many of the same palynological elements are also reported from more southerly locations in Washington State (Newman, 1981; Reiswig, 1983) and the western in - ter ior of the United States (Cushman, 1983; Newman, 1983; Wingate, 1983). 176 Three of the palynof1 oral constituents in the assemblage are inter- preted as c l imat ica l ly diagnostic. They are P i s t i l l i p o l l e n i t e s mcgregorii, Platycarya sp. and Rhoipites latus. Pistillipollenites, which makes i ts f i r s t stratigraphic appearance in the late Paleocene, has a widespread occurrence in the late Paleocene to early middle Eocene of North America and Europe (Frederiksen, 1985). According to Rouse (1977), i t has a probable a f f in i ty with the modern herbaceous family Boraginaceae. He compares i t to the modern genus Tournefortia, which is native to tropical Central America. Boulter and Hubbard (1982) also associate i t with the Eocene paratropical rain forests of southern Br i ta in. The early to middle Eocene Platycarya (Juglandaceae) is very similar in appearance to the extant genus Platycarya, which is now restr icted to the tropical evergreen broadleaved and mixed mesophytic forests of China and Japan (Frederiksen, 1985). Rhoipites latus resembles the modern genus Triumfetta which is a tropical member of the Ti l iaceae family (Rouse, 1977). Faunal assemblages along the Labrador and Newfoundland continental shelves show a maximum incursion of low-latitude planktic foraminifera in the early and middle Eocene. Gradstein and Srivastava (1980) use the occurrence of Morozovella, to indicate the northernmost l imit of Paleogene tropical waters in the Labrador Sea. The poleward extent of i t s geographic range was around 50°N. 177 Although early and middle Eocene foss i l leaf assemblages from northern Alaska and the Canadian Arct ic are not very well known, in middle Eocene assemblages from south Akaska they indicate boreo-tropical con- ditions with a mean annual temperature of around 22°C (Wolfe, 1980). Further south, Leopold and MacGinitie (1972) correlate early Eocene leaf and pollen assemblages from the Rocky Mountain western interior with the broad-leaved evergreen forest of Southeast Asia. Mammalian (including primates, rodents and a type of " f ly ing " lemur, Dermoptera) and rept i l ian (including turt les, l izards and an a l l i ga tor - l i ke species) foss i l evidence from the Eureka Sound Forma- tion on Ellesmere Island in the Canadian Arctic also indicate warmer climatic conditions during the early and middle Eocene (Dawson et a l . , 1976; West et a l . , 1975; Estes and Hutchison, 1980). Modern Dermoptera are currently restricted to Southeast Asia and al l igators are not found north of the Gulf Coast and North Africa (McKenna, 1980). An isolated oxygen isotope determination of a marine mollusc (scaphopod shell) from the Eureka Sound Formation indicates marine surface temperatures of 17°C (Donn, 1982). The Eureka Sound Formation foss i l sites are currently at latitude 79°N. McKenna (1980) calcu- lated the position of the Ellesmere Island sites in the early Eocene as approximately 77.5°N. 178 Late Eocene to Early Oligocene The late Eocene to early Oligocene Labrador Sea pollen and spore f lora is also characterized by a f a i r l y diverse and abundant assemblage. Triporate and tricolporate pollen predominate. Common elements i n - clude Liquidambar, Fagus, Corylus/Carpinus, Pterocarya and Quercus. Onagraceous pollen (e.g., Boisduvalia and Jussiaea) are also present. Similar pollen and spore assemblages are also reported from Br it i sh Columbia (Rouse, 1977; P ie l , 1977). Most of the above genera have broad geographic ranges today that ex- tend from subtropical to temperate climatic zones (Frederiksen, 1969). The modern distr ibution of Pterocarya is in the deciduous broad leaved forests of eastern China and Japan and in the Caucasus Mts. of eastern Europe (Leopold and MacGinitie, 1972). However, because Pterocarya has a well documented stratigraphic range extending from the late Paleocene to the Miocene in western Canada and parts of the Canadian Arct ic , i t is l ike ly that i t had a much broader climatic tolerance than i t does today. Nevertheless, an absence of the more tropical to paratropical genera Platycarya and P i s t i l l i p o l l e n i t e s suggests cooler temperatures. Physiognomic