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MichiganStatc University This is to certify that the thesis entitled RALYNOLOGY OF THE LOWER CRETACEOUS BEAR RIVER FORMATION IN THE OVERTHRUST BELT 0F SOUTHWE STERN WYOMING presented by John Craig Tingey has been accepted towards fulfillment of the requirements for Ph '1) - degree in 990108)’ Wfflww Major professor September 21. 1978 Date OVERDUE FINES ARE 25¢ PER DAY _ PER ITEM Return to book drop to remove this checkout from your record. PALYNOLOGY OF THE LOWER CRETACEOUS BEAR RIVER FORMATION IN THE OVERTHRUST BELT OF SOUTHWESTERN WYOMING BY John Craig Tingey A DISSERTATION Submitted to Michigan State University in partial fulfillment of the requirements for the degree of DOCTOR OF PHILOSOPHY Department of Geology 1978 ABSTRACT EALYNOLOGY OF THE LOWER CRETACEOUS BEAR RIVER FORMATION IN THE OVERTHRUST BELT OF SOUTHWESTERN WYOMING BY John Craig Tingey Rock samples from two sections of the Bear River Formation and one section of the Smiths Formation (both Lower Cretaceous) in the Overthrust Belt of southwestern Wyoming were studied for their acid insoluble plant microfossil content. The palynomorphs were isolated using conventional chemical and physical techniques in the laboratory. 113 distinct taxa were differentiated and systematically treated. Tabulation of the stratigraphic ranges of the previously reported taxa indicates a middle (?) to late Albian age for the Bear River Formation and Smiths Formation. A four part subdivision of the Bear River Formation is suggested from comparison of lithology, relative abundance counts of palynomorphs and terrestrial and marine percentages. These coincide with transgressive and regressive periods. The Bear River Formation in southwestern Wyoming was apparently deposited in a pronounced embayment of the Cretaceous seaway which contained marine or at least brackish waters during most of Bear River time. Local freshwater environments have also been indicated by other studies treating charOphytes, ostracods and John Craig Tingey molluscs. The overall palynofloral assemblage suggests a sub- tropical to warm temperate climate existed in southwestern Wyoming during middle (?) to late Albian time. ACKNOWLEDGMENTS The author gratefully acknowledges the direction and help of Dr. A. T. Cross of the Department of Geology and the Department of Botany and Plant Pathology, Michigan State University who served as chairman of the doctoral committee and provided guidance during all phases of this dissertation. Appreciation is also extended to Drs. R. L. Anstey, J. H. Fisher and C. E. Prouty of the Department of Geology and Dr. R. E. Taggart of the Department of Botany and Plant Pathology who served on the doctoral committee. The generosity of Chevron U.S.A., Inc. and particularly H. L. Ott in securing the description, measurements and samples from the Stowe Creek section and financial support for this study was greatly appreciated. This study was also supported by grants from the Michigan State University Chapter of Sigma Xi, the American Association of Petroleum Geologists and Union Oil Company through the Geological Society of.America. Lastly, I wish to acknowledge the patience and encouragement of my family and particularly my wife, Anne, without whose support the completion of this dissertation would not have been possible. 11 TABLE OF CONTENTS Page LIST OF TABLES..... ........................................... v LIST OF FIGURES ............................. .. ................ vi INTRODUCTION.. .............. . ........................... . ..... 1 Objectives of the Study ...... . .............. . ............ 1 Previous Studies ...... . .............. . ................... 1 GEOLOGY ........................ . .............................. 3 Regional and Structural Setting .......................... 3 Stratigraphy.................... ..... ...... ....... ....... 7 General Remarks ............. . ....... ........... ..... 7 Gannett Group............ ......... .................. 8 Bear River Formation........ ...... ....... ........... 10 Aspen Shale......................... ................ 12 Time Equivalent Strata in Adjacent Areas... ........ . 13 Paleogeography. .................................. ........ 14 DATA COLLECTION ............................................... l9 Localities ...................... . ........................ 19 Sample Collecting. .. . .............................. 21 Preparation of Samples and Slide Making. ............ . 22 Counting Procedure ....... ....... ......................... 24 SYSTEMATICS ............................................. . ..... 26 Introduction ............................................. 26 Trilete Spores..... ................... . .................. 29 Monolete Spores .......................................... 53 Spores-Incertae Sedis .................................... 53 Gymnosperm Pollen ........................................ 54 Angiosperm Pollen ........................................ 65 Monosulcate ..................... . .................. . 65 Tricolpate .......................................... 66 Tricolporate ........................................ 71 Incertae Sedis ...... . ............................... 71 Class DinOphyceae..... ................................... 72 Family Apteodiniaceae ............................... 72 iii Page Family Ctenidodiniaceae ............................... 73 Family Spiniferitaceae ................................ 73 Family Pareodiniaceae ......... . ....................... 74 Family Deflandreaceae... .............................. 75 Family Palanperidiniaceae ............................ 77 Family Hexagoniferaceae ............................... 77 Family Pseudoceratiaceae .............................. 78 Family Muderongiaceae ........ . ........................ 80 Family Membranilarnaciaceae ........................... 82 Family HystrichOSphaeridiaceae ........................ 82 Family Cleistosphaeridiaceae.. ........................ 84 Family Areoligeraceae ................................. 84 Group Acritarcha. . ......... .. .......................... 85 Subgroup Acanthomorphitae ............................. 85 Subgroup Polygonomorphitae ............................ 89 Subgroup Netromorphitae ............................... 89 SubgrOup Pteromorphitae ............................... 90 Incertae Sedis......... ............................. .. 9o ANALYSIS OF DATA ....... ... ...................... ...... .......... 92 Age of the Bear River Formation. ... ................ 92 Comparison with Other Palynofloras of Comparable Age ..... .. 94 Paleoenvironments of Deposition. .... ..... ...... ......... 97 Introduction .................. . ....................... 97 Comparison of the Stowe Creek and Fontenelle Creek Sections ..... . ............................... . ..... 100 Zone I ........................................... 100 Zone II .......................................... 102 Zone III ......................................... 105 Zone IV ..... . ............ ... ................. ....106 Smiths Formation Type Section ......................... 106 Paleoclimate and Paleoecology of the Bear River Formation..107 Zonation of the Bear River Formation ......... . ........... ..lll CONCLUSIONS ..................................................... 113 BIBLIOGRAPHY .................................................... 115 APPENDICES. ..................................................... 132 Appendix A - Taxonomic Listing ............................. 132 Appendix B - Stratigraphic Sections ....... . ................ 139 Appendix B-l - Stowe Creek Section .................. ..139 Appendix B-2 - Fontenelle Creek Section ............... 140 Appendix B-3 - Smiths Formation Type Section .......... 141 Appendix C - Sample Information ..... . ......... . ......... ...142 PLATES .......................................................... 148 iv Table LIST OF TABLES Page Stratigraphic occurrences as previously reported for some of the plant microfossils found in the Bear River Formation and Smiths Formation ........ ...... ..... 93 Comparison of Bear River and Smiths Formation taxa with those of similar studies in other areas of North America ......... ............................... ........ 9S Compilation of data from relative abundance counts for the Bear River Formation and Smiths Formation.....pocket Climatic distribution of probable counterparts of plant families identified in the Bear River Formation and Smiths Formation ....... ......... ................... 108 LIST OF FIGURES Figure Page 1 Index map of southern Overthrust Belt ................ 5 2 Palinspastic iSOpach and generalized facies map of the Bear River Formation .................... . ........ S 3 Stratigraphic nomenclature and probable equivalency of Lower Cretaceous strata in western Wyoming......... 9 4 East-west structural cross section near the Stowe creek sectionOOOOOOOOOOOOOO0.0000000000000000000000000 9 5 East-west structural cross section near the Fontenelle Creek section .................................... ..... 9 6 Zonation of the Bear River Formation at the Stowe Creek and Fontenelle Creek sections ......... ..........101 vi INTRODUCTION Objectives of the Study: 1) 2) 3) 4) Identify the terrestrial and marine palynomorphs of the Bear River Formation in southwestern Wyoming. Evaluate the plant microfossil assemblage in terms of age and comparison with other similar palynofloras in western North America. Interpret the probable environments of deposition of sampled sections using relative abundances of environmentally significant plant groups, terrestrially-derived/marine ratios, diversity of plant groups and correlation of occurrences to rock type. Make time correlations of the sampled sections, where possible, based on Species ranges and relative abundances. Previous Studies: Significant Lower Cretaceous and Cenomanian palynofloras have been studied in northern Wyoming (Davis, 1963, unpublished thesis), the Denver Basin of Colorado and Nebraska (Pannella, 1966, unpublished thesis), the southern Black Hills in northwestern South Dakota (Cahoon, 1964, unpublished thesis), Minnesota (Cenomanian; Pierce, 1961), southern Oklahoma (Cenomanian; Hedlund, 1966; Hedlund and Norris, 1968; Srivastava, 1975), south— western Mississippi and northeastern Louisiana (partly Cenomanian; Phillips and Felix, 1971a, b), southwestern Arkansas (Bond, 1972) 1 2 and north-central California (Warren, 1967, unpublished thesis). The western Canadian Lower Cretaceous has also been studied in east-central Alberta (Singh, 1964), central Alberta (Norris, 1967; Brideaux, 1971), northwestern Alberta (Singh, 1971), northeastern Alberta (Vagvolgyi and Hills, 1969), southern Alberta and southern Saskatchewan (Pocock, 1962, 1964), southern Saskatchewan (Steeves and Wilkins, 1967), eastern Saskatchewan and western Manitoba (Playford, 1971), the District of Mackenzie (Brideaux and McIntyre, 1975; Brideaux, 1977), the District of Franklin (Hopkins, 1971; Hopkins and Balkwill, 1973) and the Canadian Arctic Archipelago (Hapkins, 1974). Numerous studies of Lower Cretaceous palynomorphs and their stratigraphic significance in sediments of the Atlantic Coastal Plain have been carried out in recent years (Wolfe and Pakiser, 1971; Robbins and others, 1975; Doyle and Robbins, 1977) since the earlier work of Groot and Penny (1960), Groot, Penny and Groot (1961) and Brenner (1963). GEOLOGY Regional and Structural Setting; Since the first reconnaissance work in the Overthrust Belt of southwestern Wyoming by the Hayden and King surveys (1867 to 1879), a basic understanding of the structural relations has often dictated the nature of geologic interpretations. This is particularly true of the early stratigraphic placement and age determinations of the Bear River Formation. Significant studies dealing at least in part with structural complexities of the southern Overthrust Belt have been published by Veatch (1907), Schultz (1914), Mansfield (1927), Rubey and Hubbert (1959), Eardley (1960), Armstrong and Cressman (1963), Armstrong and Oriel (1965), Armstrong (1968), Oriel (1969), Rubey and others (1975) and Royse and others (1975). Armstrong and Oriel's paper is perhaps the most important contribution to an understanding of the tectonic development of the Idaho4Wyoming thrust belt, including the area where the Bear River Formation was deposited. Another particularly pertinent paper in dealing with "structural geometry and related stratigraphic problems" is Royse and others (1975). The Overthrust Belt occupies an eastwardly convex belt about 50 to 65 miles wide and 200 miles long. It extends north-south in the area southeast of the Snake River Plain, west of the Green River Basin and southward a short distance into northern Utah. The northern limit is the Teton Range where the thrusts trend 3 4 northwest-southeast as Opposed to the principal trend which is a few degrees east of north as far south as Kemmerer and Evanston. Armstrong and Oriel (1965) characterize the tectonic development of the thrust belt of southwestern Idaho and western Wyoming by three deve10pmental stages: (1) Thick sedimentary accumulation in Paleozoic miogeosynclinal and shelf environments (50,000 to 6000 feet thicknesses, respectively) with sources to the east and west. Eastern sources would include the stable craton whose contact with the miogeosynclinal shelf fluctuated considerably but generally centered in west-central Wyoming during the Paleozoic. Intermittantly elevated local areas and broad features on the craton such as the Transcontinental Arch and the Ancestral Rockies also contributed sediments to the miogeosyncline. Source areas to the west would include numerous volcanic "islands" dotting the western part of the eugeosyncline in a north-south belt and the Antler orogenic belt which became a positive area beginning in the Late Devonian. Additional thick basinal accumulations (35,000 feet in the west and 15,000 feet in the east) of marine and increasingly more terrestrial sediments continued through the Mesozoic as the result of an eastward spreading western positive area rising in the central Idaho region in Late Triassic as the miogeosyncline began to break up. By Late Jurassic time intracratonic geosynclinal basins had formed east of these highlands. (2) Crustal instability progressing eastward during latest Jurassic (in the west) to early Eocene (in the east) manifested by an area of folds overturned to the east and gently westward dipping thrust faults forming an arcuate outline convex to the east. (see Figure 1) Amnmfi ..Hm um mmzom so...“ kuwmuvwmv newumEuom uo>flm ummm wzu mo awe mwfiomw vmmwamumcow mam com OmH owummmmcfiamm N opzwfim Amoafi .waho can wcouumEu< mam whoa ..Hm um ammom wouwm mpouosuuwv ufimm amounuuo>o succuSOm mo amE xwocH H shaman 0330...: 080m mean 6 $32 .0599! $.95 0:102 035:0 395 fi ream 5:2 0.0::an l B: a team .23: I3 V- \ ‘ OUV]¥M V\ d .3}: 95» h... :3...— auoaaoz h: :32: 1.0.!O.U ..U :32» caocuaa< .—< .Ex_ov Om On _0— _ .mi On on o— o .35 oroco_oU 9.2.32 5:90» .5 032m mUm :o:uom .5 2.2.2.5”. 2953 ..U 0900 6.. comeuom 0&3. .Eu .EEm mtm mum mu.— 6 (3) North and east trending block faulting beginning in Eocene and continuing recurrently to the present. Armstrong and Oriel discuss eight major low angle reverse (thrust) faults and associated folding which, from Late Jurassic to middle Eocene time, shortened to roughly half, the original width of the westward thickening wedge of Paleozoic and Mesozoic miogeosynclinal sediments. Royse and others (1975) show, that except for broad warping, the crystalline basement is unaffected by the structurally detached sedimentary cover. The fact that younger strata are represented on the upper plate of each successively eastward thrust fault has been pointed out by Armstrong and Oriel as evidence that thrusting started in the west and progressed eastward. They also note the unusual lack of metamorphism and major fault breccia or mylonite associated with the thrust faults. Stratigraphic displacement is on the order of 5000 to 20,000 feet placing Paleozoic rocks in contact with progressively younger Upper Mesozoic and Cenozoic rocks eastward. Horizontal displacement along the major thrusts has been estimated at 10 to 15 miles by Armstrong and Oriel (1965) and to more than twice that amount by others. Royse and others (1975) discuss the importance of palinspastic isoPach and generalized facies maps in creating meaningful stratigraphic interpretations in an area such as the Overthrust Belt where stratigraphic units have been shortened laterally by thrusting. Such maps which show the original isOpach and facies pattern at the time of deposition also help to interpret the influence of uplifted and thrusted blocks on sediment source and on facies 7 detemminations. Their reconstruction of the Bear River Formation which is based on data from 110 control points (36 surface sections and 74 boreholes) is represented in Figure 2. The approximate pre-thrust (small asterisk) and present location (large asterisk) of the stratigraphic sections used in this study is plotted. In his treatment of the "Sevier orogenic belt" in Nevada and Utah, R. L. Armstrong (1968) states that "the Sevier belt is a continuous entity from Nevada to Idaho; structural style, age of deformation, magnitude of shortening, and width of the highly deformed zone show no radical changes over a distance exceeding 500 miles." He included the Idaho-Wyoming thrust belt in his newly named orogenic belt but failed to carry his investigation much beyond northern Utah. Except for the earliest thrusting in southern Idaho (Paris thrust) which probably began in latest Jurassic (Armstrong and Cressman, 1963), Armstrong's newly prOposed Sevier orogeny could be applicable to the deformation in the Idaho-Wyoming thrust belt which from earliest Cretaceous to Campanian supplied sediments to the Rocky Mountain geosyncline. Armstrong insists on the term Sevier orogeny in order to emphasize the distinction in position and timing with the earlier "classic" Nevadan orogeny and later Laramide orogeny which have sometimes been vaguely defined. Stratigraphy General Remarks: Although this study concentrates on the strata of the Bear River Formation, a brief review of Lower Cretaceous stratigraphy of southwestern Wyoming is necessary in understanding what has been called the classic "Bear River problem" which is 8 discussed later. A correlation chart of the units to be discussed is presented in Figure 3. Gannett Group: The Gannett Group (maximum thickness about 32,000 feet) was named from the Gannett Hills in Caribou County, Idaho and Lincoln County, Wyoming by Mansfield and Roundy (1916) who divided it into five distinct formations on the basis of its characteristic lithology in western Wyoming and southeastern Idaho: (1) Ephraim Conglomerate - primarily coarse conglomerates of alluvial- fan origin intercalated with fluvial channel fills of finer grained sediments (Eyer, 1969), (2) Peterson Limestone - primarily ostracod and charophyte rich, lacustrine limestones with some interbedded calcareous shale, (3) Bechler Conglomerate - similar in lithology to the Ephraim Conglomerate, (4) Draney Limestone - similar in lithology to the Peterson Limestone, and (5) Tygee "sandstone". The name was originally applied to a 100 feet thick "gray to buff, even grained sandstone" overlying the Draney Limestone at its type locality in Caribou County, Idaho. Since its original description the Tygee "sandstone" and the overlying black shale have been placed at the base of the overlying Bear River Formation (Cobban and Reeside, 1952; Moritz, 1953; Stokes; 1955; Burk, 1957; Eyer, 1969). Eyer (1969) proposed the name Smoot Formation for the previously unnamed red mudstone and siltstone just below the marine black shale of the Tygee Member. He considers it to Span the Aptian- Albian stage boundary because of the apparent Albian age of the overlying Bear River Formation. The lower boundary of the Gannett Group is considered by some to be conformable with the underlying marine Stump Formation of Jurassic age (Eyer, 1969) and unconformable UPPER CRET. Frontier Fm. Frontier Fm. Frontier Fm. R. Fm. Bechler Peterson Gonna" Grp. Undiv. Ephraim Cg. Ephraim Cg. JURASSK Figure 3 Stratigraphic nomenclature and probable equivalency of Lower Cretaceous strata in western Wyoming. Wm Eon Fossil syncun. - Meridian Anilclino T Figure 4 East-west structural cross section near the Stowe Creek section. (After Royse et a1., 1975) Pal = Paleozoic strata Horizontal Scale: 1" = 2.3 miles (3.7 km.) East Meridian Amlclino I”43):."ssrioo‘gtlio" J Green R. Basin 4000" .. ’ F" 1 "w“ ’ 7 + 7 . . 