characteristics of leaf f loras from western Washington State indicate that by late Eocene times paratropical rainforests had given way to mixed mesophytic forests, representing as much as a 10° C 179 drop in mean annual temperature (Wolfe, 1978). Subtropical paleofloral elements had also disappeared from the Rocky Mountain re- gion by early Oligocene times (Leopold and MacGinitie, 1972). Along the Pacif ic coast of the United States, marine gastropods with warm-water a f f i n i t i e s preferential ly disappeared (Hickman, 1980). Climatic cooling during the latter part of the Eocene is also re- f lected by macrofloral assemblages from southern England (Collinson et a l . , 1981). Oxygen isotope studies from the sub-Antarctic (Kennett and Shackleton, 1976), the north Atlantic (Vergnaud-Grazzini et a l . , 1978), south Atlantic (Boersma and Shackleton, 1977) and the Pacif ic (Savin et a l . , 1975) a l l indicate a cooling trend that extended from middle Eocene to early Oligocene times. The most dramatic drop in isotopic paleotemperatures occurred at the Eocene/01igocene boundary. Kennett and Shackleton (1976) estimate as much as a 4 C drop in bottom water isotopic paleotemperatures in the sub-Antarctic over a period of 75,000 to 100,000 years. The pronounced Eocene/01igocene cooling event also coincides with the development of the psychrosphere. A quantitative analysis of planktic foraminiferal assemblages from six DSDP sites in the At lant ic, Pacif ic and Indian Oceans indicates that the sharp drop in temperature at the Eocene/01igocene boundary was marked by an increase in abundance of cool water species (Kel ler, 180 1983). The faunas also indicate that the cooling trend begem in the middle Eocene before the development of the psychrosphere. Labrador Sea foraminiferal faunas show a change near the Eocene/01igocene boundary from a predominance of agglutinated to calcareous forms. Although the change may be attributable to climatic or physical oceanographic changes, i t was certainly affected by the marine regression that also occurred at the same time (Gradstein and Berggren, 1981). CONCLUSIONS The Paleogene pollen and spore assemblages of the Labrador Sea ref lect the general climatic trends found at high latitudes during the Early Tertiary. These trends have been well documented by oxygen isotope paleotemperature analyses as well as by f lora l and faunal distr ibution patterns. During the early Paleocene, there was a period of climatic cooling followed by a general warming trend in the late Paleocene and early Eocene. The combined presence of the genera P i s t i l l i p o l l e n i t e s and Platycarya, in the early to early middle Eocene sections of the six study wells, indicate that maximum high latitude paleotemperatures for the Tertiary were reached at that time. The interpreted modern relatives of these two taxa are now restricted to tropical climatic zones. Late Eocene and early Oligocene Labrador Sea pollen and spores 181 are suggestive of a return to cooler climatic conditions. Oxygen isotope data indicate as much as a 4°C drop in high latitude surface water paleotemperatures near the Eocene/01igocene boundary. 182 REFERENCES Alvarez, L. W., W. Alvarez, F. Asaro and H. V. Michel, 1980. Extraterrestrial cause for the Cretaceous-Tertiary extinction. Science, 208, 1095-1108. Alvarez, W., M. A. Arthur, A. G., Fisher, W. Lowrie, G. Napoleone, I. Premoli Si lva and W. M. Roggenthen, 1977. Upper Cretaceous-Paleocene magnetic stratigraphy at Gubbio, Italy, V. 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SUMMARY The results of this dissertation are the product of a detailed palynological study of seven Labrador Sea wells (Kangamiut 1, Hekja 0-71, Karlsefni A-13, Herjolf M-92, Roberval K-92 and Cartier D-70) from 1978 to 1981. An eighth well, Snorri J-90, was cursori ly exam- ined for recycled palynomorphs. The i n i t i a l purpose of the study was to determine the relat ive abundance of redeposited Upper Jurassic/Lower Cretaceous recyclants, in order to establish i f whether or not reworked palynomorphs could be used to indicate the location of subsurface Jurassic rock units. From detailed examination of the f i r s t well, Kangamiut 1, i t became immediately apparent .that other groups of recyclants, including Paleozoic (Carboniferous?), Upper Cretaceous