2 K 51. ‘ A I 9’. F" H‘“ ‘xg‘f' . u Poi Pol ‘, K“ -400d- Ku KI sow K " Figure 5 East-west structural cross section near the Fontenelle Creek section. (After Oriel, 1969) Pal - Paleozoic strata Horizontal Scale: 1" = 1.6 miles (2.6 km.) 10 by others (Burk, 1957). Cobban and Reeside (1952) suggested that the Gannett Group may be the only strata in the Western Interior to span the Neocomian. Bear River Formation; The age and stratigraphic position of the Bear River Formation was vehemently argued from 1859 to 1892 and constitutes what has been called by Thomas (1962) the classic "Bear River problem." The series of strata containing the nondmarine to brackish "Bear River fauna" was first discovered in 1859 by Henry Engelman, geologist to the United States exploring expedition in the charge of Captain Simpson, along the bank of Sulphur Creek near its junction with the Bear River 8% miles south- east of the present town of Evanston, Wyoming. Because of the lack of understanding of local structural conplexities, these non-marine beds appeared to be stratigraphically above the local coal-bearing strata called "Laramie." These structural problems and apparent faunal similarities with the "Lignite formation" in France (previously published and referred to the Tertiary) left little doubt that the "Bear River estuary beds,” as they were called, were Tertiary in age. In preparing the manuscript for his 1891 review of North American Cretaceous formations, C. A. White began to be convinced on the basis of paleontological evidence that the Bear River Formation might be older than the "Laramie." T. W. Stanton accompanied him in the field season of 1891 to the Bear River Valley where they were to continue White's previous studies. After a short time White had to leave Stanton to pursue the investigation alone. Stanton, through keen geological observation, was able to prove 11 that the Bear River Formation occupies a stratigraphic position between the Colorado Formation above and the Jurassic marine strata below. The following year Stanton published his results along with a supporting paper by White (Stanton, 1892; White, 1892). In 1895 White published his detailed, "The Bear River Formation and its characteristic fauna," which summarized all studies to that time. Veatch (1907) placed the Bear River Formation "conclusively in the Upper Cretaceous because of the fossil assem- blage collected on Little Muddy Creek, 3 miles southeast of Cumberland" (Sec. 3, 4, T. 18 N., R. 116 W.) More recently, Peck (1956) stated that the Bear River Formation probably contains both Upper and Lower Cretaceous rocks but later (Peck and Craig, 1962) concluded on the basis of its characteristic assemblage of freshwater charOphytes and ostracods and its stratig- raphic position below the Aspen Shale that it was entirely Lower Cretaceous. In Cobban and Reeside's "Correlation of the Cretaceous formations of the Western Interior of the United States," published in 1952, they placed the Bear River Formation in a position occupying the entire middle third of the Albian stage (pl. 1, col. 35, 62-64 and 66). Their placement was based on the late Albian cephalopods found in the Mbwry Shale (Aspen Shale equivalent). Yen, (1952) presents four reasons, based on comparison of non-marine gastropod faunas (particularly gygulifera) of the Bear River Formation with those of EurOpe, why the Bear River Formation must be Upper Cretaceous (Cenomanian) in age. As Moritz (1958) points out by quoting Reeside, "the difference of Opinion as not really great, for the tbme involved - latest Albian to earliest 12 Cenomanian - is only a small part of one EurOpean stage." The lithology of the Bear River Formation is heterogeneous and somewhat cyclic. Its Spatial relations suggest a complex array of westward thickening and intertonguing marine, brackish and non- marine beds represented by tan to buff sandstones, black to gray shales, siltstones, coquinoid limestones, coals and bentonites. The intertonguing facies relationships are most apparent in the central portions of the thrust belt and have warranted separate terminology east and west of the trace of the Absaroka thrust fault (Rubey, 1973). Rubey named four new formations which occur west and north of the Absaroka thrust fault and defined them as equivalent to the Bear River Formation and Aspen Shale on the east side (see Figure 3). These new formations are, in descending order: (1) the Sage Junction Formation, (2) the Cokeville Formation, (3) the Thomas Fork Formation and (4) the Smiths Formation, of which part of the type section is included in this study. It is time equivalent to roughly the lower third to half of the Bear River Formation. The Bear River Formation east of the Absaroka thrust attains a thickness of at least 1500 feet (Burk, 1957) and thins northward and eastward where its presumed equivalent, the "Dakota," is about 250 feet thick in the subsurface on the Rock Springs Uplift according to Anderman (1956). The t0p of the Bear River Formation is usually placed at the youngest sandstone below the Aspen Shale porcelanites or at the base of these distinctive porcelanites. Aspen Shale: The Aspen Shale was described by Veatch (1907, p. 64) 13 for 1500 to 2000 feet of black and gray shales near Aspen Station, Uinta County, Wyoming (T. 14 N., R. 118 W.) The Aspen Shale is easily distinguished by its light silvery-gray colored, weathered porcelanites containing fish scales locally. The formation thins locally to less than 1000 feet and also contains darker shales, siltstones and sandstones as well as the porcelanites of quartz latite composition. The Aspen Shale has been placed in the Lower Cretaceous since the work of Cobban and Reeside (1951) who identified Gastropites and NeogastroPites collected from both it and the equivalent Mowry Shale. Time Equivalent Strata ig_Adjacent Areas: The faunal uniqueness and heterogeneous lithology of the Bear River Formation have compounded the problem of age correlations in other areas. It is widely accepted that the Bear River Formation is time equivalent to the ThermOpolis Shale (restricted; Eicher, 1960), Muddy Sandstone and Shell Creek Formation to the east although the absence of foraminifera in the Bear River Formation makes this difficult to demonstrate. The Wayan Formation's partial time equivalence to the Bear River Formation is summarized by Stokes (1955): "The Wayan and Bear River Formations are nearly contemporaneous deposits laid down during the Early (?) and Late Cretaceous in such a manner that they show interfingering facies relation- ships along the central portions of the thrust belt. Although the lowest part of the Bear River has no equivalent in the Wayan and the highest part of the Wayan has no counterpart in the Bear River, the main bulk of the two formations may be considered as contemporaneous. Tongues of Bear River extend westward into the Wayan and tongues of the Wayan extend eastward into the Bear River." The Wayan Formation was named by Mansfield and Roundy (1916) for about 11,800 feet of strata in southeastern Idaho (Bannock County) without a defined t0p or base, which had previously been referred 14 to the Bear River Formation. Rubey (1973) points out that "redefinition of the Wayan Formation is clearly necessary" especially in light of its great thickness and Rubey's new Lower Cretaceous units. Although parts of the Beckwith Formation as originally defined (Veatch, 1907) and the revised Beckwith Formation (Mansfield and Roundy, 1916) have included strata which are time equivalent to the Bear River Formation, the general abandonment of the term precludes its discussion in this study. Paleogeography: In order to fully appreciate the problems involved in understanding the Early Cretaceous strata of southwestern Wyoming, it is desirable to envision the broad changes which had taken place since the Paleozoic and early Mesozoic. Thomas (1962) has discussed some of these changes and their related problems. During the Paleozoic and early Mesozoic southwestern Wyoming had been situated on the eastern shelf of the Cordilleran and Mesocordilleran miogeosynclines, respectively. These epicontinental seas had Pacific connections and although their depth varied through time with each transgression the waters were fairly shallow across Wyoming. Late Triassic and Early Jurassic time was marked by major paleotectonic change as a north-south trending landmass of folded and faulted Paleozoic sedimentary rocks began emerging west of Wyoming in the old miogeosyncline. This buckling had created a number of small, shallow basins to the east which received marine sediments (Stump Formation) up to Late Jurassic time when the sea (Sundance Sea) began retreating and the area east of the landmass developed into one huge, elongate basin. It was along the prograding 15 shorelines of this sea that the Morrison Formation was being deposited by northeasterly flowing, low gradient streams on the coastal plains (Furer, 1970). Contemporaneous terrestrial deposition of a synorogenic clastic wedge (lower Ephraim Conglomerate) adjacent to the new north-south landmass and the deposition of volcanic ash carried eastward from sources, probably, in west-central Idaho or possibly western Oregon also characterized the latest Jurassic. The upper Ephraim Conglomerate and Bechler Conglomerate which were deposited in western Wyoming and southeastern Idaho attest to the continued subsidence in this area during the Neocomian. Intervening periods of quiescence are apparent as indicated by the accumulation of freshwater sediments (Draney and Peterson Limestones) rich in charOphytes and ostracods which may be of Aptian age (Eyer, 1969). In early Albian time the Gulf Coast waters were not far from the Mexican border and boreal waters were invading northern Alberta and British Columbia (Lower Mannville Group). This boreal sea (Clearwater Sea) transgressed southward into central Alberta in middle Albian time. It was during this same time from middle Albian to earliest late Albian that the first marine waters since Late Jurassic time invaded the interior of the continent in a narrow north-south trough. According to Eicher (1962) the boreal sea extended far into the center of the continent but did not connect with the Gulf Coast sea until late ThermOpolis time (about middle-early Bear River time) when the Gulf Coast sea advanced northward over the former drain- age divide south of Kansas. This seaway which connected the Gulf 16 Coast and boreal seas has been called the Skull Creek seaway. It was also during late-middle (?) to middle-late Albian time that the Bear River Formation was being deposited in south* western Wyoming, southeastern Idaho and northeastern Utah. Royse and others (1975) envision the paleogeography as follows: "it is obvious that deposition of the Bear River Formation and equivalent strata centered in a structural downwarp in front of the Willard-Paris fault system. Much of the clastic material was derived from source areas on the hanging wall of this early fault plate. A large part of the deposition took place under marine conditions in an embayment that extended southwest across the Idaho-Wyoming boundary into northern Utah." Their reconstruction (Figure 2) shows a deep invagination of the sea with an outlet to the northeast and peripheral source areas to the south and southeast besides the Willard-Paris thrust to the west. The freshwater fossils reported in the Bear River Formation (charOphytes, ostracods and molluscs) probably lived in local areas bordering the embayment on the landward side where streams draining the western highlands flowed into the embayment. Transgressions and regressions of the sea undoubtedly effected the configuration of the embayment besides controlling the distribution of freshwater and brackish waters throughout Bear River time. The Bear River Formation does not contain foraminifera, possibly because of eutoxic conditions in the protected areas of the embayment or perhaps because of dilution of seawater by numerous streams flowing off the western highlands. Its coquinoid limestones and some shale units, however, contain a diverse molluscan fauna which has been studied by White (1895) 17 and more recently by Yen (1952). Some faunas observed in soft shale units appear to be dwarfed and further suggest locally adverse bottom conditions characteristic of restricted areas such as lagoons or estuaries. Thomas (1962) considers the Bear River Formation to be the nearshore, brackish water equivalent of the ThermOpolis (restricted, Eicher, 1960), Muddy Sandstone and Shell Creek Shale which were deposited farther to the east in generally more offshore marine conditions as evidenced by their foraminiferal content and general facies relationships. The seas apparently were again disconnected prior to the deposition of the boreal Shell Creek Shale (Eicher, 1962) which is probably roughly equivalent to the upper part of the Bear River Formation. Eicher suggests that this was the result of renewed warping or tilting during the "Muddy orogeny" perhaps in the area of the old continental divide south of Kansas. The latest Albian saw the deposition of marine shales (Aspen Shale = Mowry Shale) in a boreal embayment which extended south- ward only as far as northern Colorado and east into western North Dakota, South Dakota and Nebraska. Distribution of large quantities of volcanic ash from west-central Idaho and perhaps northeastern Oregon extended eastward over an area from western Colorado and north-central Montana across Wyoming and into the Dakotas. This is apparently the main factor responsible for the characteristically siliceous nature of the Aspen Shale and Mowry Shale. A renewed marine connection of the boreal and Gulf Coast 18 seas was effected in the early Cenomanian which would continue to latest Cretaceous time. DATA COLLECTION Localities: Stowe Creek Section: This section is located about 2 miles (3.2 kilometers) north-northeast of the type section of the Bear River Formation at "Old Bear River City," Uinta County, Wyoming (see Figure 1). The section was measured across steeply dipping overturned beds on the south end of Knight Ridge, northeast of Stowe Creek and the Union Pacific Railroad tracks. (Sec. 21, 22, T. 14 N., R. 119 W.; see Figure 4). The formation is 1299 feet (395.9 meters) thick and well exposed except for some of the softer shale units. This section is located just west of the Absaroka thrust trace and was deposited in a nearshore mud, sand and shale facies according to the reconstruction of Royse and others (see Figure 2). Fontenelle Creek Section: This section is well exposed in a gap of Oyster Ridge (Frontier Formation) formed by Fontenelle Creek (NEk Sec. 6, T. 24 N., R. 115 W.; see Figure 5) about 21 miles (33.8 kilometers) north of Kemmerer in Lincoln County, Wyoming. The Bear River Formation at this locality is 760 feet (231.6 meters) thick and exposed on both sides of Fontenelle Creek. This section is located between the Absaroka and Hogsback thrusts and was deposited in an offshore marine shale facies according to the reconstruction of Royse and others (see Figure 2). l9 20 LaBarge Creek Section: This section is exposed under structural conditions similar to the Fontenelle Creek section, located about 16 miles (25.7 kilometers) to the south. It is exposed along LaBarge Creek (SWk Sec. 17 and SE% Sec. 18, T. 27 N., R. 115 W.) in Lincoln County, Wyoming. During processing, the samples collected from this section were found to contain a residuum of carbonized and corroded palynomorphs of very low diversity. There is no apparent explanation for this phenomenon in terms of increased thermal alteration or depth of burial which would not have also affected the Fontenelle Creek section, a short distance to the south. Both sections are located 5-10 kilometers from major thrust traces and about 8000 feet (2450 meters) stratigraphically above the underlying plane of the Pine Ridge thrust where some thermal alteration should be expected. One possible explanation would be locally increased oxidizing conditions during deposition (perhaps in a semiclosed basin) or after burial. This is, however, very hard to envision having affected the entire Bear River Formation of the area. Because of the extremely poor palynomorph preservation and representation, the LaBarge Creek section is not treated further in this study. Smiths Formation Type Section: This section is located about 17 miles (27.4 kilometers) south of Afton, Wyoming (NW%, NE% Sec. 27, T. 29 N., R. 118 W.) and 1% miles (2.4 kilometers) west-northwest of the Smiths Fork Guard Station. According to Rubey (1973) the Smiths Formation is about 700 feet (169.0 meters) thick at this locality and is divided into an upper sandstone member and a lower shale member. The upper sandstone member is only partly exposed 21 as a ledge about 5 feet (1.5 meters) thick at the type locality. It averages 215 feet (65.6 meters) in thickness, however, at two of Rubey's reference sections a short distance away. Only the upper 195 feet (59.4 meters) of the lower shale member is now exposed and was sampled by the author for use in this study. This section is west of the Absaroka thrust and was deposited in an offshore marine facies according to the reconstruction of Royse and others (see Figure 2). Sample Collecting: The three stratigraphic sections of the Bear River Formation examined in this study were measured, described and sampled systematically in order to obtain the necessary stratigraphic information for later interpretation and compar- ison. This was achieved by collecting samples at significant lithologic changes and at approximately 15 foot (4.6 meter) intervals within the thick shale units. Each sample represents a 6 to 12 inch (15 to 30 centimeter) interval of relatively unweathered rock collected sometimes as deep as 2% feet (76 centimeters) below the surface in a pit dug with a mattock. Composite samples were collected from some thinner, resistant units (especially limestones and sand- stones) as noted in the sample information in.Appendix C. The Stowe Creek section was measured, described and sampled by Chevron U.S.A., Inc. geologists. The Bear River Formation at the Fontenelle Creek section and LaBarge Creek section were remeasured, redescribed and sampled by the author in the summer, 1977, using the measured sections of Horstman (1966, unpublished thesis) as a guide. The Smiths Formation type section was sampled by the author using the lithologic description given by Rubey (1973). 