and Paleogene palynomorphs, were also present in the sam- ples. In addition to the recyclants, re lat ively abundant and diverse contemporaneous pollen and spore assemblages were found associated with the indigenous offshore f lora of dinoflagellates and other marine algae. In the upper Eocene and younger sections of the wells the ter - restr ia l palynomorphs were the dominant component of the overall palynological assemblage. As a result of these observations, i t was decided that a preliminary zonation for the Tertiary of the Labrador Sea based on pollen and spores be established. In addition, the relative abundance and d i s - tribution of the four different age-categories of recyclants through 189 time were determined. The composition of the palynological f lora and the recycling trends in the wells permitted several general observa- tions to be made regarding the provenance of the sediments of the Labrador Sea and the Paleogene paleoclimatology of the overall region. The results are br ief ly summarized below. Provisional Pollen and Spore Zonation of the Tertiary Sediments of the Labrador Sea The Tertiary pollen and spore assemblages from six Labrador Sea wells were used to establish eight preliminary biostratigraphic interval zones. Because cuttings samples were used almost exclusively in the study, zonal boundaries were defined by extinction events (range tops). Ages were assigned to the intervals based primarily upon the well-documented ranges of age-diagnostic dinoflagellate species found in association with the pollen and spore assemblages. The zonation represents a good biostratigraphic framework that can be used in con- junction with marine assemblages to characterize and correlate T e r t i - ary rock units in the Labrador Sea and perhaps other offshore locales in northern and western Canada. The Identification and Class i f icat ion of Redeposited Palynomorphs from the Labrador Sea Pre-Tertiary recycled palynomorphs recovered from the shelf sediments of the Labrador Sea were divided into three main categories: 190 Paleozoic (Carboniferous?), Upper Jurassic/Lower Cretaceous and Upper Cretaceous. Cr i ter ia used to identify the redeposited grains included taxonomy, color, stain acceptance, state of preservation and fluorescence intensity and color. The relative percentage of Paleozoic recyclants is generally very low, however, in Roberval K-92 they are very abundant in the Upper Cretaceous and upper Eocene to lower Oligocene sections of the well. The Upper Jurassic/Lower Cretaceous group of reworked palynomorphs is also characterized by f a i r l y low percentages. Although redeposited Upper Cretaceous grains are f a i r l y common in the uppermost Cretaceous and Tertiary sections of the study wells, they do not show any particular pattern of concen- tration when compared among wells. The recycled palynomorphs associ- ated with the Cretaceous sections of the wells were very l ike ly local ly derived, whereas a large percentage of the redeposited grains found in the Tertiary sections were probably delivered to the Labrador Sea from distant sources. Provenance of Paleogene Shelf Sediments of the Labrador Sea The recycled and contemporaneous pollen and spore assemblages recov- ered from the Paleogene shelf sediments of the Labrador Sea show a re- markable s imilar ity to assemblages reported from the Canadian Arctic and western inter ior of Canada. Due to the composition and relat ively high abundance of these grains, i t is suggested that they were de l iv - ered to the Labrador Sea over long distances via a large r iver system. It is well documented that pollen and spores can be f luv ia l l y trans- 191 ported for hundreds of miles from their source to their eventual site of depostion. The existence of a large r iver capable of such long-distance transport was proposed by McMillan (1973). The proposed r iver would have entered the Labrador Sea through what is now the Hudson Strait . A clay mineralogy study of the Labrador Sea sediments by Hiscott (1985) supports the palynological data by also suggesting a Canadian inter ior/Arct ic Canada sediment source. Paleogene Paleoclimatic Trends of the Labrador Sea Region Pollen and spore assemblages recovered from marine sediments are often good indicators of broad regional paleoclimatic trends. Based on this assumption, the Paleogene palynoflora of the Labrador Sea helps sup- port other paleofloral and faunal evidence that warm temperatures pre- vailed at high northern latitudes during the Lower Tertiary. Cl imatical ly diagnostic pollen indicates that the early Paleocene was characterized by a cooling period which gave way to an overall warming trend that persisted into the middle Eocene. Subtropical to tropical conditions are indicated at the peak of the trend in the early to early-middle Eocene. By late Eocene to early Oligocene time, there was a return to overall cooler climatic conditions. Though punctuated by several warming cycles, the cooling trend continued through the Tertiary and Pleistocene. 192 In conclusion, this study demonstrates the u t i l i t y of integrating both pollen/spore and dinoflagellate data in palynological studies of ma- rine sediments. The pollen and spores can provide valuable biostratigraphic input as well as important paleoecological informa- tion. The results from the examination of recyclants, on the other hand, have important implications with regards to geological and biostratigraphic interpretations. 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Stanford Univer- sity Press, Stanford Ca l i f . , 193-206. 209 APPENDIX 210 TERTIARY POLLEN FIND SPORE RANGE CHART: KANGAMIUT 1 WELL 2 G 0 0 2 7 0 0 2 7 5 0 2 9 0 1 2 9 4 9 3 0 0 3 3 0 9 9 3 2 0 1 3 2 9 7 3 3 9 9 3 4 4 7 3 5 0 7 3 5 4 9 3 G 0 0 3 6 4 2 3 6 5 4 3 6 9 0 C O Z D Z cn cr • C D Cu C C C C CU D Z 2= _J C O Q_ I D • UJ C C f— C O •—• C O C O tn ZD C D C C Z D LJJ Z I— z C O C C h- • < cr tr LJ ZD «—' Q_ Ou cn _j >- cc fr-ac LiJ CU co C C 0 Z D CJ or cr —̂ cr CU 2T 2Z • LO O •—• cc CD C O C C Z D CL. ~) Li-CJ 1 LU \ 0 cc: C O CD cr Cu o cr C O 0 CD a cn en D Z co U- 2: • C D cc Cu ID f—> cu 1 0 C O Q _ CJ CJ ZZ or cc t—• >H t-t Z D t—1 or cn tO Cu C O ce 1 CD CJ or cc LiJ CJ CJ cr cr 0 LJ cr >- > H cr Z D cn a: CJ CJ CJ CD U_ _ I az CU 0 O *** Pd C O L O C O C O CD m ZD *-> zz • CO cr CJ LO o_ z or CO cu Q_ LO COQ_ • CL. CL. CO o_ CO cr 0_ • CO cu O. CO to CJ to cc CL. D_ cn CO to to CL. CO CO LO CO LO Cu CO CC S3 • • CO UJ CO 1— LO (—• CL. LO CO S3 o_ CO fr- CO CO fr— CO DD UJ CO cu LO fr— CL. Q_ l - H to UJ z to f — «—1 CO •-—• z LO to * to • CO * 1—» UJ CO zz LO Z I LO LO LO zz LO to CO o_ 1 CO or to LO (-> ZD J » I—• _ J co CO a_ LO I LO I—« Q_ CU 1 LO CD f—< _ J •-̂  1 CL. —) O *—t 1 LO co 1 1 J— LO LJ CL. 0 i— Q_ t—t Q_ — J CL. L_ LU O CL. CH O • CO h-t _ J 0 CC CO • _ J CO Q_ •—• CO CL. Cu O • — i •—• to Cu LO 0 • CL. LO CO O 0- or CD OL. _ J •—• or LO 1—• CO CO CD CO CC o_ 0. CC 0- I—• z LO CU 0 Q_ D— CL. O cr O O er CJ « CO «—i CO ZD » CD CO D_ LO co •—1 LO h- 0 0 CL. CO fr-CO CU >- or CU _ j CO CO O cc CC ZD ZZ Q- ZD CD CO CJ Q_ 1 or or CO *—% CO ' — ' cc CO co 1 LO CO CO or 1—« o_ 1—1 a_ CO i—i (—1 sr t—t 1 O CD LO L J az Q_ O cr t—1 LO :> fr-0 O > or 0_ CO {—• cr cr Q_ ZJ DT O Q_ U_ cr CC CJ z ZZ CJ < (— O 1—< cc cc \ \ CD CD I— o_ CD 1 _ ) 0 f—' cc i—» CD 1 OZ >—i cc Q_ »—1 cc cc CD to CO cc 1—1 zz CC CD Z 0 CJ CD 1 1 L<_ CC 1 X or ZD z f—< - J >-> 0 ZD ZD CQ > ZD LO a CC ^£ or O ZD LO • CD CC UJ Q_ QZ —1 _ J CD cc 1 cn CD ZZ ZZ ZD LO Z I O X _ l 1 LO o_ CJ CO CJ ZD or: h-< ZD CC ZD 1—« zn cc *—( cr O •—t _ J CO cr CO •—1 cr O ZD or ZD ZD cn L_ o_ CD CD 3= fr-or cc t-t CJ CU CL. cc fr-* _ J CD i-t CC DZ CD CD CD Li- cn LO CO 1— CD CT) 0 OJ m LO CO r- CO cn O OJ CO LO CO CO en OJ OJ OJ OJ OJ OJ OJ OJ OJ OJ CO CO CO CO CO cn CO CO ro ro oc UI Li- t-» LJ UJ s: CD _j _i cc ai —1 i o CJ O C3 U. —• O - O . z= •—• •—• CO CD CD U l Ul U l O O —< CE CC U. * ^-t »—« ^ Q_ — I _ J CJ t—( cc <n « ^ ai cc a a . Q_ CO to CO tt. ui o a. E—• O CO CO »—1 tn RU S 0 DZ or • CO Cu CJ to CD UJ Cu CO to to CD or CU • to ZD z ZD CD to CO to CU zz co fr- or to or or CO Cu LO ZD ee to z ^ a_ CD • CD ZD • CO to UJ 1 fr-_ J fr- QZ to CO o_ X cu CJ fr- CO fr-to to —1 ZD CD _J to co CC CU az ee ZD t— CO ZD ZD z CD cc DZ LO LO ZD a_ • ca cn • CC 1 or • t—l to CD az ZD O CL. I-H > to Q Cu Z I CU CO cn ZD CD U- zz. • I—1 or to az or CO c r • co •-̂  o_ • or to CO cu CD CO to r—i UJ • O • CU 0 to CU •—« ZD CO LO f— ZD CD CO to z • • CL. cc • fr- CO CD to CO fr-CL. cc t—c CD 1 CO zz ZD CO CD LO • cn to fr- • >• 1 LO CL, Cu CU O, CO fr- CO zz CO fr-o_ fr-CO 1 to CO ZD z fr-1 or CU cc 3— CO ZD _J CL. a_ CO Cu ee LO CO to 1—I • LO LO z CD LO to Cu to 0 CO 1 zz _ J ZD 1—1 E—• • z CO U- cc or LO E—< _J to to to to 0 t—« LO LO or a. fr-ZD LO to t-— or >- fr-Cu LO _ J LO CU fr- • Cu LO CJ LU 0 l—' az O CO LO Q_ 1—1 J— • t— 0 CO •—• 1 —1 to DZ CO or «—• CD fr-0 CO 3Z 0 to Li- zz Cu 1 CO CD 1 . 