22 Those sections sampled by the author were measured using a brunton compass and jacob staff. Complete lithologic descriptions of the three productive sections are included in Appendix B. Preparation of Samples and Slide Making; Although it is impossible to prepare all samples of a stratigraphic suite identically, it is desirable to be as uniform as possible within practical limits. Samples in this study were processed according to the following schedule with microscopic examination at the conclusion of steps 5, 6, 7, 8 and 9. 1) Crush 50 to 100 grams of sample to 3 to 5 mm size; avoid powdering. 2) Place crushed sample in a pile on a paper towel and roll edges from all sides several times so sample is moved several inches each time. Quarter sample and transfer a representative quarter to balance for weighing (30 grams for limestones and sandstones and 5 to 10 grams for shales). 3) Transfer sample to beaker and cover with HCl (10%) if sample is calcareous; wash three times with distilled water after reaction is complete. 4) Cover sample with concentrated HF (50%) and allow to set with frequent stirring until disaggregated (24 to 96 hours); wash three times with distilled water. 5) Cover sample with warm.HCl (10%) and allow to set for 30 mdnutes with frequent stirring; wash three times with distilled water. 6) Transfer one-third aliquot of sample to 50 ml glass test tube and cover sample with 10 ml Schultz solution (7 parts concentrated 23 HNO3 to 1 part saturated KCLO3); the time allowed for this step varied with each sample (1 to 15 minutes) and was determined by the condition of organic material in each sample after step 5. Dilute immediately and wash three times with distilled water. 7) Cover sample with 5 to 10 m1 of KOH (5%) and allow to set after initial agitation for 2 minutes; dilute immediately with distilled water and wash three times. 8) For samples with considerable mineral matter proceed with heavy liquid separation. Mix sample with 10 to 15 ml ZnClz (sp. gr. 1.95) and centrifuge at 1200 R.P.M. for 30 minutes or until a clear separation is attained. Pour floating fraction into 90 m1 test tube and examine sink fraction to assure that it is devoid of palynomorphs. Repeat separation for a second crap of organic material from the sink fraction of the first separation. Transfer the float fraction to a 90 m1 test tube and dilute with distilled water in order to lower the specific gravity so the organic material will sink with further centrifuging. Centrifuge initially with twice the usual time and continue washing three additional tflmes. 9) Cover sample with 15 m1 of distilled water and add 1 drOp NH40H (10%) and 2 to 5 drOps Safranin O (1% in water). Dilute with distilled water after thirty seconds and wash until clear. 10) Transfer to small vial and cover with enough H.E.C. (Hydro- xyethyl Cellulose WP-09, Union Carbide Corp.) so that about one drop of residue will make one slide with the prOper density for easy identification and counting of palynomorphs. 11) Mix residue vigorously and transfer one drOp to a coverslip 24 with a Pasteur pipette and distribute as evenly as possible by using a toothpick. Allow to dry to a thin film on the hot plate and mount on microscOpe slide with 1% drops of Elvacite (Grade 2044, E. I. DuPont de Nemours & Co., Inc.) Allow to cure in oven at 35°C overnight. Counting Procedure: Counting of the palynomorphs in productive samples was carried out as described below in order to establish ranges and relative percentages of each taxon for later interpre- tation. Slides were first examined from representative parts of each section in order to establish the basic floral framework. The most suitable minimum number of palynomorphs to be counted per sample was determined by plotting the number of palynomorphs counted against the number of taxa encountered. These plots form species-diversity curves similar to those used by ecologists and others dealing with sampling from a pOpulation of organisms. With three samples of average diversity the curve leveled off between 125 and 150 palynomorphs counted. A count of 250 was decided upon as it would probably insure an adequate sampling for even any unusually diverse samples. During the counting some samples were found to contain taxa comprising over 40% of all palynomorphs in the sample. Counts on these samples were carried to 300, 400 or 500 to insure an adequate sampling of other palynomorphs. Every attempt was made in this study to identify palynomorphs to the generic and species level. When this was not possible they were identified at least to some potentially useful group such as unidentified trilete, bisaccate, tricolpate, angiosperm, 25 dinoflagellate, acritarch or simply counted as unidentified palynomorph. All slides were counted at 500x magnification on a Leitz Ortholux microscOpe (Michigan State University No. GG2667) in horizontal traverses in a prescribed, random method determined beforehand. In order to partially overcome any bias due to the positioning of residue on slides the first four traverses were made at 5.0, 9.0, 13.0 and 17.0 mm in from the tOp edge of the slide (farthest from the observer). These four traverses cross the middle of the four horizontal quarters of the slide. No more than 63 palynomorphs were counted in any one of these traverses so all four could be made. The remaining traverses (up to 47) were randomly chosen and recorded before counting began. Any additional slides were treated in the same manner until the sample was adequately counted. Several hundred additional specimens from each sample were scanned on a slide not used in counting to ensure representation in the record of most of the rarer palynomorphs. These occurrences were not included in counts but are recorded as a "trace" on the range charts (see Table 3). SYSTEMATICS Introduction: Several schools of thought exist on the systematic treat- ment above the generic level of Cretaceous terrestrial palynofloras. Some have followed the totally artificial placement of spores and pollen into morphologically distinct genera and artificial suprageneric taxa (Potonie and Kremp, 1954, 1955, 1956; Potonie, 1956, 1958, 1960). Others (Couper, 1958; Singh, 1964, 1971) have followed a more natural approach and attempted to place these existing morphologically distinct genera in suprageneric taxa based on their resemblance to living families, classes or orders, depending upon the strength of comparison. The second approach has obvious paleoenvironmental advantages if the relationship to modern taxa can be demonstrated or strongly suggested. This is not possible, however, in many cases and may create misconcep- tions about affinities which lead to invalid conclusions. In spite of these limitations it is usually possible to speculate broadly about the affinities of certain genera when they are found in associa- tion with other genera in numerous floras and under similar paleo- environmental conditions. In this study the terrestrially-derived palynomorphs have been listed in alphabetical order in the following categories: TRILETE SPORES, MDNOLETE SPORES, SPORES-INCERTAE SEDIS, GYMNOSPERM POLLEN and ANGIOSPERM POLLEN. The angiosperm pollen have been further divided into the subcategories: Monosulcate, Tricolpate, Tricolporate and Incertae Sedis. The artificial classifications of Sarjeant and Downie 26 27 (1974) and Downie, Evitt and Sarjeant (1963) have been followed in the treatment of the dinoflagellate cysts and acritarchs, respectively. Because of the poor preservation and paucity of bisaccate pollen, all but several distinct forms were placed in categories based upon their superficial morphological resemblance to modern genera. The following information is included, as applicable, with each taxon listed: (1) basionym and currently accepted generic designation for published species. (2) pertinent synonymy or reference. (3) description for previously unpublished species or species of uncertain taxonomic placement (designated with cf. or "?"). (4) size range of specimens in this study if pertinent. (5) stratigraphic range reported from other studies; number of samples in which the species is present, relative abundance of the species in all samples (trace = found only by scanning beyond number counted, rare = <1%, occasional = l-l.9%, common = 2-4.9%, abundant = 5-9.9%, dominant = 10-40% and flooding = >40%) and stratigraphic occurrence in this study (SCS = Stowe Creek section, FCS = Fontenelle Creek section and SFTS = Smiths Formation type section). (6) suggested affinity for terrestrially-derived forms. (7) comments on various tapics pertinent to taxonomic placement, affinities, distinguishing characteristics, etc . (8) slide number and coordinates of a typical Specimen for unpublished species and Species of uncertain taxonomic placement. A complete listing of the Slide numbers and coordinates of all illustrated specimens is found in Appendix A. Slide numbers are accession numbers of the palynology and paleobotany laboratory at Michigan State University. The horizontal 28 and vertical coordinates, respectively, are taken from a Leitz Ortholux microsc0pe (Michigan State University No. GGZ667). Each slide examined is marked with "X" scratched just off the coverslip in the upper left-hand corner of the slide. The coor- dinates of this "X" are noted on each slide label and provide the possibility to examine reference and illustrated specimens with other microscOpeS (see Traverse, 1958). Appendix A provides a complete taxonomic listing with: (1) the number assigned to each species in the palynoflora, (2) reference and illustrated specimen coordinates, (3) plate and figure locations for each taxon and (4) the text page number where the systematic treatment is located. Photomicrographs were taken with a Leitz Orthomat microscOpe camera mounted on a Leitz Ortholux microsc0pe. Photos were taken with Panatomic-X film developed in Microdol-X and printed on polycontrast paper. 29 TRILETE SPORES GENUS Acanthotriletes Naumova, 1939 ex Potonie and Kremp, 1954 Type species: Acanthotriletes ciliatus (Knox) Potonie and Kremp, 1954 Acanthotriletes varispinosus Pocock, 1962 Plate 1, Figure 1 1962 Pocock, p. 36, pl. 1, fig. 18-20. Occurrence: Early Cretaceous, see Singh (1971, p. 45); 7 samples, trace to rare, found in all three sections. Suggested affinity: Selaginellaceae. Comments: Pocock (1962) points out the close resemblance of this Species to several modern species of Selaginella. GENUS Aequitriradites Delcourt and Sprumont, 1955 Type Species: Aequitriradites dubius Delcourt and Sprumont, 1955 Aequitriradites spinulosus (Cookson and Dettmann) Cookson and Dettmann, 1961 Plate 1, Figure 2 1958 Cirratriradites spinulosus Cookson and Dettmann, p. 113, pl. 18, fig. 9-13; pl. 19, fig. 1-5. 1961 Aequitriradites spinulosus (Cookson and Dettmann) Cookson and Dettmann, p. 426, pl. 52, fig. 1-12. Occurrence: Early Cretaceous to Danian, see Singh (1971, p. 34); 3 samples, trace to common, not found in SFTS. Suggested affinity: Selaginellaceae. Comments: Brenner (1963) points out the similarity of this Species 30 to spore types in the modern Selaginella megastachys group. GENUS Appendicisporites Weyland and Krieger, 1953 Type species: Appendicisporites tricuspidatus Weyland and Krieger, 1953 Appendicisporites potomacensis Brenner, 1963 Plate 1, Figure 3 1963 Brenner, p. 46, pl. 6, fig. 4, 5. Occurrence: Barremian to Albian, see Singh (1971, p. 62); 5 samples, rare to common, not found in SFTS. Suggested affinity: Schizaeaceae. Comments: This Species differs from.AppendiciSporites problematicus (Burger) Singh which has outer flange-like equatorial ribs. AppendiciSporites problematicus (Burger) Singh, 1971 Plate 1, Figure 4 1966 Plicatella problematica Burger, p. 245, pl. 10, fig. 3. 1971 Appgndicisporites problematicus (Burger) Singh, p. 63, pl. 6, fig. 1-6. Size range: Equatorial diameter (6 specimens): 42(46)53.umi Occurrence: Berriasian to Albian, see Srivastava (1975, p. 17); 7 samples, trace to occasional, not found in SFTS. Suggested affinity: Schizaeaceae. Appendicisporites Sp. Plate 1, Figure 5 Description: Trilete Spore; laesurae extending to equator; commissure raised and becoming wider toward the equator where a 3 to 5.um 31 projecting appendix is formed. Amb triangular with slightly convex sides. Proximal face canaliculate with 5 to 8 equally Spaced ribs running parallel with the Side in each interradial area. Ribs on both faces about 2.um thick and distinctly raised. Size range: Equatorial diameter (3 Specimens): 43(49)53.um. Occurrence: 4 samples, trace to rare, found only in the lower 500 feet (150 meters) of SCS and lowermost FCS. Sgggested affinipy: Schizaeaceae. Comments: Specimens assigned to this Species superficially resemble Appendicipporites bilateralis Singh but have significantly different canaliculate sculpture. Reference ppecimen: Slide Pbll602-5, 38.2 X 127.8. GENUS BiretiSporites Delcourt and Sprumont, 1955 Type ppecies: Biretisporites potoniaei Delcourt and Sprumont, 1955 Biretispprites potoniaei Delcourt and Sprumont, 1955 Plate 1, Figure 6 1955 Delcourt and Sprumont, p. 40, fig. 10. Sypgpzmy and description: see Delcourt, Dettmann and Hughes (1963, p. 284). §155_£gpgg: Equatorial diameter (4 specimens): 40(43)47.um. Occurrence: Early Cretaceous, see Singh (1971, p. 49); 20 samples, trace to common, found throughout all three sections. §gggested affinity: Osmondaceae and/or HymenOphyllaceae. Comments: This Species is characterized by its raised commissures and scabrate exine. 32 GENUS Camarozonosporites Pant, 1954 ex Potonie, 1956, emend. Klaus, 1960 Type species: Camarozonosporites cretaceus (Weyland and Krieger) Potonie, 1956 Camarozon08porites ambigens (Fradkina) Playford, 1971 Plate 1, Figure 7 1964 Camptotriletes ambigens Fradkina 13 Fradkina and Kiseleva, p. 70, pl. 1, fig. 3-5. 1971 Camarozonosporites ambigens (Fradkina)Playford, p. 540, pl. 104, fig. 22, 23. Sngngy: see Playford (1971, p. 540). Size range: Equatorial diameter (5 Specimens): 27(30)36.um. Occurrence: Albian to Senonian, see Playford (1971, p. 540); 25 samples, trace to common, not found in SFTS. §pggested affinipy: Lyc0podiaceae. Comments: The average size of specimens in this study approaches the lower limit of ranges quoted by previous authors (Fradkina, 1967, 27(43)60.um; Norris, 1967, 30 to 55.nm). Brenner (1963, p. 43) points out the resemblance of this Species to the modern spores of Lchpodium cernuum. GENUS Cicatricosisporites Potonie and Gelletich, 1933 Type species: Cicatricosisporites dorogensis Potonie and Gelletich, 1933 Cicatricosisporites hallei Delcourt and Sprumont, 1955 Plate 1, Figure 8 1955 Delcourt and Sprumont, p. 17, pl. 1, fig. 1. §ypgpygy: see Norris (1967, p. 92). 33 Occurrence: Early Cretaceous to Cenomanian, see Singh (1971, p. 71); 8 samples, trace to occasional, not found in SFTS. Suggested affinity: Schizaeaceae. Cicatricosisporites minor (Bolkhovitina) Pocock, 1954 Plate 1, Figure 9 1959 Mohria minor Bolkhovitina, p. 93, pl. 2, fig. 31. 1961 Pelletieria minor (Bolkhovitina) Bolkhovitina, p. 68, pl. 19, fig. 8; pl. 22, fig. 3a-c. 1964 Cicatricosisporites minor (Bolkhovitina) Pocock, p. 160, pl. 2, fig. 20-23. ‘Sigg_ggpgg: Equatorial diameter (5 Specimens): 22(25)29.nm. Occurrence: Middle Albian to Late Cretaceous, see Singh (1971, p. 74); 22 samples, trace to dominant, found throughout all three sections. §gggested affinity: Schizaeaceae. Cicatricosisporites subrotundus Brenner, 1963 Plate 2, Figure l 1963 Brenner, p. 51, pl. 10, fig. 1, 2. Sigg_ggpgg: Equatorial diameter (3 specimens): 42(46)51 um” Occurrence: Albian, see Singh (1971, p. 79); 4 samples, trace to rare, not found in SFTS. Suggested affinity: Schizaeaceae. Cicatricosisporites venustus Deak, 1963 Plate 1, Figures 10, 11 1963 Deak, p. 252, pl. 2, fig. 8-9, 12-13. Synonymy: see Singh (1971, p. 80). 34 Occurrence: Barremian to Cenomanian-Turonian, see Singh (1971, p. 80); 17 samples, trace to occasional, not found in SFTS. Suggested affinity: Schizaeaceae. Cicatricosisporites sp. Occurrence: 49 samples, trace to abundant, found throughout all three sections. Sgggested affinity: Schizaeaceae. Comments: Canaliculate and cicatricose Specimens here included were not identified to species level because of mechanical distortions, poor preservation or lack of a complete Specimen. These factors are particularly critical in the identification of CicatricosiSporites- like spores because the proximal and distal sculpture pattern must be clearly visible for Speciation. GENUS Cingutriletes Pierce, 1961, emend. Dettmann, 1963 Type Species: Cingutriletes congruens Pierce, 1961 Cingutriletes clavus (Balme) Dettmann, 1963 Plate 2, Figure 2 1957 Sphagnites clavus Balme, p. 16, pl. 1, fig. 4-6. 1963 Cingutriletes clavus (Balme) Dettmann, p. 69, pl. 14, fig. 5-8. Synonymy: see Dettmann (1963, p. 69) and Norris (1967, p. 97). Occurrence: Worldwide distribution in Jurassic and Tertiary rocks; 2 samples, rare, found only in SFTS and SCS. Suggested affinity: Sphagnaceae. 35 GENUS Concavisporites Pflug ip_Thomson and Pflug, 1953, emend. Delcourt and Sprumont, 1955 Type Species: Concavisporites rugulatus Pflug ip Thomson and Pflug, 1953 ConcaviSporites jurienensis Balme, 1957 Plate 2, Figure 3 1957 Balme, p. 20, pl. 2, fig. 30, 31. Synonymy and description: see Burger (1966, p. 237). §l££.£2282? Equatorial diameter (5 Specimens): 25(28)33 um. Occurrence: Worldwide distribution in Late Jurassic and Early Cretaceous rocks; 6 samples, trace to rare, found only in SCS. Suggested affinity: PteridOphyta. Comments: Although the illustrated specimens in the literature assigned to this Species Show considerable morphologic variation, the Specimens in this study compare favorably with the holotype of Balme (1957, pl. 2, fig. 30, 31). GENUS Concavissimipporites Delcourt and Sprumont, 1955, emend. Delcourt, Dettmann and Hughes, 1963 Type Species: Concavissimisporites verrucosus Delcourt and Sprumont, 1955, emend. Delcourt, Dettmann and Hughes, 1963 Comments: Dettmann (1963) noted the Similarity of spores assigned to this genus with Spores of certain living Species of Cyathea Smith, Dicksonia L'Herit and Lygodium Swartz. Concavissimisporites punctatus (Delcourt and Sprumont) Brenner, 1963 Plate 2, Figure 5 1955 Concavisporites punctatus Delcourt and Sprumont, p. 25, pl. 1, fig. 8; pl. 2, fig. 2. 36 1963 Concavissimisporites punctatus (Delcourt and Sprumont) Brenner, p. 59, pl. 14, fig. 6. Synonymy: see Srivastava (1975, p. 31). Occurrence: Upper Bathonian to Turonian, see Srivastava (1975, p. 32); 17 samples, trace to occasional, found in all three sections. Suggested affinity: PteridOphyta. Concavissimisporites variverrucatus (Couper) Brenner, 1963 Plate 2, Figure 4 1958 Concavisporites variverrucatus Couper, p. 142, pl. 22, fig. 4, 5. 1963 Concavissimisporites variverrucatus (Couper) Brenner, p. 59, pl. 14, fig. 4. Sypgpymy: see Srivastava (1975, p. 32). Occurrence: Bajocian to Albian, see Srivastava (1975, p. 33); 2 samples, trace, found only in SCS. Suggested affinity: PteridOphyta. GENUS CoronatiSpora Dettmann, 1963 Type Species: Coronatispora perforata Dettmann, 1963 Coronatispora valdensis (Couper)Dettmann, 1963 Plate 2, Figure 7 1958 Cingulatisporites valdensis Couper, p. 146, pl. 24, fig. 6, 7. 1963 CoronatiSpora valdensis (Couper) Dettmann, p. 67. Sypgpygy: see Srivastava (1975, p. 33, 34). Occurrence: Late Jurassic to Albian, see Srivastava (1975, p. 34); 2 samples, rare, found only in SCS and FCS. Suggested affinity: PteridOphyta. 37 GENUS CostatOperforOSporites Deak, 1962 Type species: Costatoperforosporites fistulosus Deak, 1962 CostatOperforosporites fistulosus Deak, 1962 Plate 2, Figure 8 1962 Deak, p. 233, pl. 27, fig. 1-3. Description: see Singh (1971, p. 86). Sigg_£gggg: Equatorial diameter (3 Specimens): 33(38)47.um. Occurrence: Late Aptian to Albian, see Singh (1971, p. 86); 8 samples, trace to common, not found in SFTS. Suggested affinity: Schizaeaceae. Comments: The Specimens from this study are Slightly smaller than the type material of Deak which is 45 to 50.nm. GENUS Cyathidites Couper, 1953 Typg Species: Cyathidites australis Couper, 1953 Comments: Balme (1957, p. 21) points out that Cyathidites is basically a morphologic form genus with similar types occurring in the Dicksoniaceae and Polypodiaceae as well as the Cyatheaceae. Srivastava (1975) has suggested the synonymy of Deltoidoppora Miner and Cyathidites Couper. He feels that distinction on the basis of amb shape of exine thickness is hypothetical and thus, meaningless. In this study the two genera were sucessfully differentiated as in other Lower Cretaceous Studies in North America. Cyathidites australis Couper, 1953 Plate 2, Figure 10 38 1953 Couper, p. 27, pl. 2, fig. 11, 12. §ypgpymy: see Dettmann (1963, p. 22). Occurrence: Worldwide distribution in Jurassic and Cretaceous rocks; 16 samples, trace to common, found in all three sections. Spggested affinity: Cyatheaceae, Dicksoniaceae and/or Polypodiaceae. Cyathidites minor Couper, 1953 Plate 2, Figure 9 1953 Couper, p. 28, pl. 2, fig. 13. Occurrence: Worldwide distribution in Jurassic and Cretaceous rocks; 50 samples, rare to dominant, found throughout all three sections. Suggested affinity: Cyatheaceae, Dicksoniaceae and/or Polypodiaceae. GENUS Deltoidospora Miner, 1935, emend. Potonie, 1956 Type Species: Deltoidospora hallii Miner, 1935 DeltoidOSpora psilostoma Rouse, 1959 Plate 2, Figure 6 1959 Rouse, p. 311, pl. 2, fig. 7, 8. Occurrence: Late Jurassic to Late Cretaceous of North America; 1 sample, common, found only in Pb11602 at the base of FCS. Suggested affinity: Cyatheaceae and/or Dicksoniaceae. Deltoidospora Sp. cf. 2, juncta (Kara-Morza) Singh, 1964 Plate 2, Figure 11 cf. 1956 Cibotum junctum Kara-Murza i_n Bolkhovitina, p. 37, pl. 3, fig. 25a-e. 39 cf. 1964 Deltoidospora junctum (Kara-Murza) Singh, p. 81, pl. 9, fig. 16. cf. 1967 Deltoidospora jpncta (Kara-Murza) Singh: Norris, p. 86, pl. 10, fig. 4, 5. Description: Trilete; commissures slightly raised and reaching or nearly reaching the equator; equatorial outline deltoid with Straight or very Slightly concave sides; apices rounded; proximal exine smooth to slightly scabrate; distal exine folded on itself perpendicular to the laesurae between 1/2 and 1/3 the distance to the apices. Size range: Equatorial diameter (10 specimens): 17(19)22 um. Occurrence: 17 samples, trace to abundant, not found in SFTS. Sgggested affinity: Cyatheaceae and/or Dicksoniaceae. Comments: Part of the Albian material described by Brenner (1963, p. 52, pl. 11, fig. 3a, b) as Gleicheniidites gpilobatus appears to be conspecific with Deltoidospora Sp. cf. 2, jgpgtg. Reference gpecimen: slide Pbll621-1, 39.0 X 119.0. GENUS Foraminisporis Krutzsch, 1959 Type gpecies: Foraminisporis foraminis Krutzsch, 1959 Foraminipporis wonthaggiensis (Cookson and Dettmann) Dettmann, 1963 Plate 2, Figure 13 1958 ApiculatiSporis wonthaggiensis Cookson and Dettmann, p. 100, pl. 14, fig. 7-10. 1963 ForamdniSporiS wonthaggiensis (Cookson and Dettmann) Dettmann, p. 71, pl. 14, fig. 19-23, text-fig. 40. Occurrence: Valanginian to Turonian, see Singh (1971, p. 36); 2 samples, trace to rare, found only in FCS and the Aspen Shale 40 of SCS. Suggested affinity: Hepaticae. Comments: Dettmann (1963) points out the Shmilarity of this species to spores in the modern hepatic Species Nothylas breutelii Gottsche. GENUS Gleicheniidites Ross, 1949 ex Delcourt and Sprumont, 1955, emend. Dettmann, 1963 Type ppecies: Gleicheniidites senonicus Ross, 1949 Gleicheniidites senonicus Ross, 1949 Plate 2, Figure 12 1949 Ross, p. 31, pl. 1, fig. 3, 4. Occurrence: Worldwide distribution in Jurassic, Cretaceous and Tertiary rocks; 58 samples, rare to dominant, found throughout all three sections. Sgggested affinity: Gleicheniaceae. Comments: There is a great amount of morphologic diversity and size variability with this Species (Srivastava, 1975). The specimens of this Study most resemble the illustrated material of various authors from Western and Arctic Canada. Gleicheniidites Sp. cf. g, circinidites (Cookson) Dettmann, 1963 Plate 3, Figure 1 cf. 1953 Gleichenia circinidites Cookson, p. 464, 465, pl. 1, fig. 5, 6. 1957 Gleichenia Sp. cf. Q, circinidites Cookson: Balme, p. 23, pl. 3, fig. 42-44. 1963 Gleicheniidites Sp. cf. g, circinidites (Cookson) Dettmann, p. 65, pl. 13, fig. 6-10. Occurrence: Late Jurassic and Early Cretaceous, see Singh (1971, 41 p. 97); 20 samples, trace to common, found in all three sections. Sggggsted affinity: Gleicheniaceae. Comments: This Species is differentiated from Gleicheniidites senonicus Ross which has more rounded apices and thinner interradial crassitudes. Norris (1967) illustrates Specimens similar to Q, Sp. cf. g, circinidites of this Study but places them in g, senonicus. He suggests that Q, Sp. cf. Q, circinidites may be a distinctive preservational type of Q, senonicus. Reference Specimen: Slide Pb11639-1, 38.0 X 119.3. GENUS Klukisporites Couper, 1958 Type ppecies: Klukisporites variegatus Couper, 1958 Klukisporites pseudoreticulatus Couper, 1958 Plate 3, Figure 2 1958 Couper, p. 138, pl. 19, fig. 8-10. Occurrence: Late Jurassic to early Cenomanian, see Singh (1971, p. 96); 5 samples, trace to common, not found in SFTS. Suggested affinity: Schizaeaceae (Couper, 1958; Dettmann, 1963). "Koilisporis excavatus" (Brenner) Pannella, 1966 (unpublished manuscript name) Plate 3, Figures 4, 5 1963 Matonisporites excavatus Brenner, p. 54, pl. 12, fig. 2, 3. 1966 "KoiliSporis excavatus" (Brenner) Pannella (unpublished manuscript name), p. 48, pl. 4, fig. 3. Description: see Brenner (1963, p. 54) and Pannella (1966, p. 48). Size range: Equatorial diameter (4 specimens): 39(45)52.um. 42 Occurrence: Albian to Cenomanian. Patapsco Formation in Maryland (Brenner, 1963), Dakota Group and Graneros Shale of the Denver Basin (Pannella, 1966); 1 sample, rare, found only in Pbll602 at the base of FCS. Spggested affinity: Matoniaceae 2 Comments: Pannella (1966, p. 46—48, unpublished thesis) designated a new manuscript genus, "KoiliSporis," to accommodate Matonisporites- type Spores with a "distal thinning and the absence of true valvae." One of his three manuscript Species, "Koilisporis excavatus" (Brenner) Pannella, appears to be conspecific with Specimens encountered in this study. Pannella created the new genus because the distinctive distal thinning with a thick ring is present on all three of his prOposed new manuscript Species and Dettmann (1963) had amended Matonisporites to include only valvate spores. This is a case in which the erection of a new genus is clearly justified but must be published so as to be valid and useful. The name "KoiliSporiS excavatus" is used in this study as a convenience pending the publication of a valid name. GENUS Kuylisporites Potonie, 1956 Type Species: Kuylisporites waterbolki Potonie, 1956 prliSporites lunaris Cookson and Dettmann, 1958 Plate 3, Figure 3 1958 Cookson and Dettmann, p. 103, pl. 14, fig. 21-23. Description: see Dettmann (1963, p. 39). Size rapge: Equatorial diameter (1 Specimen): 31,um. 43 Occurrence: Early Cretaceous, see Singh (1971, p. 102); 1 sample, rare, found only in Pb11238 (ASpen Shale) at the t0p of SCS. Suggested affinity: Cyatheaceae and/or Dicksoniaceae. Comments: The only Specimen encountered was slightly smaller than the type material. Dettmann (1963) points out the slight resemblance of this species to Alsophila blechnoides of the Cyatheaceae. GENUS Lyc0podiumsporites Thiergart, 1938 ex Delcourt and Sprumont, 1955 Type species: Lyc0podiumsporites agathoecus (Potonie) Thiergart, 1938 Lyc0podiumsporites austroclavatidites (Cookson) Potonie, 1956 Plate 3, Figure 6 1953 Lyc0podium austroclavatidites Cookson, p. 469, pl. 2, fig. 35. 1956 Lyc0podiumSporites austroclavatidites (Cookson) Potonie, p. 46. Sypgpygy: see Dettmann (1963, p. 44). Size range: Equatorial diameter (5 Specimens): 36(42)45 um. Occurrence: Worldwide distribution in Jurassic and Cretaceous rocks; 4 samples, trace to rare, found only in the lower half of FCS and SCS. Suggested affinity: Lyc0podiaceae. GENUS Neoraistrickia Potonie, 1956 Type gpecies: Neoraistrickia truncata (Cookson) Potonie, 1956 44 Neoraistrickia truncata (Cookson) Potonie, 1956 Plate 3, Figure 7 1953 Triletes truncata Cookson, p. 471, pl. 2, fig. 36. 1956 Neoraistrickia truncata (Cookson) Potonie, p. 34, pl. 3, fig. 32. Synonymy and description: see Dettmann (1963, p. 36). Occurrence: Worldwide distribution in Jurassic and Cretaceous rocks; 1 sample, rare, found only in Pb11613 near the tOp of FCS. Suggested affinity: Selaginellaceae. Comments: Only a single Specimen of this Species was encountered. Dettmann (1963, p. 36) points out the Similarity of this Species to the Spores of Knox's (1950) Selaginella biformis group. GENUS Ornamentifera Bolkhovitina, 1966 Type species: Ornamentifera echinata (Bolkhovitina) Bolkhovitina, 1966 Ornamentifera echinata (Bolkhovitina) Bolkhovitina, 1966 Plate 3, Figure 8 1953 Gleichenia echinata Bolkhovitina, p. 55, pl. 8, fig. 17. 1966 Ornamentifera echinata (Bolkhovitina) Bolkhovitina, p. 69. Synonymy and description: see Singh (1971, p. 98). Occurrence: Hauterivian to Senonian, see Singh (1971, p. 98); 8 samples, trace to occasional, found near the base of FCS and SCS. Suggested affinity: Gleicheniaceae (Singh, 1971). 45 GENUS Osmundacidites Couper, 1953 Type species: Osmundacidites wellmanii Couper, 1953 Osmundacidites wellmanii Couper, 1953 Plate 3, Figure 10 1953 Couper, p. 20, pl. 1, fig. 5. Occurrence: Worldwide distribution in Jurassic and Cretaceous rocks; 1 sample, trace, found only in sample Pb11642 near the t0p of FCS. Suggested affinity: Osmundaceae. GENUS Pilosisporites Delcourt and Sprumont, 1955 Type species: Pilosisporites trichopapillosus (Thiergart) Delcourt and Sprumont, 1955 Pilosisporites trichgpapillosus (Thiergart) Delcourt and Sprumont, 1955 Plate 3, Figure 11 1949 Sporites trichOpapillosus Thiergart, p. 22, pl. 4, fig. 18. 1955 Pilosisporites trichOpapillosus (Thiergart) Delcourt and Sprumont, p. 34, pl. 3, fig. 3. Occurrence: Purbeckian to Albian, see Singh (1971, p. 129); 3 samples, trace to rare, not found in SFTS. Suggested affinity: PteridOphyta. GENUS Psilatriletes van der Hammen, 1954 ex Potonie, 1956 Type species: Psilatriletes detortus (Weyland and Krieger) Potonie, 1956 46 Psilatriletes radiatus Brenner, 1963 Plate 3, Figure 9 1963 Brenner, p. 63, pl. 20, fig. 6, 7. Occurrence: Barremian to early Cenomanian, see Singh (1971, p. 133); 2 samples, occasional to common, found in the lower half of SCS. Suggested affinity: PteridoPhyta. GENUS Stereisporites Pflug ig_Thomson and Pflug, 1953 Type species: StereiSporites stereoides (Potonie and Venitz) Pflug, 1953 Stereisporites antiguasporites (Wilson and Webster) Dettmann, 1963 Plate 3, Figure 12 1946 Sphagnum antiguasporites Wilson and Webster, p. 273, fig. 2. 1963 Stereisporites antiquasporites (Wilson and Webster) Dettmann, p. 25, pl. 1, fig. 20, 21. §y§ggygy: see Dettmann (1963, p. 25). Occurrence: Worldwide distribution in Jurassic and Tertiary rocks; 33 samples, trace to abundant, found throughout all three sections. Suggested affinity: Sphagnaceae. GENUS Todisporites Couper, 1958 Type species: Todisporites major Couper, 1958 Todisporites minor Couper, 1958 Plate 3, Figure 13 1958 Couper, p. 135, pl. 16, fig. 9, 10. 47 Occurrence: Bajocian to Cenomanian, see Singh (1971, p. 50); 6 samples, trace to rare, found in the ASpen Shale of FCS and throughout SCS. §gggested affinity: Osmundaceae. Comments: Couper (1958, p. 135) points out the likelihood of spores in this genus belonging to the fern represented by mega- fossils identified as Todites williamsonii and Todites princeps. GENUS Trilobosporites Pant, 1954 ex Potonie, 1956 Typg_species: Trilobosporites hannonicus (Delcourt and Sprumont) Potonie, 1956 Trilobosporites minor Pocock, 1962 Plate 4, Figure 1 1962 Pocock, p. 44, pl. 4, fig. 61, 62. Occurrence: Aptian to Cenomanian. Quartz Sand'Member and Calcareous Member (Lower Mannville Group) of the Western Canada.P1ains (Pocock, 1962); Mannville Group except the basal Deville Member of east— central Alberta (Singh, 1964); Lower Cretaceous of the Saskatoon area (Steeves and Wilkins, 1967); "Walnut" clay facies of southern Oklahoma (Hedlund and Norris, 1968); Tuscaloosa Formation of the southern U.S.A. (Phillips and Felix, 1971a). This study: 3 samples, rare, not found in SFTS. Suggested affinity: PteridoPhyta. GENUS Triporoletes Mtchedlishvili igLMtchedlishvili and Samoilovitch, 1960, emend. Playford, 1971 Type species: Triporoletes singularis Mtchedlishvili ig.Mtchedlishvili and Samoilovitch, 1960 48 Triporoletes reticulatus (Pocock) Playford, 1971 Plate 4, Figure 2 1962 Rouseisporites reticulatus Pocock, p. 53, pl. 7, fig. 101- 105. 1971 Triporoletes reticulatus (Pocock) Playford, p. 552, pl. 106, fig. 5. Synggygy: see Srivastava (1975, p. 72). Description: see Dettmann (1963, p. 97). Occurrence: Early Cretaceous, see Srivastava (1975, p. 72); 4 samples, trace, found only in SCS. §gggested affinity: Hepaticae. Comments: Dettmann (1963) pointed out the resemblance of this species to spores of the modern hepatic species Riccia beyrichiana Hampe. GENUS Undulatisporites Pflug ig_Thomson and Pflug, 1953 Type species: Undulatisporites microcutis Pflug i9 Thomson and Pflug, 1953 Undulatisporites undulapolus Brenner, 1963 Plate 4, Figure 3 1963 Brenner, p. 72, pl. 24, fig. 1. Occurrence: Barremian to Albian, see Singh (1971, p. 148); 10 samples, trace to rare, found in all three sections. §gggested affinity: PteridOphyta. Comments: Specimens in this study were somewhat variable in the width of the thickened lips bordering the laesurae and the shape of the amb. 49 GENUS Verrucosisporites Ibrahim, 1933, emend. Potonie and Kremp, 1954 Type species: VerrucosiSporites verrucosus Ibrahim, 1933, emend. Potonie and Kremp, 1954 Verrucosisporites rotundus Singh, 1964 Plate 4, Figure 4 1964 Singh, p. 96, pl. 13, fig. 3. Occurrence: Aptian and Albian, see Singh (1971, p. 149); 4 samples, trace to rare, not found in SFTS. Suggested affinity: PteridOphyta. Verrucosisporites sp. Plate 4, Figure 5 Description: Trilete ? Laesurae, if present, are indistinct. Equatorial outline ovoid. Exine about 1 to 2,um thick and densely covered with verrucae with diameters from 1 to 5.um. Central area of one face very thin or missing but with no apparent marginal features. Sig; gangs: Equatorial diameter - long dimension (8 specimens): 36(43)55 .um. Equatorial diameter - short dimension: 29(37)40,um. Occurrence: 12 samples, trace to rare, found in all three sections. Sgggested affinity: Unknown. Comments: The lack of an observable trilete mark makes the assign- ment to this genus provisional. Verrucosisporites obscurilaesuratus Pocock is similar to specimens of Verrucosisporites sp. but has very indistinct laesurae and continuous verrucose sculpture on both faces. 50 Reference specimen: slide Pb11642-6, 37.5 X 116.1. MDNOLETE SPORES GENUS Laevigatosporites Ibrahim, 1933, emend. SchOpf, Wilson and Bentall, 1944 Type species: Laevigatosporites vulggris (Ibrahim) Ibrahim, 1933 Comments: Singh (1964) remarks that the bean-shaped form of this genus indicates a close affinity with the Polypodiaceae and Dennstaedtiaceae. Laeviggtosporites ovatus Wilson and Webster, 1946 Plate 4, Figure 6 1946 Wilson and Webster, p. 273, fig. 5. Synonypy: see Dettmann (1963, p. 86). Description: see Singh (1964, p. 99). Size range: Length (5 specimens): 32(34)40‘um. Breadth: 18(25)35,um. Occurrence: Worldwide distribution in Jurassic, Cretaceous and Tertiary rocks; 18 samples, trace to occasional, found throughout all three sections. Suggested affinity: Polypodiaceae and/or Dennstaedtiaceae. SPORES (Incertae Sedis) GENUS Schizosporis Cookson and Dettmann, 1959 Type species: Schizosporis reticulatus Cookson and Dettmann, 1959 51 Schizosporis parvus Cookson and Dettmann, 1959 Plate 4, Figure 7 1959 Cookson and Dettmann, p. 216, pl. 1, fig. 15-20. Occurrence: Barremian to Cenomanian, see Singh (1971, p. 151); 2 samples, trace to rare, found only in SCS. Suggested affinity: Unknown. Schizosporis reticulatus Cookson and Dettmann, 1959 Plate 4, Figure 9 1959 Cookson and Dettmann, p. 216, pl. 1, fig. 5-9. Occurrence: Berriasian to Cenomanian, see Singh (1971, p. 151); 1 sample, trace, found only in Pb11212 near the base of SCS. Suggested affinity: Unknown. GYMNOSPERM.POLLEN Abies-type pollen Plate 4, Figure 8 Size range: Total length: 60 to 100 um. Occurrence: 34 samples, trace to abundant, found throughout all three sections. §pggested affinity: Pinaceae. Comments: Included here are bisaccate pollen grains like those in.Apigg_with comparable size and shape. Some of the larger specflmens are probably conspecific with Abiespollenites sp. of Singh (1971). Reference specimen: slide Pb11602-5, 38.7 X 113.0. 52 GENUS Araucariacites Cookson, 1947 ex Couper, 1953 Type species: Araucariacites australis Cookson, 1947 Araucariacites australis Cookson, 1947 Plate 4, Figure 10 1947 Cookson, p. 130, pl. 13, fig. 1-4. Occurrence: Worldwide distribution in Jurassic, Cretaceous and Tertiary rocks; 30 samples, trace to abundant, found throughout all three sections. Spggested affinity: Araucariaceae. Comments: Couper (1958) points out the similarity of this species to the pollen of the Jurassic araucarian Brachyphyllum.mamillare Brongniart. Araucariacites limbatus (Balme) Habib, 1969 Plate 4, Figure 11 1957 InsperturOpollenites limbatus Balme, p. 31, pl. 7, fig. 83-84. 1969 Araucariacites limbatus (Balme) Habib, p. 91, pl. 4, fig. 6. Occurrence: Cretaceous; 22 samples, trace to occasional, not found in SFTS. Suggested affinity: Araucariaceae. GENUS Callialasporites Dev, 1961 Type species: Callialasporites trilobatus (Balme) Dev, 1961 Callialasporites dampieri (Balme) Dev, 1961 Plate 4, Figure 12 53 1957 Zonalapollenites dampieri Balme, p. 32, pl. 8, fig. 88-90. 1961 CallialaSporites dampieri (Balme) Dev, p. 48, pl. 4, fig. 26, 27. 1961 ApplanOpsis dampieri (Balme) Doring, p. 113, pl. 16, fig. 11-15. 1962 Pflugipollenites dampieri (Balme) Pocock, p. 72, pl. 12, fig. 183, 184. 1963 Tsugaepollenites dampieri (Balme) Dettmann, p. 100, pl. 24, fig. 1-5. Occurrence: Worldwide distribution in Jurassic to Eocene rocks; 2 samples, trace, found only in SCS. Suggested affinity: Gamerro (1965) found pollen similar to CallialaSporites dampieri and g, trilobatus in the male podocarpaceous cone Apterocladus lanceolatus Archangelsky, thus suggesting its affinity to the Podocarpaceae. GENUS Cedripites Wodehouse, 1933 Type species: Cedripites eocenicus Wodehouse, 1933 Cedripites cretaceus Pocock, 1962 Plate 5, Figure 1 1962 Pocock, p. 63, pl. 9, 10, fig. 145-148. Occurrence: Barremian to Albian, see Singh (1971, p. 171); ll samples, trace to common, found in all three sections. Suggested affinity: Pinaceae. GENUS ClassOpollis Pflug, 1953, emend. Pocock and Jansonius, 1961 Type species: Classopollis classoides Pflug, 1953 54 ClassOpollis classoides Pflug, 1953, emend. Pocock and Jansonius, 1961 Plate 5, Figures 2, 3 1953 Classopollis classoides Pflug, p. 91, pl. 16, fig. 29-31. 