1 Q_ CC CO LO I— CO —1 z •—1 CU t—1 Cu CC CD 1 fr-CJ CO to CD or or —1 cu "—f cc or 1 CD to co 1 to CO CO QZ or O »—t LO 1—t 1—< O LO O • to O to tr 0 tr O t—t 0 LO fr- 0 0 or t—t _l _ J 0 fr-LO LO z CO CD CO or CD I— •—• CD or CD — J CU >-> Q_ fr-Q_ CU 1 fr-t—1 CO CU o_ CD 0 QZ CO CO 0 CO 1 CO cu fr-fr-LO •_ to CD ZD CD t—1 0 t—1 1 z Q_ Z I CJ or 1— I—1 •—) CD t—1 CD LO _j t—1 o_ to >-* to to Q_ to CD LO 1—1 cu or E— *—> E—< o_ a CL. »—l LO o_ or CD 1—1 to ZD CC or tr CD to _ l rc CU 1—1 fr-0 or CO CJ or fr-fr-0 fr-cu fr-zz _l Q_ Cu f -k—1 CD — 1 to 1 CD CJ CO a_ or z CJ CD CJ O 1—- 0 fr-QZ —1 O •—1 0 fr-t—. cc CC or cc 1 0 —1 D_ CC Q_ 0 CO CD CC CC t ZD cc cc to CD cc Lk_ >-* t-t >• 1—1 z 1 CD CJ CU CC CC LO - J CJ cu cu CD cu _ J CU cc CJ CD CD co » - H t—« t—* CJ CC O t—« I— CD or CO ZD LO CC CO ( t-t CJ cc t-t QZ 1 CD az 1< or or or ZD 1 t—t CU ZD cc >-. CJ CD ZDZ I or O fr- I or or or CO to DZ Z I CO GC ZZ CO CO 1 O or CD (— t-» LO fr-to Z I az 0 CO az or 1 z O (—• or UJ or *—< >-« O LO >-« cr m CU 0 ZD _ J ZD to 1—f or cr 3Z UJ fr-to or 0 CD or =c zz. CD cc 0 or cn 3Z CO or 2C t-t —1 3C >• z CJ cc tn CO U_ CU Q_ CU CU cc CC f -—1 or fr-1—• to CO CU az az f -or 1—« az Cu CU f -fr-cc Q Z to 3Z CO Z D az L O L O L O CO CO LO LO L O to r * C O C D C O C D •-— OJ C O r* r*- p*-L O CD r - CO CD o co —• OJ C O U D C O C O C O C O C O C O C O x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X . X X X X X X X X X X X X X X X X X X X X x x x x x x X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X x x x x x x X X X X X X X X X X X X X X X X X x x x x x x x x x X X X X X X X X X X X X - - 2 6 0 0 Parviprojectus sp. A Zone - 2 7 0 0 - 2 7 5 0 Rhoipites latus Zone - 2 9 0 1 - 2 9 4 9 - 3 0 0 3 - 3 0 9 9 Pistillipollenites mcgregorii Zone X X X X X X X X X X X X X X X X X X X X X X X X X X - 3 2 0 1 - 3 2 9 7 - 3 3 9 9 Tricolpites sp. A Zone X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X •X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X - 3 4 4 7 - 3 5 0 7 - 3 5 4 9 - 3 6 0 0 - 3 6 4 2 - 3 6 5 4 - 3 6 9 0 Paraalnipollenites alterniporus Zone SORTED BY DESCENDING RANGE TOP. 211 tnocnocoo-JOcnrjtDtn t / l t n t n m c n m o t n t n o o o • —I CO in o t n o m t n o t n o t n o ut • cn in cn #- u> TO t\j o ID tn 10 o cn - j o o tn tn cn o i— tn CO o —i o CD >-c o n cn o n ID CD n o •a x x x x x x x x x - X X X X X X X X XXX XXX X X X X XXX XXX X X X X XXX X X X X X X X X X X XX X X XXX X X X X X X X X X X X X X XXX X XXX X X X X X X X X XXX XX X X X X X X X X X X X X X X X X X X X XX XX X XXX X X X X XX X X X X X X X X X X X X XXX X XXX X X X X X X X X X X XX XX X X X X X X X X X X X X X X X X X XXX X X X X X X X X X X X X X X X X X X X X X X X X X XXX X X X X X X X X X X X X X X X X X X XXX X X X X X X X X X XXX X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X XXX X X X X X X X X X X X X X X XX XX XX X X X X X X XX XXX X XX X X XX XXX X X X X X X X X X X X X X X X X X XXX XXX X X X X X X X X X X X X X X X X X X X X X X XX XX X X X X X XX XX X X X X X X X XX X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X XXX X X X X X X X XXX XXX X X -X X XXX X I 1 I I I X X X XX XXX X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X XXX x x X X X X X X X X X X XXX XXX XXX XXX X X X X X X X X X X X X X X XX X X X X X X X X X X X X X X XXX X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X 4-1- X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X X 4-4- r t 1 COMPOSURE SP. 2 CHENOPQOIPOLLIS SPP. 3 GRAMINEAE SPP. 4 TSUGA IGNICULUS 5 BETULA CLAR1PITES 6 QUERCUS FORM 8 7 ABIES SPP. 8 PINUS/P1NUSP0LLENITES SPP. 9 ALNUS SPP. 10 LAEVIGATOSPORITES SPP. 11 OSMUNDfi SPP. 12 PICEA/P1CERP0LLENITES SPP. 13 SflL1XPOLLENITES SPP. 14 TILIfl SP. A is TSUSR v iR in i r iuMNiPnes 16 ACER SP. 17 MYRICA 5P. R 18 PSEUOOTSUCn 9P. 19 JUQLRN5 SP. B 20 LflRACOlOITES SPP. 21 SPHRSNUM SP. 22 FAGUS GRANULATA 23 LIOUIDAMBAR TORtl B 24 OUERCUS FORM A 25 LIOUIDAMBAR FORM A 26 SC1AT0P1TYS SPP. 27 FRGUS. CF. F. GRANULATA 28 CORYLUS/CARPINUS SPP. 29 ILEX SPP. 30 METRSEDU01A SPP. 31 ULMUS SPP. 32 CAPRIF0L11P1TES SPP. 33 CARTA