1961 Clas30pollis classoides Pflug, amend. Pocock and Jansonius, p. 443, 444, pl. 1, fig. 1-9. Occurrence: Worldwide distribution in uppermost Triassic to Eocene rocks; 57 samples, trace to abundant, found throughout all three sections. §pggested affinity: Pollen of the Classspollis type was probably produced by plants of the extinct conifer family Cheirolepidiaceae, consisting of Brachyphyllum, Cheirolepis, Masculostrobus and PagiOphyllum. GENUS Cycadopites Wodehouse, 1933 Type species: Cycadopites follicularis Wilson and Webster, 1946 CycadOpites sp. Plate 5, Figure 4 Description: Monosulcate pollen. Sulcus extending the entire length of the grain and slightly overlapping the entire length on most specimens leaving a uniformly wide sulcus. Exine smooth to very slightly scabrate and about l,nm thick. Ends of grain pointed; length to width ratio of grains from 2 to 3. Sips pspge; Total length (8 specimens): 29(36)40 um. Total width: 11(14)18.um. Occurrence: 41 samples, trace to abundant, found throughout all three sections. 55 Suggested affinity: CycadOphyta or Ginkgophyta. Comments: The non-broadening sulcus of this species distinguishes it from most species in the related genera: Cycadopites, Ginkgo- sycadsphytus and Monosulcites. There is some resemblance to Monosulcites epakros Brenner but the overall shape is different. Monosulcites sp. of Brenner (1963) is also similar but much larger. Reference specimen: slide Pbll609-5, 36.8 X 117.2. GENUS Eucommiidites Erdtman, 1948, emend. Hughes, 1961 Type species: Eucommiidites troedssonii Erdtman, 1948 Eucommiidties minor Groot and Penny, 1960 Plate 5, Figure 5 1960 Groot and Penny, p. 234, pl. 2, fig. 14. Occurrence: Late Jurassic to Albian, see Singh (1971, p. 177); 20 samples, trace to common, found in all three sections. Suggested affinity: Unknown gymnosperm. Comments: Eucommiiditian pollen (Eucommiidites delcourtii) was found in the micrOpylar canal of the Lower Cretaceous gymnospermous seed Spermatites pettensis Hughes by Hughes (1961). Brenner (1963, 1967) has reported pollen similar to E, ping; in the micrOpylar canal and pollen chamber of over 50% of the Lower Cretaceous gymnospermous seeds, Spermatites patuxensis Brenner which he examined from the Patuxent Formation in Virginia. Eucommiidites troedssonii Erdtman, 1948 Plate 5, Figure 6 56 1948 Tricolpites (Eucommiidites) troedssonii, p. 267, test-fig. 5-10, 13-15. Occurrence: Worldwide distribution in Jurassic and Cretaceous rocks; 8 samples, trace to occasional, not found in SFTS. Suggested affinity: Unknown gymnosperm. GENUS Equisetosporites Daugherty, 1941 Type species: EquisetOSporites chinleana Daugherty, 1941 Equisetosporites multicostatus (Brenner) Norris, 1967 Plate 5, Figures 7, 8 1963 Ephedripites multicostatus Brenner, p. 90, pl. 38, fig. 1-20 1967 Eguisetosporites multicostatus (Brenner) Norris, p. 105, pl. 16, fig. 15. Occurrence: Late Barremian to Cenomanian, see Norris (1967, p. 103); 1 sample, trace, found only in Pb11642 near the tap of FCS O Suggested affinity: Ephedraceae. Comments: Although only two specimens from a single sample were encountered, the existence of this family of plants is important in the overall paleofloral picture. GENUS Exesipollenites Balme, 1957 Type species: Exesipollenites tumulus Balme, 1957 Exesipollenites tumulus Balme, 1957 Plate 5, Figure 9 1957 Balme, p. 39, pl. 11, fig. 123-125. 57 Occurrence: Jurassic and Cretaceous, see Singh (1971, p. 178); 7 samples, trace to occasional, not found in FCS. Suggested affinity: Coniferales: possibly Taxaceae, Taxodiaceae or Cupressaceae; Bennettitales (Harris, 1974). GENUS GinkgocyeadOphytus Samoilovitch, 1953 Type species: GinkgocycadOphytus caperatus (Luber) Samoilovitch, 1953 Ginkgosyeadophytus nitidus (Balme) de Jersey, 1962 Plate 5, Figure 10 1957 Entylissa nitidus Balme, p. 30, pl. 6, fig. 78-80. 1962 GinkgesycadOphytus nitidus (Balme) de Jersey, p. 12, pl. 5, fig. 1-3. Occurrence: WOrldwide distribution in Triassic and Cretaceous rocks; 8 samples, trace to rare, found in all three sections. Spggested affinity: Cycadophyta or GinkgOphyta. Comments: This species exhibits some morphological variation but most specimens resemble the holotype (Balme, 1957, pl. 6, fig. 78). Several specimens with slightly expanded ends similar to Brenner's specimens (1963, pl. 25, fig. 3) were encountered. GENUS InaperturOpollenites Pflug, 1952 ex Thomson and Pflug, 1953, emend. Potonie, 1953 Type species: InaperturOpollenites dubius (Potonie and Venitz) Thomson and Pflug, 1953 Comments: Potonie (1966, p. 141) amended the generic description to include more or less laevigate or very weakly and more or less loosely granulate forms that may show numerous secondary folds. 58 This type of pollen grain is abundant in some samples of this study and warranted the counting of additional specimens in these samples to compensate for its "flooding" effect. Initially, an attempt was made to divide the group on the basis of: (1) exine granularity or smoothness, (2) degree of folding and splitting, (3) size and (4) wall thickness. This proved to be totally arbitrary and unsatisfactory except for groupings based on size. Inaperturopollenites sp. 1 Plate 5, Figure 12 Description: Specimens referred to this species form a gradational series from nearly laevigate to distinctly granular forms. Some have split into two nearly equal halves with long folds as well as secondary folds being common. The exine thickness is less than 1 pm. Size range: Diameter ranges from 19 nm to about 60,um with an average of about 20-25.um. Occurrence: Similar forms have worldwide distribution in Jurassic, Cretaceous and Tertiary rocks; 62 samples, common to flooding, found in all samples. Spggested affinity: Taxodiaceae, Cupressaceae and/or Taxaceae; possibly some affinity with Araucariaceae also. Comments: This species is probably conspecific in part with Inaperturopollenites dubius and Taxodiaceaepollenites hiatus and may include a whole complex of plants belonging to the Taxodiaceae and Cupressaceae (Groot and Penny, 1968). The characteristic splitting of many specimens and overall morphology are very similar 59 to modern Taxodium. Reference specimen: slide Pb11642-6, 37.7 X 127.0. InaperturOpollenites sp. 2 Plate 5, Figures 13, 14 Description: Specimens referred to this species are identical to InaperturOpollenites sp. 1 except that the size range is smaller. Sise_pspge: Diameter ranges from about 10 to 18.nm. Occurrence: Similar forms have worldwide distribution in Jurassic, Cretaceous and Tertiary rocks; 59 samples, rare to flooding, found in nearly all samples. Suggested affinity: Taxodiaceae, Cupressaceae and/or Taxaceae. Reference specimen: slide Pb11642-6, 43.9 X 118.5. Inaperturspollenites sp. 3 Plate 5, Figure 11 1967 Inaperturopollenites sp. Norris, p. 104, pl. 16, fig. 8. 1971 InaperturOpollenites sp. of Norris: Singh, p. 150, pl. 21, fig. 1. Description: see Norris (1967, p. 104). Occurrence: Triassic and Lower Cretaceous of various parts of the world, see Norris (1967, p. 104); 12 samples, rare to common, not found in SFTS. Suggested affinity: Unknown gymnosperm 7 Reference specimen: slide Pb11202-1, 44.3 X 122.0. 60 GENUS Laricoidites Potonie, Thomson and Thiergart, 1950 ex Potonie, 1958 Type species: Laricoidites magnus (Potonie) Potonie, Thomson and Thiergart, 1950 Comments: Laricoidites has been artificially separated from InaperturOpollenites on the basis of its larger size (Brenner, 1963). Laricoidites gigantus Brenner, 1963 Plate 5, Figure 16 1963 Brenner, p. 88, pl. 36, fig. 1, 2. Occurrence: 5 samples, trace to rare, not found in FCS. Suggested affinity: Pinaceae ? Comments: Pollerxhere assigned are similar to pollen of modern Larix. Laricoidites magpus (Potonie) Potonie, Thomson and Thiergart, 1950 Plate 5, Figure 15 1931 Sporites (?) magnus Potonie, p. 566, fig. 6. 1950 Laricoidites magnus (Potonie) Potonie, Thomson and Thiergart, p. 48, p1. C, fig. 9, 10. gypppygy: see Stanley (1965, p. 278). Occurrence: Similar forms have worldwide distribution in Cretaceous and Tertiary rocks; 9 samples, trace to occasional, not found in SCS. Suggested affinity: Pinaceae 7 Comments: Pollen here assigned are similar to pollen of modern Larix. This species is similar to Laricoidites gigantus but has a smaller size of about 60 to 90.nm. 61 GENUS Monosulcites Cookson ex Couper, 1953 Type species: Monosulcites minima Cookson, 1947 Monosulcites sp. Plate 5, Figures 17, 18 Description: Monosulcate pollen. Sulcus 3/4 of total length and bordered by lips less than 1 um wide; outline oval with broadly rounded ends. Exine less than 1 nm.thick and very finely scabrate. Sulcus slightly opened and straight sided. Size range: Total length (6 specimens): 11(12)14 um. Total width: 7(8)10.nm. Occurrence: 26 samples, rare to common, found in all three sections. Suggested affinity: CycadoPhyta or GinkgOphyta. Comments: Specimens assigned to this species are smaller than any previously described in the related genera: CycadOpites, Ginkgocycadophytus and Monosulcites. Reference specimen: slide Pb11642-6, 38.7 X 117.3. GENUS Perinopollenites Couper, 1958 Type species: PerinOpollenites elatoides Couper, 1958 PerinOpollenites sp. cf. P, elatoides Couper, 1958 Plate 5, Figure 19 cf. 1958 PerinOpollenites elatoides Couper, p. 152, pl. 27, fig. 9-11. Description: see Pocock (1962, p. 60); this species differs from Perinopollenites elatoides Couper only by its significantly smaller size. The size range of P, elatoides as reported from 62 previous studies is from 38 to 54,um. Size range: Equatorial diameter of perispore (8 specimens): 20(27)37 um. Equatorial diameter of central body: 14(21)32.um. Occurrence: 33 samples, rare to abundant, found in all three sections. §pggested affinity: Taxodiaceae. Comments: This species is undoubtedly closely related or con- specific with PerinOpollenites elatoides. Couper (1958) concluded that the pollen of this type belongs to Elatides williamsonii of the Taxodiaceae. Reference specimen: slide Pb11216-5, 38.1 X 117.2. GENUS Phyllocladidites Cookson, 1947 ex Couper, 1953 Type species: Phyllocladidites mawsonii Cookson, 1947 Phyllocladidites sp. Plate 5, Figure 20 1964 Phyllocladidites sp. Singh, p. 114, pl. 15, fig. 10. 1971 Phyllocladidites sp. of Singh: Singh, p. 161, pl. 22, fig. 12. Description: see Singh (1964, p. 114). Occurrence: Middle and late Albian of central and northwestern Alberta; 3 samples, trace to rare, found only near the base of FCS. Suggested affinity: Podocarpaceae. Comments: Singh (1964) points out the similarity of pollen in Phyllocladidites to Dacrydium. 63 Reference specimen: slide Pb11602-1, 44.8 X 118.4. Pipps_- Pipes-type pollen Plate 6, Figure 1 Size range: Total length: about 50 to 110,um. Occurrence: 57 samples, trace to abundant, found throughout all three sections. Suggested affinity: Pinaceae. Comments: Included here are bisaccate pollen grains similar in size and shape with those in 22222 and Pipes, This group also includes several species of pollen assignable to AliSporites which, according to Rouse (1959) has probable affinity with Pinaceae. Reference specimen: slide Pb11238-l, 46.8 X 118.6. Large Podocarpus-type pollen Plate 6, Figure 2 Size range: Total length: 80 to 120 um. Occurrence: 21 samples, trace to coumon, found in all three sections. Suggested affinity: Podocarpaceae. Comments: Included here are bisaccate pollen grains similar in shape to those in Podocsrpus with the size limitations indicated above. Reference specimen: slide Pb11609-l, 42.6 X 118.0. Small Podocarpus-type pollen Plate 6, Figure 3 Size range: Total length: 45 to 80 um. 64 Occurrence: 18 samples, trace to common, found in all three sections. Spggssted affinity: Podocarpaceae. Comments: Included here are bisaccate pollen grains similar in shape to those in Podocarpus with the size limitations indicated above. Reference specimen: slide Pb11232-5, 32.5 X 121.9. GENUS Rugubivesiculites Pierce, 1961 Type species: Rugubivesiculites convolutus Pierce, 1961 Rugubivesiculites rugosus Pierce, 1961 Plate 6, Figure 4, 5 1961 Pierce, p. 40, pl. 2, fig. 59, 60. Occurrence: Late Albian and Cenomanian, see Singh (1971, p. 167); 6 samples, rare, not found in SFTS. Spggested affinity: Podocarpaceae. Comments: Pierce (1961) points out the similarity of some Dacrydium pollen to those in Rugubivesiculites. GENUS Vitreisporites Leschik, 1955, emend. Jansonius, 1962 Type species: Vitreisporites signatus Leschik, 1955 Vitreisporites pallidus (Reissinger) Nilsson, 1958 Plate 6, Figure 6 1938 Pityosporites psllidus Reissinger, p. 14 (not figured). 1950 Pityosporites pallidus Reissinger, p. 109, pl. 15, fig. 1-5. 1958 Vitreisporites pallidus (Reissinger) Nilsson, p. 78, pl. 7, fig. 12-14. 65 gypppypy: see Norris (1967, p. 100). Occurrence: Worldwide distribution in Triassic to Cretaceous rocks; 21 samples, trace to common, found in all three sections. Suggested affinity: Caytoniaceae. ANGIOSPERM POLLEN (Monosulcate) GENUS Clavatipollenites Couper, 1958 Type species: Clavatipollenites hughesii Couper, 1958 Clavatipollenites minutus Brenner, 1963 Plate 6, Figure 7 1963 Brenner, p. 95, pl. 41, fig. 8, 9. Occurrence: Barremian to Albian, see Singh (1971, p. 182); 19 samples, trace to common, found in all three sections. Suggested affinity: Gymnospermous or angiospermous, see Kemp (1968). GENUS Liliacidites Couper, 1953 Type species: Liliacidites kaitssgataensis Couper, 1953 Liliacidites dividuus (Pierce) Brenner, 1963 Plate 6, Figure 8 1961 Retimonocolpites dividuus Pierce, p. 47, pl. 3, fig. 87. 1963 Liliacidites dividuus (Pierce) Brenner, p. 93, pl. 40, fig. 7-10. Occurrence: Albian and Cenomanian, see Singh (1971, p. 185); 14 samples, trace to common, not found in SFTS. 66 Suggested affinity: Monocotyledoneae. Liliacidites peroreticulatus (Brenner) Singh, 1971 Plate 6, Figures 9, 10 1963 Peromonolites peroreticulatus Brenner, p. 94, pl. 41, fig. 1, 2. 1971 Liliacidites peroreticulatus (Brenner) Singh, p. 188, pl. 28, fig. 6-11. Occurrence: Barremian to early Cenomanian, see Singh (1971, p. 188); 8 samples, rare to common, not found in SFTS. Suggested affinity: Monocotyledoneae. Liliacidites textus Norris, 1967 Plate 6, Figures 11, 12 1967 Norris, p. 106, pl. 16, fig. 21-25; pl. 17, fig. 1, 2. Occurrence: Late Albian of central and northwestern Alberta; 11 samples, trace to occasional, not found in SFTS. Suggested affinity: Monocotyledoneae. ANGIOSPERM.POLLEN (Tricolpate) GENUS Cupuliferoidaepollenites Potonie, Thomson and Thiergart, 1950 Type species: Cupuliferoidaepollenites liblarensis Thomson i2 Potonie, Thomson and Thiergart, 1950 Cupuliferoidaepollenites minutus (Brenner) Singh, 1971 Plate 6, Figures 13, 14 1963 Tricolpopsllenites minutus Brenner, p. 93, pl. 40, fig. 5, 6. 67 1967 Cornaceoipollenites minutus (Brenner) Norris, p. 107, pl. 17, fig. 7-11. 1971 Cupuliferoidaepollenites minutus (Brenner) Singh, p. 194, pl. 29, fig. 8, 9. Occurrence: Albian and early Cenomanian, see Singh (1971, p. 194); 15 samples, trace to common, found in all three sections. Suggested affinity: Dicotyledoneae. GENUS Psilatricolpites van der Hammen, 1956 Type species: Psilatricolpites incomptus van der Hammen, 1956 Psilatricolpites parvulus (Groot and Penny) Norris, 1967 Plate 6, Figures 15-17 1960 TricolpOpollesites parvulus Groot and Penny, p. 232, pl. 2, fig. 8, 9. 1967 Psilatricolpites parvulus (Groot and Penny) Norris, p. 107, pl. 17, fig. 5, 6. Occurrence: Late Albian to Danian, see Singh (1971, p. 198); 37 samples, trace to abundant, found in all three sections. Suggested affinity: Dicotyledoneae. Psilatricolpites sp. Plate 6, Figure 18 Description: Tricolpate pollen; ratio of polar to equatorial diameter about 1.5. Colpi closed, slit-like and extending nearly to the poles. Exine smooth or very slightly roughened. Sips pspgs: Polar diameter (8 specimens in equatorial view): 20(23)26 um. Equatorial diameter: 10(15)17 um. Occurrence: 9 samples, rare to common, found only in SCS. 68 Suggested affinity: Dicotyledoneae. Comments: The specimens assigned to this species somewhat resemble Psilatricolpites psilatus Pierce but differ by having closed colpi and slightly more elongate shape. Reference specimen: slide Pb11212-2, 42.0 X 119.5. GENUS Retitricolpites van der Hammen, 1956 ex Pierce, 1961 Type species: Retitricolpites ornatus van der Hammen, 1956 Retitricolpites georgsnsis Brenner, 1963 Plate 6, Figures 20, 21 1963 Brenner, p. 91, pl. 38, fig. 6, 7. Occurrence: Albian to early Cenomanian, see Singh (1971, p. 200); 11 samples, trace to occasional, found only in SCS. §pggested affinity: Dicotyledoneae. Comments: This species is characterized by the reduction in size of the lumdna toward the poles. Retitricolpites prosimilis Norris, 1967 Plate 6, Figure 22, 23 1967 Norris, p. 108, pl. 18, fig. 5-14. Occurrence: ‘Middle and late Albian, see Singh (1971, p. 202); 13 samples, trace to abundant, found in all three sections. Suggested affinity: Dicotyledoneae. Retitricolpites vulgaris Pierce, 1961 Plate 6, Figures 25, 26 1961 Pierce, p. 50, pl. 3, fig. 101, 102. 69 Occurrence: Middle Albian to Maestrichtian, see Srivastava (1975, p. 103); 47 samples, trace to abundant, found throughout all three sections. §pggested affinity: Dicotyledoneae. Comments: Srivastava has placed specimens of this species from the Maestrichtian of Alberta in the genus Tricolpites (1969, p. 57). He has concluded from examination by both the Optical and scanning electron microsc0pe that the exine is infratectate and not intectate as Pierce (1961), Norris (1967) and Singh (1971) had described. The designation R. vulgaris Pierce is used here to conform to nomenclatural practice in other Lower Cretaceous studies. GENUS StriatOpollis Xrutzsch, 1959 Type Species: Striatopollis sarstedtensis Krutzsch, 1959 StriatOpollis paraneus (Norris) Singh, 1971 Plate 6, Figure 24 1967 Retitricolpites paraneus Norris, p. 109, pl. 18, fig. 15- 20. 1971 StriatOpollis paraneus (Norris) Singh, 1971, p. 206, pl. 32, fig. 1- 3. Occurrence: Middle and late Albian, see Singh (1971, p. 206); 3 samples, rare, found only at the base of SCS and the tap of FCS. Suggested affinity: Dicotyledoneae. GENUS Tricolpites Cookson, 1947 ex Couper, 1953, emend. Potonie, 1960 Type species: Tricolpites reticulatus Cookson, 1947 70 Tricolpites crassimurus (Groot and Penny) Singh, 1971 Plate 6, Figure 27 1960 Tricolpgpollenites crassimurus Groot and Penny, p. 232, pl. 2, fig. 4, 5. 1971 Tricolpites crassimurus (Groot and Penny) Singh, p. 207, pl. 32, fig. 4-6. Occurrence: Albian to Coniacian, see Singh (1971, p. 207); 19 samples, trace to occasional, found throughout all three sections. Suggested affinity: Dicotyledoneae. Tricolpites micromunus (Groot and Penny) Singh, 1971 Plate 6, Figure 28 1960 Tricolpspollenites micromunus Groot and Penny, p. 232, pl. 2, fig. 6, 7. 1971 Tricolpites micromunus (Groot and Penny) Singh, p. 209, pl. 32, fig. 7-11. Occurrence: Albian to Danian, see Singh (1971, p. 209); 5 samples, trace to comon, found near the base of SCS and the tap of FCS. Suggested affinity: Dicotyledoneae. Tricolpites sp. Plate 6, Figure 29 Description: Tricolpate pollen; oblate to spherical. Amb trilobate with gaping, V-shaped colpi almost reaching the poles. Exine thin and smooth to very slightly scabrate. Sise_£spgs: Equatorial diameter (8 specimens): ll(l4)l8,nm. Occurrence: 9 samples, trace to occasional, not found in SFTS. Suggested affiniyy: Dicotyledoneae. Comments: Specimens assigned to this species somewhat resemble Tricolpites sp. B of Hopkins (1974, p. 24) from the ChristOpher 71 Formation (Albian) of the Canadian.Arctic Archipelago. Reference specimen: slide Pb11205-1, 33.9 X 117.9. ANGIOSPERM POLLEN (Tricolporate) GENUS Nyssapollenites Thiergart, 1937 Type species: Nyssapollenites pseudocruciatus (Potonie) Thiergart, 1937 Nyssapollenites albertensis Singh, 1971 Plate 6, Figure 19 1971 Singh, p. 213, pl. 32, fig. 20, 21. Occurrence: Late Albian and early Cenomanian, see Singh (1971, p. 213); 11 samples, trace to common, not found in SFTS. Suggested affinity: Dicotyledoneae. Comments: Singh accepts the genus Nyssapgllenites as a form genus only, with no botanical affinities implied. ANGIOSPERM.POLLEN (Incertae Sedis) GENUS Asterspollis Hedlund and Norris, 1968 Type species: Asteropollis asteroides Hedlund and Norris, 1968 AsterOpollis asteroides Hedlund and Norris, 1968 Plate 7, Figures 1-3 1968 Hedlund and Norris, p. 153, pl. 6, fig. 18-20; pl. 7, fig. 1-5. Occurrence: ? Middle Albian to Turonian, see Srivastava (1975, 72 p. 86); 22 samples, trace to abundant, not found in SFTS. Spggested affinity: Unknown angiosperm. Comments: Specimens assigned by Davis (1963, p. 123, unpublished thesis) to "Genus A, sp. A" are probably conspecific with Asteropollis asteroides. Class DINOPHYCEAE Pascher Family APTEODINIACEAE Eisenack, 1961, emend. Sarjeant and Downie, 1974 GENUS Spinidinium Cookson and Eisenack, 1962 Type species: Spinidinium styloniferum Cookson and Eisenack, 1962 Spinidinium vestitum Brideaux, 1971 Plate 7, Figure 4 1970 Deflandrea cf. echinoidea Cookson and Eisenack: Davey, p. 339, pl. 1, fig. 6; pl. 2, fig. 2. 1971 Spinidinium vestitum Brideaux, p. 99, pl. 29, fig. 99-103, text-fig. 10a, d. 1971 Deflandrea limpida Singh, p. 359, pl. 61, fig. 1, 2. 1974 Deflandrea echinoidea Cookson and Eisenack, 1960, emend. Sverdlove and Habib, p. 58, pl. 1, fig. 1-6, text-fig. 2a, b. Occurrence: Late Albian to early Cenomanian, see Brideaux (1971, p. 101); 12 samples, trace to flooding, not found in SFTS. Comments: This species is quite variable in size and reaches prolific abundance near the base of the FCS. The attempt to transfer this species to Deflandrea by Sverdlove and Habib (1974) was rejected by Lentin and Williams (1975). 73 Family CTENIDODINIACEAE Sarjeant and Downie, 1966, emend. Sarjeant and Downie, 1974 GENUS DinOpteryginm Deflandre, 1935 Type species: Dinopterygium cladoides Deflandre, 1935 DinOpterygium 8p. A Plate 7, Figure 5 1971 DinOpterygium.sp. A Brideaux, p. 97, pl. 28, fig. 89-92. Description: see Brideaux (1971, p. 97). Sips gspgs: Equatorial width including equatorial ledges (3 specimens) : 60(65) 70 um . Occurrence: Late Albian of central Alberta; 2 samples, trace to rare, found only in FCS. Comments: The several specimens observed appear to be conspecific with Brideaux's Species. The apical horn and sulcal area are visible on the illustrated specimen. No recognizable archeOpyle structure was observed. Reference specimen: slide Pb11642-6, 34.6 X 123.8. Family SPINIFERITACEAE Sarjeant, 1970, emend. Sarjeant and Downie, 1974 GENUS Spiniferites Mantell, 1850, emend. Sarjeant, 1970 Type species: Spiniferites ramosus Ehrenberg, 1838 Spiniferites sp. cf. S, cingulatus (O. Wetzel) Sarjeant, 1970 Plate 7, Figure 6 74 cf. 1933 Qymatiosphaera cingulata O. wetzel, p. 28, pl. 4, fig. 10. cf. 1955 Hystrichosphaera cingulata (O. Wetzel) Deflandre and Cookson, p. 267, pl. 6, fig. 4, 5. cf. 1970 Spiniferites cingulatus (O. Wetzel) Sarjeant, p. 76. Description: Central body not always distinct but ovoid to spherical when visible. Tabulation superficially resembling S, cingulatus but no clear cingulum observed. Crests dentate and supported by gonal processes not extending beyond crests. Wall of central body smooth to very finely granulate. Size range: Maximum dimension of cyst including crests (3 specimens): 45(54)59 um. Height of crests: 2 to 7.nm. Occurrence: 3 samples, rare, found only near the base of FCS. Comments: The small number of specimens encountered allow only a tentative assignment of this species. This species differs from S. cingulatus in Singh (1971, p. 351) by having more highly dentate crests between processes. S, cingulatus has been subdivided by some authors into a number of varieties having some stratigraphic significance. Reference specimen: slide Pb11607-1, 35.2 X 120.6. Family PAREODINIACEAE Gocht, 1957, emend. Sarjeant and Downie, 1974 GENUS Pareodinia Deflandre, 1947, emend. Wiggins, 1975 Type species: Pareodinia ceratophora Deflandre, 1947, emend. Gocht, 1970 75 Pareodinia sp. cf. 2, ceratOphora Deflandre, 1947, emend. Gocht, 1970 Plate 7, Figure 7 cf. 1947 Pareodinia ceratophora Deflandre, p. 4, text-fig. 1-3. Description: see Singh (1971, p. 313). Size range: Total length of cyst (3 specimens): 68(70)71,um. Total width of cyst: 34(37)40.um. Occurrence: 1 sample, rare, found near the base of FCS. Comments: Only three Specimens of this species were encountered making its taxonomic assignment tentative although it closely resembles Pareodinia ceratophora. The illustrated specimen shows a hint of breakage suggesting an intercalary archeOpyle. Reference specimen: slide Pb11610-l, 35.0 X 122.1. Family DEFLANDREACEAE Eisenack, 1954, emend. Sarjeant and Downie, 1974 GENUS Deflandrea Eisenack, 1938, emend. Lentin and Williams, 1977 Type species: Deflandrea phosphoritica Eisenack, 1938 Deflandrea sp. 1 Plate 7, Figure 8 Description: Epicyst roughly triangular with apical horn having straight or concave sides and forming a slender point; hypocyst roughly symmetrical with one antapical horn centrally placed or less commonly slightly to one side, apex of antapical horn blunt or rounded. EndOphragm spherical or ovoid and usually slightly off center in the periphragm. 76 Siss_pspgs: Total length of cyst (8 specimens): 70(80)90,um. Total width of cyst: 35(40)49 um. Occurrence: 5 samples, rare to common, found only near the base of FCS. Comments: One of the Specimens illustrated by Davis (1963, pl. 10, fig. 7) as Deflandrea sp. B may be conspecific with 2, sp. 1 of this study if it were rotated 180°. Reference specimen: Slide Pb11618-l, 32.1 X 122.8. Deflandrea Sp. 2 Plate 7, Figures 9, 10 Description: Epicyst roughly triangular with apical horn having straight sides and coming to a sharp point when not broken; hypo- cyst strongly asymmetrical with one longer horn coming to a rounded point while the Shorter horn is little more than a slight protuberance on the opposite side. EndOphragm slightly ovoid with its long diameter parallel to the cingulum and slightly off center in the periphragm. Sise_pspgs: Total length of cyst (7 specimens): 60(66)75.um. Total width of cyst: 38(40)43,um. Occurrence: 2 samples, occasional to common, found only near the base of FCS. Comments: The asymmetrical nature of the hypocyst of this Species makes it easily identifiable and differentiatable from Deflandrea sp. 1. Reference Specimen: slide Pb11618-1, 40.0 X 125.8. 77 Family PALAEOPERIDINIACEAE Vozzhennikova, 1961, emend. Sarjeant, 1967 GENUS Palanperidinium Deflandre, 1934, emend. Sarjeant, 1967 Type Species: Palaesperidinium pyrophorum (Ehrenberg) Sarjeant, 1967 Palaereridinium cretaceum Pocock, 1962 Plate 8, Figures 1, 2 1962 Pocock, p. 80, pl. 14, fig. 219-221. Size range: Total length of cyst (5 Specimens): 64(75)86 pm, Total width of cyst: 49(57)60,um. Occurrence: Cretaceous, see Singh (1971, p. 385); 6 samples, rare to abundant, found only near the base of FCS. Comments: This species has been treated differently by various authors. S, cretaceum is the type of the genus Astrocysta Davey, 1970, which is considered to be a junior synonym of Palaeoperidinium Deflandre, emend. Sarjeant by Lentin and Williams (1975, p. 110). It has also been placed in Lejeunia by Brideaux (1971, p. 86). Family HEXAGONIFERACEAE Sarjeant and Downie, 1966, emend. Sarjeant and Downie, 1974 GENUS Hexagonifera Cookson and Eisenack, 1961, emend. Cookson and Eisenack, 1962 Type species: Hexagonifera glabra Cookson and Eisenack, 1961 Hexagonifera Sp. cf. S, chlamydata Cookson and Eisenack, 1962 Plate 8, Figure 3 cf. 1962 Hexagonifera chlamydata Cookson and Eisenack, p. 496, 78 pl. 7, fig. 1-3, 5—8. Description: see Cookson and Eisenack (1962, p. 496). Occurrence: 2 samples, trace, found only near the base of FCS. Comments: Only three Specimens of this Species were encountered allowing only a tentative taxonomic placement. The only well- preserved specimen lacked the archeopyle and had the characteristic size, outer membrane and verrucose inner body surface sculpture of Hexsggnifera chlamydata. Lentin and Williams (1976, p. 84) questionably retained S, chlamydata in Hessgonifera in Spite of its apparent apical archeOpyle, pending reexamination of the type material. Reference specimen: slide Pb11642-6, 33.4 X 127.4. Family PSEUDOCERATIACEAE Eisenack, 1961, emend. Sarjeant and Downie, 1966 GENUS Odontochitina Deflandre, 1935, emend. Davey, 1970 Type species: Odontochitina sperculata (O. Wetzel) Deflandre and Cookson, 1955 Odontochitina costata Alberti, 1961, emend. Clarke and Verdier, 1967 Plate 8, Figure 4 1961 Odontochitina costata Alberti, p. 31, pl. 6, fig. 10-13. Sypgpypy: see Clarke and Verdier (1967, p. 58). Occurrence: Albian to Cenomanian, see Davey and Verdier (1973, p. 198); 3 samples, trace, found only near the base and middle of FCS. Comments: Singh (1971, p. 372) considers Q, costata Alberti and 79 Q. striatOperforata Cookson and Eisenack as distinct Species contrary to the emendation of Clarke and Verdier (1967). Only one complete specimen was encountered in this study along with several apical and antapical halves. GENUS Pseudoceratium Gocht, 1957 Type species: Pseudoceratium pelliferum Gocht, 1957 Pseudoceratium ? Sp. Plate 8, Figures 5, 6 Description: Cyst flattened; asymmetrical outline with two prominent horns. Apical born with rounded or blunt point and slightly convex or Straight sides. Antapical horn drawn to a long slender point and set to extreme side of hypocyst. Second antapical horn not deve10ped but suggested by broad bulge on Opposite Side of hypocyst. ArcheOpyle apical; paratabulation absent. The cyst wall is patterned with an irregular reticulum having no apparent relief. ‘Siss.pspgs: Total length of cyst (4 Specimens): 103(111)126,nm. Total width of cyst: 41(43)47.um. Occurrence: 3 samples, trace to rare, found only in SFTS. Comments: This species was tentatively placed in the genus Pseudoceratium because it lacks a distinct second antapical horn. Only several complete Specimens were encountered in the study allowing little chance for comparison. Reference specimen: slide Pb11681-l, 37.1 X 119.8. 80 Family MUDERONGIACEAE Neale and Sarjeant, 1962, emend. Sarjeant and Downie, 1966 GENUS Muderongia Cookson and Eisenack, 1958 Type species: Muderongia mcwhaei Cookson and Eisenack, 1958 Muderongia Sp. 1 Plate 8, Figures 7, 10 Description: Cyst flattened; roughly bilaterally symmetrical with one apical, two lateral and two antapical horns. Apical horn slightly longer and broader than the other four. Two lateral horns about equal in length and postcingular in position. Antapical horns equal in length or only slightly unequal and within the same length and width range as the lateral horns. Endocyst not clearly defined. Periphragm surface smooth or faintly roughened. Paratabulation and paracingulum faintly suggested on some Specimens. ArcheOpyle apical. Size range: Total length of cyst (6 Specimens): 119(130)144 um. Total width of cyst: 83(98)110,nm. Length of apical horn: 43(48)50.um. Length of lateral and antapical horns: 29(34)50 pm, Occurrence: 7 samples, rare to dominant, found only in SFTS and uppermost Bear River Formation in FCS. Comments: This Species is distinguished from Muderongia asymmetrica Brideaux, 1977, which exhibits the pairing of long left antapical and short right postcingular horns and Short right antapical and long left postcingular horns. "Pseudoceratium Sp A" of Davis (1963, unpublished thesis) is distinguished by its shorter and 81 broader horns and appears to be conSpecific with Muderongia Sp. 2 of this study. Reference specimen: slide Pb11681-1, 37.8 X 124.4. Muderongia Sp. 2 Plate 8, Figures 8, 9 1963 "Pseudoceratium sp. A", Davis, p. 130, pl. 10, fig. 9-12 (unpublished thesis). Description: Cyst flattened; roughly bilaterally symmetrical with one apical, two lateral and two antapical horns. Apical horn broadly triangular and Sharply pointed with a slightly longer length than the other four horns. Two lateral and two antapical horns broadly based and about equal in size and shape with sharp points. Endocyst not clearly defined. Periphragm surface smooth or faintly roughened. Paratabulation, paracingulum and archeOpyle not observed. Siss_£spgs: Total length of cyst (8 specimens): 75(87)100,um. Total width of cyst: 61(69)75 um, Length of apical horn: 25(27)31.nm. Length of lateral and antapical horns: 16(21)25 um. Occurrence: Middle to late Albian of northern Wyoming (Davis, 1963); 2 samples, rare to dominant, found only in the uppermost SFTS. Comments: This species appears to be conspecific with "Pseudoceratium Sp. A" of Davis (1963, unpublished thesis) differing only by having a slightly smaller overall size. It differs from Muderongia asymmetrica Brideaux which does not have lateral and antapical horns of equal length. This Species is usually folded or broken 82 with the horns folded over the body. Reference specimen: Slide Pb11687-5, 29.3 X 125.5. Family MEMBRANILARNACIACEAE Eisenack, 1963, emend. Sarjeant and Downie, 1966 GENUS ChlamydOphorella Cookson and Eisenack, 1958 Type Species: Chlamydophorella nyei Cookson and Eisenack, 1958 ChlamydOphorella nyei Cookson and Eisenack, 1958 Plate 9, Figure 1 1958 Cookson and Eisenack, p. 56, pl. 11, fig. 1-3. Occurrence: Aptian to early Turonian, see Singh (1971, p. 377); 2 samples, rare to occasional, found only in FCS. Family HYSTRICHOSPHAERIDIACEAE Evitt, 1963, emend. Sarjeant and Downie, 1974 GENUS Oligosphaeridium Davey and Williams, 1966 Type species: Oligosphaeridium complex (White) Davey and Williams, 1966 Oligpsphaeridium anthOphorum (Cookson and Eisenack) Davey, 1966 Plate 9, Figure 2 1958 Hystrichosphaeridium anthophorum Cookson and Eisenack, p. 43, pl. 11, fig. 12, 13. 1969 Oligosphaeridium anthophorum (Cookson and Eisenack) Davey, p. 147, pl. 5, fig. 1-3. Occurrence: Late Jurassic to Albian, see Singh (1971, p. 336); 2 samples, trace to rare, found only near the base of FCS. 83 Oligosphaeridium complex (White) Davey and Williams, 1966 Plate 9, Figures 3, 4 1842 Xanthidium tubiferum complex White, p. 39, pl. 4, div. 3, fig. 11. 1946 HystrichOSphaeridium complex (White) Deflandre, p. 111. 1966 Oligosphaeridium complex (White) Davey and Williams, p. 71, pl. 7, fig. 1, 2; pl. 10, fig. 3, text-fig. 14. Occurrence: Valanginian to early Eocene, see Singh (1971, p. 334); 12 samples, rare to common, not found in SFTS. GENUS TanyOSphaeridium Davey and Williams, 1966 Type Species: Tanyosphaeridium variecalamum Davey and Williams, 1966 Tanyosphaeridium sp. A Plate 9, Figure 5 1971 Tanyosphaeridium sp. A Brideaux, p. 93, pl. 26, fig. 71. 1971 TanyOSphaeridium sp. Singh, p. 344, pl. 57, fig. 7. 1975 TanyoSphaeridium sp. A of Brideaux: Brideaux, p. 31, pl. 9, fig. 11. Description: see Brideaux (1971, p. 93) and Brideaux (1975, p. 31). Occurrence: Middle and late Albian of central and west-central Alberta and Horton River area (Brideaux, 1971; Singh, 1971; Brideaux and.McIntyre, 1975); 4 samples, rare to occasional, not found in SFTS. Comments: This species is distinguished by processes with Open and flared ends. Norvick (1975, p. 63) describes a new Species, Tanyosphaeridium salpinx, with Similar processes which he considers 84 as conSpecific with T, Sp. of Singh, 1971. The Specimens illustrated by Singh and Brideaux and those encountered in this study Show little variation in number of processes and have a more elongate cyst outline than Norvick's illustrated specimen (he does not include length to width ratios for comparison). For these reasons Tspyg- sphaeridium Sp. A is not considered conspecific with T, salpinx Norvick pending further study. Reference Specimen: slide Pb11618-l, 39.0 X 126.2. Family CLEISTOSPHAERIDIACEAE Sarjeant and Downie, 1974 GENUS CleistOSphaeridium Davey and others, 1966 Type species: Cleistosphaeridium diverSiSpinosus Davey and others, 1966 Cleistosphaeridium multispinosus (Singh) Brideaux, 1971 Plate 9, Figure 6 1964 Baltisphaeridium multiSpinosus Singh, p. 141, pl. 20, fig. 1, 2. 1971 Cleistosphaeridium multispinosus (Singh) Brideaux, p. 93, pl. 27, fig. 77-79. Occurrence: Middle Albian to early Cenomanian, see Brideaux (1971, p. 94); 25 samples, trace to dominant, found throughout all three sections. Family AREOLIGERACEAE Evitt, 1963, emend. Sarjeant and Downie, 1966 GENUS delonephelium Deflandre and Cookson, 1955, emend. Ioannides and others, 1977 85 Type species: chlonephelium compactum Deflandre and Cookson, 1955 Cyelonephelium Sp. A Plate 9, Figure 7 1971 Cyclonephelium Sp. A Brideaux, p. 97, pl. 28, fig. 88. Occurrence: Late Albian of central Alberta, see Brideaux (1971, p. 97); 7 samples, trace to abundant, found only near the base of FCS. Comments: Complete Specimens were not observed but the remaining cyst falls within the circumscription of this genus and the description of Cyclonephelium Sp. A of Brideaux. Reference Specimen: slide Pb11618-1, 42.8 X 115.7. Group ACRITARCHA Evitt, 1963 Subgroup ACANTHOMDRPHITAE Downie, Evitt and Sarjeant, 1963 GENUS Baltisphaeridium Eisenack, 1958, emend. Downie and Sarjeant, 1963 Type Species: Baltisphaeridium longispinosum (Eisenack) Eisenack, 1958 Baltisphaeridium sp. Plate 9, Figures 8, 9 Description: Body Spherical to ovoid, thin walled and densely covered with short spines distributed over the entire surface; processes of approximately equal length, never longer than 1.5 nm and with pointed, blunt or less commonly capitate tips. 86 Spines Spaced about 1 to 1.5 mm apart. Body not uncommonly slightly folded and/or broken. Size range: Total diameter of test with spines (15 Specimens): 18(23)26 um. Occurrence: 9 samples, trace to dominant, not found in SFTS. Comments: This species falls within the circumscription of Downie and Sarjeant's emendation of the genus Baltisphaeridium Eisenack. Although a few Specimens are smaller than their arbitrary 20 ,um limit the mean diameter is 23 um. Reference Specimen: Slide Pb11210-2, 40.5 X 119.3. GENUS Micrhystridium Deflandre, 1937, emend. Downie and Sarjeant, 1963 Type Species: Micrhystridium inconSpicuum (Deflandre) Deflandre, 1937 Micrhystridium bifidum Davey, 1970 Plate 9, Figures 10, 11 1970 Davey, p. 368, pl. 7, fig. 10, 11, text-fig. 2L. Occurrence: Cenomanian of England; 11 samples, rare to dominant, found in all three sections. Comments: Specimens assigned to this Species compare favorably in all aspects with those of Davey. Micrhystridium fragile Deflandre, 1947 Plate 9, Figure 12 1947 Deflandre, p. 8, fig. 13-18. Description: see Singh (1971, p. 399). Occurrence: Jurassic to Oligocene in various parts of the world, 87 see Drugg (1967, p. 34); 2 samples, rare, found only near the base of FCS. Comments: The few specimens assigned to this species fall well within the variable size range and spine number of this species reported in the literature. Micrhystridium inconspicuum (Deflandre) Deflandre, 1937 Plate 10, Figures 1, 2 1935 Hystrichosphaera inconspicua Deflandre, p. 233, pl. 9, fig. 11, 12. 