VIRID1FLUMIPITES 34 PTEROCARYR SPP. 35 TAX0D1UM SPP. 36 TILIR CRRSSIPITES 37 NUPHUR? SP. 38 CYRILLACEAEPOLLENITES SP. 39 ER1C1P1TES FORM B 40 ERIC1P1TES FORM R 41 METASEOUOIfl SPP. 42 CEDRUS SP. 43 JUSIREA SP. 44 PARVIPROJECTUS SP. A 45 PfJirPOOllSPORITES SP. 46 CUPRESSACEOUS SPP. 47 FRAX1NUS SP. 48 ONAGRACEOUS SP. 49 TRICOLPAIE SP. (VERRUCATE) 50 TSUGR/TSUGREP0LLEN1TE5 SPP. 51 PER1P0RRTE SP. 52 PC-DOCARPUS SPP. 53 JUGLRNS SPP. 54 NYSSAP0LLEN1TES SPP. 55 DIERVILLfi ECHINRTA 56 LYC0P0D1UM VENUSTUM 57 LILIACI01TES SPP. 58 MOMIPITES VENTIFLUM1NIS 59 TRIC0LP0R0P0LLEN1TES SCABRATUS 60 MYRICA SPP. 61 P0LLEN1TES PSEUD0LAESU5 62 ACANTHACERE ' 63 0RQSERR SP. 64 ROUSEfl M0N1LIFERA 65 ROUSEfl RRRNEOSfl 66 BOlSDUVRLlft CLAVIT1TES 67 EPHREDRR CF. E. CLRRICR15IATA 68 SIGM0P0LLIS SP. 69 CYRILLACEREPOLLENITES SPP. 70 T0ROISP0R1S SPP. 71 ARALIACEOIPOLLENITES PROFUNDUS 72 CUPUL1FERO1P0LLEN1TES SPP. 73 VERRUTRICOLPORITES SPP. 74 ARALIACEOIPOLLENITES GRANULRTUS 75 MYRIC1P1TE5 SPP. 76 R0USEA SP. 77 RRRLIACE0IP0LLENITES SPP. 78 MILF0RD1R? SP. 79 VERRUTRICOLPORITES CRUCJRIUS 80 TETRRCOLPORITES CF. T. BREVIS 1 ARALIACEOIPOLLENITES MEGAPORIFER 82 TILIfl VESCIPITES 83 TRIC0LP0R0P0LLENITES CF. 1. KRUSCHII 4 TRICOLPOROP0LLENITES SPP. 85 VERRUTRICOLPORITES SP. C 86 ARALIACEOIPOLLENITES SP. fl 87 CASSIA SPP. TETRRCOLPORITES BREVIS 89 TRIP0ROP0LLENITES SPP. 90 SYMPLOCOIPOLLENITES SP. A 91 TETRRCELLRESPORITES SPP. 92 ARALIACEOIPOLLENITES M1CR0P0RIFER 93 TETRAC0LP0R1IES SPP. 94 TRICOLPITES SP. C (SENSU HNS < BR 19751 95 PSILATRICOLP0RITES SP. Z ISENSU HMS I BR1 96 STRIRD1P0RI7ES SPP. 97 VERRUTRICOLPORITES SP. B VERRUTRICOLPORITES SP. A 99 MOMIPITES HICR0F0VE0LATUS 100 AILANTH1P1TES SP. B 101 MULT ICELLAESP0RITES SPP. 102 FRAX1N01POLLENITES SPP. 103 0UERC0ID1TE3 SPP. 104 CUPUL1FER01P0LLENITES SP. B 105 L0NICERA SP. 106 HORNIELLA SPP. 107 MOMIPITES C0RTLOIDES 108 RHOIPITES LATUS 109 RHOIPITES SPP. 110 MOMIPITES SPP. U l PESAVIS PRRVUS 112 SYMPLOCOIPOLLENITES SP. B 113 AILANTHIPIIES SP. 114 PESRVIS TRGLUENSIS 115 CRPRIFOLIIPITES SP. A 116 FUSIFORMISPORITES SPP. 117 MTRTACE1DIIES PARVUS 118 FUSIFORMISPORITES SP. A (SENSU ROUSE 19771 119 H0LK0P0LLENITES SP. fl (SENSU ROUSE 19771 120 TRICOLPOROPOLLEMTES KRUSCHII 121 DICELLAESPORITES SPP. 122 GRANAT1SPOR1TES SP. 129 CAPRIFOLIIPUCS INELEBANTUS 124 GOTHflNlPOLLENITES SP. 125 GOTHflNlPOLL]S C0CKF1EL0EMSIS 126 SYMPLOCOS SP. fl 127 SYMPLOCOS SP. B 128 TRICOLPITES SPP. 129 VERRUTRICOLPORITES SP. 0 130 CUPULIFERO1P0LLENITES SP. C 131 TETRRCOLPORITES SP. A 132 TRICOLPITES SP. XX (SENSU HMS 4 BR 19751 133 PLATYCARYA SP. 134 RHOIPITES RNGUSTUS 135 AILANTHIPIIES SP. A 136 PUNCTOOIPORITES SP. 137 B0HBACAC1DITES B0MBAX010ES 138 CTENOSPORITES WOLFE I 139 SYMPLOCOS SPP. 140 INTRATR1P0R0P0LLENITES SPP. 141 AZ0LLA GL0CHIDIR 142 CASUAR1NID1TE5 SP. 143 CASUARIN101TES SPP. 144 PISTILLIPOLLENITES MCGREGORII 145 SAGENOPOLLIS RRANEOSA 146 TRICOLPITES SP. ZA (SENSU HMS i BR 19751 147 CUPULIFEROIOEIPOLLENITES SPP. 148 SILTAR1A SPP. n ID ~v a n ID -z. • CO "0 o 3D n ID z n r j ID o i - ^ i n tnotnotiiôjtocorototn tninmtncni/i. OLncnooo 5' lOCDtt̂ ĵ Jcooicn oo>o~J»-»cmo cnowaiotnDcn © <» " 3 o ft- a "i 3 o 3} S-0 0 5' 3 * a <* tn Ln Ln tt Cl <» a •5' o im 5" o 3 3 tt a ui 3 •8 o LO ru u • tn to o co o cn tn tn "6 tt 13' IM O 3 a -n «i «s c IM £ c ST c N » §1" / TERTIARY POLLEN AND SPORE RANGE CHART: KARLSEFNI fl-13 WELL tn 0. in tn o "* *& U =3 i n 3 13 X 1 1 fc ac cj m tv « i n n i n 1 y S _» tn tc O U l EE a CJ o tn X 3 ui a *- CB X CC tn X tc _ i tc i n IB >H J 3 3 0:: CD X •— O - l 3 D —< CE ac: x — y c j K 4 3 Q_ O LJ 3 5 m c J J u> CJ . J LT u c m r _j K u i eg u . M u. 8: -j X tc 0- Q CS V x x tn 3 > U ^ X u> u o> o ~ »— CJ : » 3 O O ~ X (_'[>. U L M C et O fid — _ J J- b>* i> LJ X CC CC cc n o_ o L - x tn CJ _ i CJ cn H 3 O Ul -J U _ 0 _ tc OL CL, CL _J O tn C l x •— cn *-> 1; • tn • 1 i in H fc. gig" CL. - 5i C t ft* Ul _J — D K SE B- _* tn D »s — c tn _ J Ui ft. —" U) 1— — E g E g 1 i I £ x cn u i _ J C3 UJ _ J _ J _J — tc tc b. — x a D_ L_ ~~ a o _» •-> M O _l 3 CJ U 3 in & X Ul — ut x « • LJ CD LJ £ t r m a> CJ S * o 1 .1 s S" . S i t • z co i— t» tn — tft - j u i a . » t ^ t - > D : i / i __j U l »— CE M Ul Ul D h I C D l l L l i . h Ul — IS D_ _J 2 m "* u • in in h I I I ! Ul U L U x tn x Q.t-il->U'->EJ>->'-< o n _ x > - > - 5 _ ( Q . Id — XI— X CJ 3 — _JX.JXtn — tl-O Z K t E B _ C > . > - > U K _l _J a M U 1— •~ tn C L) « J J C U J 1 ID d: LI D JC Ul O cc to m ca «n _ J r> •~> Ul cu • " = SI I c? i c 5 g 8s X i-t ™ m o CJ o tn u> t- I— oc „ — - _J o cc X o o . X 6. DC _ J m r J U l i e s £ x a . Ul • o J L g § S - a; Of S . «* B- H 3 3 Ol ti - i i n M _i x i n 5 S iri e u t " • « a 3 x X 2 l-i O W X a . x of j » t : - I £ i i J D. U Lt 3 — 1 3 — X 1- i— in ui in x ui tn in ID r* ID • rn i t * i n to o i o — rv. m CD cn o * Bl ID P- O Dl D T y r ^ * l P U l i n U l L I l U l U l u 1 1 f l L n i O C I l L D CD S3 S CD CO CO H, 8* t n u ce m S | X X d Si X u. Ul U tt d UJ t j £ X CL. _J 3 U i-> x n . tn x o 3 x u x tc — r* CD CD D Dj • - . x x x x x x x x x x x x x x x x x Fagus granulata Zone xxxx xxxxxxxxx : XXX XXRXXXX X XX xxxxxxx XX X X xxxxx x x x x x x x x x x x x x x XX x x x x x x x x x x x x x X X X X X X X XX XXXX XX XX XX X -6720 -6005 -7020 -7144 Araliaceoipollenites megaporifer Zone 7416 X X X X X X XXXX X X X X X -7416 7462 XXX X XXX X XXX X X X X X XXX -74B2 7972 XXXXXX XXX X xxxxxxx X X X X X X XXX X -7972 B20D XX X XXX X xxxxx X X X X -8200 Rhoipites latus B40S X X XXX X X XXXX X X X X -8406 Zone B490 XXXX X XXX X XX XXX X X X X X X X -8490 BEOS XXXX XXX X XXXX X X X X X XXX X X X -8600 B700 X X X X X X XX X X X X -8700 B7BI 8B00 X X X X X X X X X X X X X XXXX -B7B1 -8B0D B900 X X X X -B800 9000 XXX X X —9DDD 9080 X X X X XXX -S0BO 9100 9200 X X X X X X X X X -9100 -9200 9406 X X X X X X -9406 3613 X X X -9613 9752 X X X X X X -9752 9780 9834 9950 X X X X X X X X X X X X X X X -97B0 -9834 -9950 Pistillipollenites mcgregorii Zone 10175 X X X X X X X X -10179 10238 X X X X X -L0238 10342 X X X X X -10342 1040S X X XX X X X X X XX X -10408 10472 X X -10472 10SOO XXX X X X X X X X X X X X X X X X XXXX XXXXXX X X -J0500 1072E XXX X X X X X X X X X XXX X X X -10726 ID760 XXX X X X X X X X X X X X X XXX X X X XXXX -10760 10903 X X X X X X XXXXX -10909 11143 X X X X X X X X -11143 11243 X X X -11243 11464 XXX X X X . X X X X X X X XX XXX X -11454 Tricolpites sp. A Zone 11653 X X X X -11653 11762 X X X X X X X -11762 11952 X X X X X -11S52 12460 X X X X X -124ED 12640 X X X X X X X X X X X X -12640 12850 12950 X X X X X X X X X X -12850 -12950 Paraalnipollenites altemiporus 13140 X X X X X X X X -13140 Zone 13250 X X X -13250 13350 X X X X X -13350 13460 t > X X 1 1 X 1 1 . -J- I > 1 1 X X -13460 SORTED BY DESCENDING RANGE TOP. 213 4> C o N a w n a u .9. 0* 8 Kl 4) 0) C c o e M o .0. o « u <a 2 8 a o cc o o a o a o Q O O O O O -W- 0 J" 4> 8> «> 01 4) C * o C N o o o o o 0 O O O O O O O O o o o o o o o o o o o o r * o c o r ^ o o o o — cvim^ci»LO(Dr*r-cn L O L n L O U l t D i O l O U l t D l D C D C O l O t a I I I I I I I I I I 1 I 1 I 01 c o N a w in 41 .g. 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B . H i L c a o : i L i n H a n . o u u i L z i - — c- = n z z u E o _ i D c i c e c : c c £ c » D S 3 D C £ E u i l j ' e j > - — 0 3 0 0 3 — c c s CH U Ml 3 ^ — CC Ml — u. JE B: C3 BC UJ IE JZJI — V* H ZJ (C CU — CC CC K K _^ ̂ 3 2 m ££ — E — n S FS w ( E K U I C e C f l C I - . l / l e u l - ' J i — " C U Z — C C O O II K K •-• 3 ^ J U O OC BC fc O CC L Z £ U QC U VI iii J 1— — C l/l E CC O —• — —J —• —1 Ml CU — O Z O — —• — Z •—• •—• —• Ul — bC Z — Ml O t 1" BC BC Z I E C O I M I J 3 t C C U - I C I I U | M U - J U C B K U . C 3 _ l — U — U M l C u f t » t L u U 1 3 ^ 1 t j c ^ 1̂  CU CC CI O CC CC >» ™̂ U U CB IE CJI ZC 1— Cu CE OC Cu CJI IE I - 1̂  CU Z UJ C3 ^ E C3 •— CC E l Z SC Ul Ml ^ Lu Ul OC 1— 1̂  BO S. Ml L L _J #™ CC •— CU CJ 1— C3 CU BC 1— 1— Kl fr* IM IU U JE CU — JJ3 CD IE CU CC X X X  X X X X X  X X X X X X X X X x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x X X  x x x x x x -709 -710 Tsuga igniculus -750 Zone -760 -780 790 — BIO - B30 - BOO — 860 - 1 0 1 0 - 1 1 0 0 - IZOO - 1300 - XX  X X X X X X  X X X  X X X X X X X X X X X X X X X X X X X X X X X X X x x x x x x x x x x x x x x x x x x x x x x x x x x x X X X X X X  X X X X X  X X  x x x x x x x x x x x x x x x x x x X X X X X X X  X X  XX  X  X X  X X X  X X X  X X X X X X X  X X X  X X  X X  x x x x x x X X X X  X X  X X  X X X X  X X X -7S0 -810 -830 -900 -suo Fagus granulata -loio Zone - 1 1 0 0 - 1 2 0 0 -1300 1420 - 1450 - 1470 - 1500 - 1600 - 1650 - 1700 - 17S0 - 1 B 0 0 — X X X X X X X X X X X  X X X X X X X X X  X X X X X X X  X X X X X  X X  XX X X  X  X X