1937 'Micrhystridium inconspicuum (Deflandre) Deflandre, p. 32, pl. 12, fig. 11-13. Occurrence: Oxfordian to Senonian, western EurOpe and northern Wyoming (Davis, 1963, unpublished thesis); 39 samples, rare to flooding, found throughout all three sections. Comments: Specimens assigned to this Species are comparable to those illustrated in drawings by Davis (1963, pl. 13, fig. 3, 8) in the upper Albian of northern Wyoming. Micrhystridium sp. cf. s. densispinium Valensi, 1953 Plate 10, Figures 3, 4 cf. 1953 Micrhystridium densispinium Valensi, vol 32, no. 68. Description: Radially symmetrical test; spherical to ovate. Wall less than 1.um thick and evenly covered with closely spaced spines. Spines no longer than about 2,nm high and with slightly expanded bases. Sigg_pgpgg: Total diameter of test with spines (10 Specimens): 8(1l)l7 um. Occurrence: 47 samples; rare to dominant, found throughout all 88 three sections. Comments: Specimens assigned to this Species are similar to those described and illustrated in drawings by Davis (1963, fig. 7, 9, unpublished thesis) as Micrhystridium densispinium Valensi. Reference Specimen: slide Pb11232-5, 32.2 X 118.8. Micrhystridium Sp. cf. M, piliferum Deflandre, 1937 Plate 10, Figure 5 cf. 1937 Micrhystridium piliferum Deflandre, p. 80, pl. 15, fig. 11. 1971 Micrhystridium Sp. cf. M. piliferum Deflandre: Brideaux, p. 73, pl. 21, fig. 7. Description: Test spherical; wall thin and covered with short, slightly tapered spines. Spines evenly distributed and about 3 to 4.nm apart and 3 to 6,nm long. Size rssge: Total diameter of test with spines (4 specimens): 13(18)25.nm. Occurrence: 2 samples; trace to occasional, found only in the basal ASpen Shale of FCS and near the base of SCS. Comments: Specimens of Micrhystridium sp. cf. s, piliferum Deflandre reported by Brideaux (1971) are Slightly smaller than those found in this study but otherwise appear to be conSpecific. This species differs fromifl, piliferum Deflandre by having fewer Spines and spines with broad bases rather than being rod-like. Reference specimen: slide Pb11653-l, 35.9 X 121.1. 89 Subgroup POLYGONOMORPHITAE Downie, Evitt and Sarjeant, 1963 GENUS Veryhachium Deunff, (1954) 1958, emend. Downie and Sarjeant, 1963 Type Species: Veryhachium trisulcum (Denuff) Deunff, 1958 Veryhachium Sp. cf. 3, eurOpaeum Stockmans and Williere, 1960, forma 1 Wall and Downie, 1962 Plate 10, Figures 6, 7 cf. 1962 Veryhachium eurOpaeum Stockmans and Williere forma 1 Wall and Downie, p. 782, pl. 114, fig. 4, 5. Description: Body tetrahedral with a triangular outline and bearing 4 hollow spines of equal length. Sides of the body nearly Straight and extending to form apices of the triangular outline. Fourth spine vertical and usually flattened against body. Spine length up to 5 diameter of body. Size range: Total diameter of test with Spines (5 specimens): 7(9)11.nm. Occurrence: 7 samples, trace to dominant, found in the basal Aspen Shale of SCS and throughout FCS. Comments: Specimens here assigned were considerably smaller than those described in the literature but morphologically similar to Veryhachium eurOpaeum forma 1. Referance specimen: slide Pb11642-l, 42.3 X 120.0. Subgroup NETROMORPHITAE Downie, Evitt and Sarjeant, 1963 GENUS Leiofusa Eisenack, 1938 Type species: Leiofusa fusiformis (Eisenack) Eisenack, 1938 9O Leiofusa jurassica Cookson and Eisenack, 1958 Plate 10, Figure 8 1958 Cookson and Eisenack, p. 51, pl. 10, fig. 3, 4. Occurrence: Permian to Oligocene of various parts of the world, see Brideaux and McIntyre (1975, p. 39); 6 samples, trace to occasional, found in the basal ASpen Shale of SOS and throughout FCS. Subgroup PTEROMORPHITAE Downie, Evitt and Sarjeant, 1963 GENUS PterOSpermopsis W. Wetzel, 1952 Type species: Pterospermopsis danica W. Wetzel, 1952 Pterospermopsis australiensis Deflandre and Cookson, 1955 Plate 10, Figure 9 1955 Deflandre and Cookson, p. 286, pl. 3, fig. 4, text-fig. 52, 53. Occurrence: Early Cretaceous to Paleocene of various parts of the world, see Brideaux and McIntyre (1975, p. 39); 12 samples, rare to common, found in all three sections. Group ACRITARCHA (Incertae Sedis) GENUS Palaeostomocystis Deflandre, 1935 Type Species: Palaeostomocystis reticulata Deflandre, 1935 Palaeostomocystis fragilis Cookson and Eisenack, 1962 Plate 10, Figure 10 91 1962 Cookson and Eisenack. p. 496, pl. 7, fig. 10, 11. Occurrence: Aptian to Late Cretaceous, see Brideaux and McIntyre (1975, p. 26); 4 samples, trace to rare, not found in SFTS. ANALYSIS OF DATA égs_gi the Bear River Formation: Table 1 presents an abbreviated listing of significant palynomorphs found in samples from two sections of the Bear River Formation in southwestern Wyoming and from the upper part of the type section of the Smiths Formation with previously reported stratigraphic occurrences of these fossils in North America and other parts of the world. Those species with Stratigraphic ranges too extended to be useful are not included. However, all previously reported species which have also been identified in this study of these strata include some part of the Albian Stage in their stratigraphic range. The data from overlapping ranges points to a late Albian age for the Bear River Formation at the two sections studied and that part of the Smiths Formation Studied at its type locality. Brenner (1976, Figure 1) has reviewed the data on first occurrences of tricolpate pollen in various latitudes of the Western Hemisphere. Their first appearance in the middle latitudes is in middle Albian sediments. The diverse angiosperm flora of tricolpate pollen and one tricolporate (Nyssapollenites) in the Bear River Formation at the Stowe Creek section and to a lesser extent at the other two sections studied suggests a possible age of late-middle Albian for the oldest of these sediments. The overlying ASpen Shale contains late Albian cephalOpods and 92 93 Table 1 Stratigraphic occurrences as previously reported for some of the plant microfossils found in the Bear River Formation and Smiths Formation. Species Whose Previously Reported Stratigraphic Range Has a Top, Base or both Tap and Base Within the Albian Stage Appendicisporites potomacensis A, problematicus CamarozonOSporites ambigens Cicatricosisporites minor * S, subrotundus Concavissimisporites variverrucatus Coronatispora valdensis Costatoperforosporites fistulosus Deltoidospora sp. cf. 2. juncta "KoiliSporis excavatus' Pilosisporites trichopapillosus Undulatisporites undulapolus * Verrucosisporites rotundus Cedripites cretaceus * Eucommiidites minor * Phyllocladidites sp. Spgubivesiculites rugosus AsterOpollis asteroides Clavatipollenites minutus Cupuliferoidaepollenites minutus Liliacidites dividuus assess Nyssapollenites albertensis Psilatricolpites parvulus * Retitricolpites georgensis S, prosimilis * S, vulgaris * StriatOpollis paraneus Tricolpites crassimurus * T, micromunus Cleistosphaeridium multiSpinosus * Cyclonephelium sp. A Dinopterygium Sp. A Muderongia sp. 2 ** Odontochitina costata Oligosphaeridium anthophorum Spinidinium vestitum Tanyosphaeridium Sp. A Part of Previously Reported Stra- tigraphic Range in the Albian Stage L Early 1 Middle 1 Late J .l I L47 [ BearlRiver Fm}. v‘] I I If ‘ 3’ '. a 1 T3 I T.) I? f} 1 Q a l_ 7’ I‘ er: .. A .. - [ T A A " k as 4L as _1 — -. — .- —-| - — — fig. 4 1. db db 1 t!-—fl—\—‘—\—’\—flfi~——\—pfl~——\_’ IN AK a!\_ ‘P w- u- ND—-JLoq-—-o°-—-o4 —-h-oq.q-~—-—.q’-bN’-—-o"--1bgo--.bQ—L—‘D * Species found in sediments of the type section of the Smiths Formation as well as the Bear River Formation. ** Species found only in sediments of the type section of the Smiths Formation. 94 provides an upper limit for the age of the Bear River Formation. According to the recent Cretaceous time scale published by van Hinte (1976), the stratigraphic range of the Bear River Formation in southwestern Wyoming would occupy a time period of about 2 to 4 million years duration. Comparison with Other Palynofloras pT_Comparable égg, A comparison of plant microfossil taxa with other similar studies in North America is presented in Table 2. Not only is there an obviously greater Similarity with palynomorphs attributed to the middle and late Albian; but a marked Similarity exists between this flora and others reported in Western Canadian Strata. This Should be expected because of the numerous terrestrial plants which would accompany the southern push of the boreal sea during late- middle Albian and late Albian time. This should also be true with phytOplankton living in those Cretaceous seas which have been so clearly shown to be alternately transgressive and regressive. Floras from areas to the south and on the east side of the seaway (Hedlund, 1966; Phillips and Felix, 1971a, b; Bond, 1972) with the exception of Hedlund and Norris's study (1968) Show somewhat less similarity and probably represent a more Gulf Coast type flora with Slightly different ecological and climatic requirements. Four of the palynofloras listed in Table 2 reported no angiOSperms (Singh, 1964; Vagvolgyi and Hills, 1969; Hopkins, 1971; Bond, 1972) and appear to be older on this basis unless the very small angiosperm pollen were lost in preparation or overlooked during microscOpic examination. According to Brenner (1976) the appearance of tricolpate pollen in the higher latitudes 95 Table 2 Comparison of Bear River and Smiths Formation taxa with those of similar studies in other areas of North America. Author - Age - Location This study ----------- Norris (1967) - M.—L. Albian - Central Alberta, Canada Hopkins (1971) - L. Valanginian- Aptian - District of Franklin, Canada Hedlund and Norris (1968) - M.? Albian - S. Oklahoma Playford (1971) - M,-L. Albian - E. Saskatchewan and W. Manitoba, Canada HOpkins and Balkwill (1973) - L. Albian-E. Cenomanian - District of Franklin, Canada Brenner (1963) - Barremian-Albian - Maryland Vagvolgyi and Hills (1969) - E.-M. Albian - NE. Alberta, Canada HOpkins (1974) - M.-L. Albian - Canadian Arctic Archipelago Davis (1963) - E.-L. Albian - N. Wyoming Singh (1964) - Barremian4M. Albian - E. Central Alberta Cahoon (1964) - Neocomian-Albian - S. Black Hills of NW. 5. Dakota Brideaux and McIntyre (1975) - Aptian#M. Albian - District of Mackenzie, Canada Singh (1971) - M.-L. Albian - NW. Alberta, Canada Pocock (1962) - L. Jurassic- Albian - S. Alberta and S. Saskatchewan, Canada Pannella (1966) - M. Albian- Cenomanian - Denver Basin of W. Nebraska and E. Colorado Bond (1972) - AptianeAlbian - SW. Arkansas Hedlund (1966) - Cenomanian - S. Oklahoma Phillips and Felix (1971a, b) - Albian-Cenomanian - SW. Missis- sippi and NE. Louisiana Comparable Taxa Spores (44) 23(52) 13(37) 14(47) 21(74) 10(31) 21(79) 20(69) 17(60) 17(55) 23(86) 11(54) 27(76) 39(133) 18(63) 19(100) 3(16) 7(35) 13(74) Gymno- Angio- Marine sperms sperms (25) 13(23) 10(11) 6(15) 11(18) 6(14) 12(28) 7(16) 5(11) 8(18) 11(21) 8(22) 14(17) 18(23) 6(20) 9(29) 3(6) 6(20) 6(19) (16) 9(11) 0(0) 7(14) 4(9) 2(5) 8(14) 0(0) 0(2) 5(9) 0(0) 3(5) 2(4) 13(25) 0(1) 7(11) 0(0) 1(10) 1(10) (28) * * 2(8) 6(41) 2(16) * 5(64) 6(114) 1(13) 1(18) 0(4) * * Total TOTAL% (113) 45(86) 23(48) 27(76) 36(101) 18(50) 41(121) 29(93) 22(73) 36(123) 36(123) 22(81) 43(161) 76(295) 25(97) 36(158) 6(26) 14(65) 20(103) * Studies reporting no marine palynomorphs or not treating them. are the total taxa reported in (1) Numbers in parentheses each group. Notes: (2) The conspecificity of certain taxa with those in other studies was interpreted by this author. This required reevaluation and reassignment of some taxa, particularly those in the earlier Studies. (3) E. = Early, n. = Middle and L. = Late 52% 48% 36% 36% 36% 34% 31% 30% 29% 29% 27% 27% 26% 26% 23% 23% 22% 19% 96 of Western Canada would be Slightly later than in areas to the south and might explain their absence in all but Bond's palynoflora. A particularly significant comparability exists between gymnosperm taxa (at the Species and group level defined in this study) found in this study and those of Hopkins (1971), Brideaux and McIntyre (1975) and Singh (1971). All are from Western Canada and show over 75% comparability with taxa found in this study. This further demonstrates the close affinity of Bear River and Smiths Formation taxa with boreal palynofloras. The Similarity of the palynoflora studied in southwestern Wyoming with that reported by Brenner (1963) is not easily explained except in light of the generally cosmopolitan nature of pre- Turonian pollen assemblages (Doyle, 1969) and any, yet unknown, boreal connection with the present Atlantic Coastal Plain. If the Skull Creek seaway did indeed split in late Bear River time prior to the Spread of the boreal Shell Creek seaway, as Eicher (1962) has suggested on foraminiferal evidence, there may have been a short interval of time when plant migration could have taken place between the east and west Side of the Western Interior seaway. Such a land connection is not suggested by the comparability of palynomorphs found in this study with the palynofloras of Hedlund (1966), Phillips and Felix, (1971a, b) or Bond (1972), all located considerably south and east of southwestern Wyoming, however, and undoubtedly representing some— what more trapical floras, lessening their potential for compara- bility. The comparability with palynomorphs found by Hedlund and Norris (1968) from southern Oklahoma is 36% but still far 97 from conclusive. The taxonomic treatment of bisaccate pollen resorted to in this study, as discussed earlier, somewhat reduced the diversity of this group. Comparisons are based mainly upon similarity to modern genera. Thus, the potential for comparison of bisaccate taxa with those of other studies is reduced and limited to these "generic groupings" except for several bisaccate pollen which could be identified to the species level. Paleoenvironments 2T_Deposition: Introduction: In attempting to determine the probable depositional regime, climatic conditions and paleoecology during Early Cretaceous time, strong comparison must be made with modern analogs tempered with common sense and imagination. The approach of this study is to present information from several lines of evidence which together give a generalized picture of the environ- mental conditions existing in southwestern Wyoming during the deposition of the Bear River Formation. The fact that most samples in this study contain marine palynomorphs is Significant and interpreted to mean that the Bear River Formation was predominantly deposited in marine or at least brackish-marine conditions. AS already discussed, however, the degree of invagination of the embayment probably allowed for local freshwater environments on the landward side near the point of debouchment of rivers draining the highlands to the west. The numerous interrelated factors governing the distribution of plant entities in marine environments are Still little understood but warrant brief review here because they 98 form the basis for interpretation of the Bear River Formation. A number of major studies have been undertaken in recent marine sedimentary environments around the world in order to shed light on this subject: Koreneva (1957) in the Sea of Okhotsk, Muller (1959) in the Gulf of Paris and the Orinoco delta, Rossignol (1961) on the Israeli continental shelf, Koreneva (1964) in the western Pacific Ocean, Cross and others (1966) in the Gulf of California, Traverse and Ginsburg (1966) on the Grand Bahama Banks, Williams (in Williams and Sarjeant, 1967) in the Niger delta region and the North Atlantic Ocean and Davey (1971) on the southwest coast of South Africa. Although each study has presented some results unique to its own conditions, the following general trends and facts have been noted from these and related studies: 1) Most pollen and spores fall within the Size range of very fine sand (125.nm) to very fine silt (8 pm) but because of their lighter Specific gravity than comparable sized rock particles they act as particles of the finer silt Sizes and should ideally occur in greatest abundance in sediments of this Size. Some grains with odd shapes or protruding bladders are even further retarded in settling and may occur in even finer sediments. 2) The very light density of pollen and Spores, dinoflagellate cysts and acritarchs precludes their deposition in regions of high turbulence because of winnowing-type Size sorting. 3) The general trend for pollen and spores is to increase in frequency toward the shoreline (Whods, 1955). Hoffmeister 99 (1954) first recognized the importance of this relationship in determining the position of ancient shorelines. The reverse trend is usually true with micrOplankton although not always (Davey, 1971; Williams and Sarjeant, 1967). 4) Numerous factors affecting the distribution of plant microfossils such as longshore currents, wind and sedimentation patterns, rates of sedimentation, bottom conditions, ecological barriers for marine microplankton (salinity and temperature), etc. do not act uniformly and create distribution patterns with frequency contours deviating from the coastal outline. 5) Wind-borne pollen and Spores which are actually transported to the sea by wind represent only a minute part of the plant entities found in marine environments. The majority of these and other terrestrial forms are transported to the sea by rivers and their vast tributaries draining the land surface. 6) MicrOplankton distribution tends to be environmentally controlled and roughly related to sedimentary facies. The results of relative abundance counts in this study are presented in columns 1 through 4 of Table 3 (in pocket). The relative abundance percentages of Spores, bisaccate pollen, inaperturate pollen, other gymnOSperms (excluding inaperturates and bisaccates), angiosperm pollen, dinoflagellate cysts and acritarchs are presented in column 1. Column 2 shows the relative percent of terrestrial and marine forms as well as the total diversity (number of distinct taxa) of terrestrial and marine forms. Terrestrial diversity is further Split into diversity 100 of pollen and spores in column 3. Column 4 simply serves as a rough index of preservational quality based upon the relative percentage of unidentified palynomorphs. This graphic information is combined with the sediment type shown on the stratigraphic column to provide a basis for interpretation. The influence of reworking of older palynomorphs in the Bear River Formation sediments appears to be minor. A few highly corroded Spores such as those found in the cicatricose and canaliculate genera of the Schizaeaceae may have been reworked from older Mesozoic Strata along with some of the bisaccate pollen which are poorly preserved as a rule. The latter could, however, be a result of long distance transport rather than reworking. Comparison _o_f_ _t_1_1_e_ S_t_o_w_e_ SEEEL‘ and Fontenelle Eggs}; Sections: These two sections are roughly correlative and lend themselves well to an analysis of their environments of deposition. They have been divided into four zones or periods of distinct depositional history based upon the integration of available stratigraphic and biostratig- raphic data. A brief treatment of these zones follows (see Figure 6). ZONE.I: Both sections have a thick sequence of sandstone with interbedded shale at their base. This stratigraphic unit has been called the Tygee Member of the Bear River Formation in northern portions of the Idaho-Wyoming thrust belt and has been interpreted recently as a fluvial sandstone (Kamis, 1977) on the basis of sedimentary structures, stratigraphic position and grain size plots. His results are incon- clusive but suggest nearshore processes have modified at least part of the Tygee'Member in some areas and may, therefore, be interpreted as partly marine. Eyer (1969) has suggested a shallow, brackish water 101 Stowe Creek Section / ”:1 ? 