X  X X X  X X X X X  X X  .X X  X  X X X X X X X X X X X X XX X  X X X X  X X X X  X X  X X X X X  X  x x x x x x x x x X X X X X X X X  X X X X x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x X X X X X  XX X X X  X  -1420 -1450 -1470 -1500 -1600 „ . _ -i6so Parvipro/ectus sp. A Zone -170D -1750 — 1BDD 1 B 1 0 - 1B30 - x x x x x X X X X X X x x x x x x x x x x x x x x x X X X X X x x x x x x x x x - 1 8 1 0 Araliaceoipollenites megaporifer - 1 8 3 ° Zone 1B50 - 1 B 0 0 - 19S0 - 2 0 0 0 — 2050 — x x x x x x x x x x x x x x x x x x x x x x x ! x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x x i _ X X X X XX X X X X X X X X X X X X X X X X XX x!x x x x x x x XX X X x x x x x x x x x x x x x x x x x x x x x x x x x X X X X X X X X X X X X X X X X X X X X X X X X X -1850 -1900 -mo Rhoipites latus - 2 0 0 0 Zone -20S0 2100 - 2140 - 2 2 0 0 - 2 2 2 0 - 2250 - 2300 - 2340 - XXXX X X X X X X X X X X X X X X x x x x x x x x x x x x x x x * X X * . X X X X X X X X X X X X X X X X X X X X X x x x x x x x x x X X X X X X X X X X X X X X X X X X X x x x X X X X X X X X X X X X X X X X X X X X X X XX X X x . x x X X X X X X X X X X X X X X X X X X X X x x x x . X X X X X XXXX XX X X X X X X X X X X X X X X X X X X X X X X XXX X XX X X X X X X x x x -2100 -2140 - 2 2 0 0 . - 2 2 2 0 Pistillipollenites mcgregorii -2250 Zone -2300 -2340 2370 — 2410 - 2460 — 2510 - ZS60 - 2600 - 2650 - X X X X x X X X X X X X X X X X X x x x X X x x x x x x x x x x x x x x x x X X X X X X X X X x x X X X X X X X X X X x x X X x x x x x x x x x x X X X X X X X X X X x x X X X X X X X X -2370 -2410 -2460 _ 3 S I D Tricolpites sp. A Zone -2560 -2600 -2650 2890 — 2750 - 2800 - x x x x x x X X XXXXX x x X X X X XXXX • • I , , . * . . * . . . XX X X X X X ' ' — 1 1 >—. ; 1 — 1 1 1 1 1 1 >̂  1 1 1 i >̂  1 1 J 1̂ -2750 Paraalnipollenites alterniporus -JBIJI-I Zone S O R T E D BY D E S C E N D I N G RANGE T O P . 215 cn tn » co to co tn tn tn tn tn ~j cn tn A . » r\> o o co o o o <=> o o co tn o to o o CO O ^3 n • CO >-< o rn co o n GO PO zn zz. CD m o 1 1 1 1 1 1 1 1 1 1 1 X 1 CORYLUS/CflRPINUS SPP. X 2 VERRUTRICOLPORITES SP. fl X X X 3 ABIES SPP. X X 4 RRflL IFICE01 POLLEN ] TES GRRNULATUS - X X 5 FRRXIN0IP0LLENITES SPP. X X 6 ILEX SPP. X X 7 MOMIPITES MICROF0VE0LRTUS X X X 8 STEREISPORITES SP. X X X 9 ARALIACEOIPOLLENITES MEGAPORIFER - X X X 10 JUGLRNS SPP. X X X 11 LYCOPOOIUM VENUSTUM X X X X 12 CRPRIFOLIIPITES SPP. X X X X 13 CUPULIFER0IP0LLENITES SP. C X X X X X 14 ERICIPITES FORM R - X X X X 15 NYSSRPOLLENITES SPP. X X X X 16 PTER0CRRYR SPP. X X X X 17 SCIRTOPITYS SPP. X X X X 18 ULMUS SPP. X X X X 19 VERRUTRICOLPORITES SPP. - X X X X 20 MULTICELLRESPORITES SPP. X X X X X X X 21 RRRLIflCEOIPOLLENlTES SPP. X X X X X X X 22 CRRYR VIRIDIFLUM1PITES X X X X X X 23 RHOIPITES LRTUS X X X X X 24 RHOIPITES SPP. - X X X X X X X X 25 TILIA CRRSSIP1TES X X X X X X X X 26 TILIfl VESCIPITES X X X X X X X X 27 0SMUN0R SPP. X X X X X X X 28 PODOCARPUS SPP, X X X X X X X X X X 29 LREVIGRTOSPORITES SPP. -X X X X X X X X X X 30 P1CEA/PICEAP0LLENITES SPP. X X X X X X X X X X X 31 TRX00IUM SPP. X X 32 HOLK0POLLENITES SP. fl (SENSU ROUSE 1977) X X 33 PUNCT0DIPORITES SP. X X X 34 TETRRC0LP0RITES BREVIS - X X X X 35 CUPULIFER01P0LLENITES SP. B X X X X X X 36 MOMIPITES C0RYL0IDES X X X X 37 TRICOLP0ROP0LLENITES SPP. X 38 RHOIPITES SP. B X 39 STRIRDIPORITES SPP. - X X 40 LONICERfl SP. X X 41 ISUGR/TSUGREPOLLENITES SPP. X X X X 42 TR1C0LP0R0P0LLEN1TES KRUSCH11 X X 43 LRRfiCOIDITES SPP. X 44 METflSEOUOIR SPP. - X X X 45 PINUS/PINUSPOLLENITES SPP. X X X 46 PLRTYCfiRYA SP. X X X X X 47 RLNUS SPP. X X X X X 48 PISTILLIPOLLENITES MCGREGORII X - 49 RHOIPITES ANGUSTUS - X 50 TOROISPORIS SPP. X X 51 PESAVIS TRGLUENSIS X X 52 AILANTHIPITES SP. fl X X X X 53 TRICOLPITES SPP. X 54 CRSUflRINIDITES SP. - X 55 INSULAPOLLENITES RUGULRTUS X 56 MOMIPITES ROTUNOUS X 57 TRIPOROPOLLENITES MULLENSIS X X 58 PRE-CflRYR (SENSU ROUSE) X 59 BETULflCEOIPOLLENITES SPP. X X 60 PARAALNIPOLLENITES ALTERNIPORUS -6130 -5860 -5810 -5720 -5600 L-5500 r-5480 h-sioo —  4800 i-4590 -4500 cu £. 3" •3' a N a o a- 2 "> n tn a o O •§"_ «••' tt to cn •O > IM O 3 a o S" M a o 5/ 3 n CB <* 3 n <o o 33 a-o ° re *> n TO • — * ZD TO -< -o o n z ZD ZZ. o C O ~0 O TO n TO ZD Z tn n o rc ZD TO o ZD PO >-H I—f n TO C3 I o ac n

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