33: < {—3 / Fontenelle Creek Section --r £1." AspgShale :;--IOOO' / 7 ...... L;; \ ...-X --- 9 7 iii \\\\\\\ :3; . E55 Zone IV 'i '7" x +800. ? 52':- % ;-;.soo- __ // 5;. 800” ESE-I. 1: :3; Zone III :1: ? 1'.“ 7 ?/ / -:-:- J soosixfi :3; / :—:-: ,4‘—'€i:%==ah> 555 cu: _. //e _ELzoo. 4oo'4__ ’ ‘" //; an: ’ 1': ‘ 0 so 100 IQQQ Zone I Terr.%—"—‘* 200'::::- \ \ '\\‘ 100 50 9 ? Ed \\‘ ‘———M8ro/c i :5.- ‘ 0 50 100 fi;; Gannett Group Terr.%r--—* on 35 100 so 0 Z ¢———-—— Mar.% fig; Figure 6 Zonation of the Bear River Formation at the Stowe Creek and Fontenelle Creek sections. Vertical Scale: 1" = 200 ' (61.0 m) B Transgressive Phase 7," Regressive Phase 102 or marine environment for some portions of the Tygee Member based on fossil evidence. The three samples studied from this thick sandstone sequence indicate at least some marine influence in the basin at the time of accumulation of the palynomorphs. The tOp of this zone is marked by the first significant increase in marine palynomorphs above the thick sandstone units (Pb11207-Pb11607). ZONE II: Overlying zone I is a thicker sequence of dark shales with thin, dark, coquinoid limestones interbedded with them. The relative percentages of palynomorphs by group shows considerable fluctuation in this interval. Of particular interest is the relative abundance percentage of marine entities which in both sections makes several distinct, correlative pulses interpreted as transgressions with sequential regressions (Pb11208-Pb11608, Pb11210-Pb11610, Pb11214- Pb11614 and Pb11219-ll621). Two additional minor pulses at the Fontenelle Creek section (see Figure 6). This could be simply the result of too wide sample spacing between comparable intervals at the Fontenelle Creek section. The tap of Zone II is marked by the final regression (Pb11222-Pb11622) following the last transgressive pulse. The absence of foraminifera, discussed earlier, and the dark, organic rich nature of these shales suggest a restricted basin or embayment similar to the model of Royse and others (1975). As the sea transgressed following deposition of the underlying sandstones a period of relative tectonic quiescence existed and finer sediments settled into this shallow, possibly restricted basin or embayment in southwestern Wyoming. The thin coquinoid limestones may represent relatively stable periods when rate and volume of sedimentation were reduced allowing a temporary domination of shallower shelf environments by bivalves and 103 gastropods. Some mudstones in this sequence from the Stowe Creek section also contain a fauna of abundant small gastropods and bi- valves which may possibly be dwarfed because of adverse bottom conditions in what seem to be lagoonal muds. Although the overall abundance of inaperturate pollen in this shale sequence is less than in overlying parts of the Bear River Formation, if their affinity to Taxodiaceae-type plants is correct, their abundance may indicate that poorly drained, swampy areas ex- isted on or near the shores of the embayment. The presence of thin coals in the Bear River Formation at various localities in south- western Wyoming (Glass, 1977) would support this idea; however, any interpretations made on the basis of inaperturate pollen must be considered tenuous because of the uncertainity involving their parent plants. Plants in genera of the modern Cupressaceae and Taxaceae, as well as the Taxodiaceae, produce inaperturate pollen similar to pollen found in this study and represent quite variable ecological and climatic conditions. The unusual abundance of inaperturate pollen is difficult to explain but similar high relative abundances were reported by Davis (1963) for strata of comparable age in northern wyoming. Angiosperm pollen are much more abundant in this interval of the Stowe Creek section than in the Fontenelle Creek section. This may reflect in a general way the existence of more favorable sites tx>the south for these plants to grow, but there are several other possible explanations. The greater abundance at the Stowe Creek section may, for example, be a function of sedimentological factors such as longshore currents concentrating these very small pollen grains 104 locally at the southern end of the embayment or a local concentration due to nearness to a river mouth carrying them from more upland areas where some authors have postulated the angiosperms to have first become diversified. Too little is known about their origin and early competi- tive strategy to interpret their distribution or abundance in marine sediments except where distribution patterns can be partly inferred from sedimentological factors. They do, however, form part of the , general paleofloral framework of the region and aid in age determi— nations as discussed earlier. The nature of the phytoplankton also appears to be characteristic in this lower shale sequence. It is readily evident that the trans- gressions at the Stowe Creek section are marked by increases in rel- ative abundance of acritarchs. Those at the Fontenelle Creek section, however, are marked by generally larger abundances of acritarchs coupled with large abundances of dinoflagellate cysts, especially during the maximum.development of the lower three transgressive pulses. The overall indication of environment is that deposition at the Fontenelle Creek section was under more normal marine con- ditions than at the Stowe Creek section as evidenced by (1) larger relative abundances, (2) greater diversity and (3) a different type of phytoplankton community. Hall (1965), in studying the paleoecological relationships of acritarchs in the Lias of England and South Wales, found them to have an environmentally controlled distribution. He noted a low phytoplankton diversity and domination of "inshore, partly en- closed" environments by members of the Acanthomorphitae (£32321- stridium and Baltisphaeridium). These findings have been backed 105 up by other similar studies which together help to explain the dif- ferences in phytOplankton at the Stowe Creek and Fontenelle Creek sections and further support the restricted embayment postulated by Royse and others (1975). The boreal sea which had pushed south- ward and expanded laterally into the region of the Stowe Creek section was relatively shallow and its restricted nature probably precluded the spread of anything but a limited Micrhystridium community. Only to the north and northwest toward the deeper, open sea could a varied dinoflagellate community flourish with a slightly more varied acritarch flora during transgressive pulses into the embayed area. ZONE III: Overlying zone II is an interval represented by 550 feet (167.6 meters) of interbedded siltstone and shale at the Stowe Creek section. This zone is reduced to about 230 feet (70.0 meters) of predominantly shale at the Fontenelle Creek section. Figure 6 illustrates the reduction of section in this interval based on the correlation of transgressive and regressive pulses below and above. Few samples from this interval of the Stowe Creek section proved pro- ductive. There, the coarser sediments suggest a regressive period of increased tectonic activity in the southernmost part of the Idaho- Wyoming Thrust Belt in middle Bear River time which apparently did not affect the Fontenelle Creek section until late Bear River time. Terrestrial percentages are high during this time in the Fontenelle Creek section suggesting a similar regressive phase with a dominance of shoreline, swampy (?) inaperturates but much less elastic sediments than to the south. Units 13 and 14 at the Fontenelle Creek section are part of this regressive phase and contain sediments locally con- taining burrowing, plant roots and some small, delicate gymnosperm- 106 like cones. A period of non-deposition cannot be ruled out as a possible factor in shortening this stratigraphic interval at the Fontenelle Creek section but no biostratigraphic data collected seems to justify the existence of such an hiatus. ZONE IV: The last nearly complete regression of the sea (Pb11234-Pb11637) marks the beginning of latest Bear River time. and zone IV (see Figure 6). The relative abundance of marine microfossils increases to a maximum in each section (Pb11238-Pb11644) just below the Bear River Formation-Aspen Shale contact. Produc- tivity of samples in this interval and into the base of the Aspen Shale is low and precludes a more complete understanding of the transition into the presumably more offshore environment of the Aspen Shale. Smiths Formation Type Section: The abbreviated nature of this section lends itself only to a very generalized interpretation of its environment of deposition. The sediments are entirely dark shale with no interbeds of limestone or coarser clastics. Relative marine abundances are rather low with gymnosperms as a whole gen- erally more abundant and spores and angiosperms less abundant than at the two sections to the south. The combination of these trends for terrestrial species suggests a closer proximity to true uplands or elevated, drier sites supporting species with bisaccate pollen and less favoring more poorly drained sites where certain spore producing plants lived. The great relative abundance of inaperturate pollen is striking and suggests extensive swampy (?) areas bordering the embayment or restricted basin possibly dominated by Taxodiaceae- 107 type plants with a relative reduction in the kinds of plants living to the south. Again, however, these trends may be more apparent than real if longshore currents, proximity to river mouths and/or high energy environments have been factors affecting the deposi- tional regime. Paleoclimate and Paleoecology 9; the; Egg; Iii-£1; Formation: Attempts to postulate paleoclimates existing during the Early Cretaceous are at best educated guesses based upon ecological requirements of mod- ern plant family counterparts. As seen from Table 4 this is very generalized with many families being presently found in all three latitudinal belts. The two basic unproven and tenuous assumptions which must be made in these types of interpretations are: (l) fossil pollen and spores can be related to modern families on the basis of morphologic similarity and (2) the basic climatic requirements of plant families in the past are analogous to their modern plant counter- parts. The association of families present in the Bear River Formation and shown in Table 4 suggests a subtropical to warm temperate climate for southwestern wyoming during the middle (?) to late Albian. Quite variable microenvironments for plant growth probably existed in this tectonically active area depending upon local edaphic conditions, nearness to the restricted boreal sea, proximity to the western highlands or rivers draining them, local tapography, etc. Slightly elevated sites near the sea with adequate drainage could well have supported many of the gymnosperms such as cycads, gink- gophytes and Classopollis-bearing plants as well as some of the bisaccate producing conifers. Some of the bisaccates, however, Table 4 Climatic distribution of probable modern counterparts of plant families identified in the Bear River Formation and Smiths Formation. (P = present but not commonest occurrence, C = commonest occurrence; WT = warm temperate) Family Sphagnaceae Lyc0podiaceae Selaginellaceae Cyatheaceae Dicksoniaceae Gleicheniaceae Osmundaceae Polypodiaceae Schizaeaceae Ginkgoaceae CycadOphyta Araucariaceae Cupressaceae Pinaceae Podocarpaceae Taxaceae Taxodiaceae Ephedraceae Climatic Distribution TrOpical SubtrOpical Temperate P C P C C P M bogs and ponds with low pH moist environments moist environments montane forests drier sites swampy or damp forests and humid areas southern hemisphere northern hemiSphere southern hemisphere arid sites 109 probably represent the small air-borne fraction brought from the tectonically active uplands in central Idaho. The exact habitat of Classopollis-bearing plants has been widely discussed and disputed. Most authors have considered them to have inhabited coastlines (Wall, 1965; Hughes and Moody-Stuart, 1967; Hughes, 1973) or floodplain and true uplands (Medus and Fans, 1967; Vakhrameev, 1970). Batten (1975) in recently restudying the paleoecology of Wealden (Neocomian) plant communities in England, believes that Classopollis-bearing plants occupied mangrove-type or sandy beaches, bars and barrier islands during transgressive stages. During periods of regression, however, they occupied "upland" sites consisting of slightly elevated sites on the floodplain whose edaphic conditions differed greatly from adjacent soils. Srivastava (1976) also suggests that Classopollis-bearing plants "occupied well-drained soils of upland slopes as well as lowlands near coastal areas pre- ferring the warm climates of transgressive seas." In both these cases the pollen of Classopollis-bearing plants would reflect relatively local vegetation when compared with the pollen from true uplands in montane regions. The abundance, relatively good preservation and widespread stratigraphic and geographic distribution of Classogollis in samples of this study would indicate the local nature of its parent plant(s) distribution near the sea and in association with a variety of other gymnosperms as Batten's flexible model suggests. The bryophytic spore genera suggest the existence of continually wet sites possibly in the uplands where extensive communities of these small plants could grow in close proximity to streams and 110 poorly drained slopes. In such environments their spores could easily be carried to the sea. Some of the bryophytic spores could also be representative of local bogs and ponds of low pH. The pteridosperm genus Vitreisporites (Caytoniaceae) is also a signif- icant element of the flora (especially in the Smiths Formation type section) but very little is presently known about its paleoecological requirements. Even xerophytic plants such as those producing Ephedroid pollen (Equisetosporites) are represented in the palyno- flora of the region, however, they may have been carried from great distances. A discussion of the paleoenvironmental significance of select plant groups as the angiosperms, inaperturates and microplankton has been included in the previous section in relationship to their ver— tical distributions. The significance of microfloral diversity in paleoecological interpretations has been treated by Cousminer (1961). Information on total marine and terrestrial diversity and pollen and spore di- versity was tabulated in this study in hopes of supplementing rel- ative abundance percentages of palynomorph groups. Diversity in- formation, for example, helps to indicate whether abundance increases are the result of a sudden "bloom" of one or several taxa or an adapt- ive peak for amore diverse and stable group of plants. The latter appears to have occurred in the following samples: Pb11642 and Pb11618 for marine forms, pollen and spores; Pb11221 and Pb11212 for pollen and spores; and Pb11231 and PblllOS for pollen. These could be interpreted as particularly favorable adaptive periods for the floras involved; however, some of the abrupt changes in diversity 111 just noted can be explained in part by sedimentological factors causing a distinct lithologic change from sediments below and/or above. Other samples such as Pb11234, Pbll628 and Pbll633 show little diversity change but abrupt changes in the relative abund- ances and nature of palynomorph groups, especially spores. These samples are all from zone III and occur in thick shale units. The relative enrichment of spores in these thick shales during short intervals suggests a temporary change in sediment source to areas occupied by a greater abundance of these plants, probably more poorly drained sites on the coastal plain. Zonation g: the Bear River Formation: The four part division of the Stowe Creek and Fontenelle Creek sections already outlined provides the best means for zonation of the Bear River Formation (see Figure 6). These four zones are admittedly not time equiv- alent, being based on lithologic facies and terrestrialdmarine per— centages, but they are useful in understanding the depositional history and associated environments of the Bear River Formation. Attempts to create a zonation based on first and/or last occurrences of index species and key assemblages failed because of the facies differences controlling key groups at the Stowe Creek and Fontenelle Creek sections. These facies differences have already been discussed in relationship to the distribution of dinoflagellates and angiosperms, these two groups being the most useful for time correlations and zonation. Additional studies of stratigraphic sections exhibiting intermediate environments of deposition are needed to carry time lines between these two sections and discover which species were responding to evolutionary rather than paleo- 112 environmental changes. Sufficient similarity between the exposed part of the Smiths Formation type section and the Stowe Creek and Fontenelle Creek sections does not exist in order to make correlations or determine to which zone(s) the Smiths Formation might belong. According to the relative stratigraphic placement of Rubey (1975), however, that part of the type section studied would fit in the lower middle part of the Bear River Formation. CONCLUSIONS 1) The analysis of palynomorphs in two sections of the Bear River Formation and one of the upper part of the Smiths Formation at its type locality has resulted in the differentiation of 113 distinct entities assignable to 30 genera of trilete spores, l genus of monolete spores, 1 genus of spores-incertae sedis, 16 genera and 4 groups of gymnosperm pollen, 9 genera of angiosperm pollen, 15 genera of dinoflagellate cysts and 6 genera of acritarchs. 2) The Bear River Formation at the sections studied and the upper part of the Smiths Formation studied at its type locality are middle (?) to late Albian in age. 3) The palynoflora of the Bear River Formation compares most favorably with palynofloras of similar age in western Canada and the Western Interior of the United States as previously reported by others. 4) The Bear River Formation exposed at the Stowe Creek and at the Fontenelle Creek sections are correlated and can be divided into four zones on the basis of lithologic facies, fluctuations in the relative abundance of select plant groups and transgressive and regressive cycles. 5) The palynofloral assemblage suggests that the paleoclimate in southwestern Wyoming during the deposition of the Bear River Formation was probably subtrOpical to warm temperate with quite 113 114 variable local environments controlled by factors such as nearness to the sea, edaphic conditions, tapography, microclimate, etc. BIBLIOGRAPHY BIBLIOGRAPHY Anderman, G. 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H., 1942, On fossil Xanthidia: Microsc. Jour., London, v. 2, p. 35-40, p1.4. White, C. A., 1892, On the Bear River Formation, a series of strata hitherto known as the Bear River Laramie: {American Jour. Sci., ser. 3, p. 91-97. ----- 1895, The Bear River Formation and its characteristic fauna: U. S. Geol. Surv. Bull., v. 128, 108 p. Williams, D. B., and Sarjeant, W. A. S., 1967, Organic-walled microfossils as depth and shoreline indicators: Marine Geol., v. 5, p. 389-412. Williams, G. L., and Downie, C., 1966, Further dinoflagellate cysts from the London Clay, in Davey, R. J., Downie, C., Sarjeant, W. A. 8., and Williams, G. L., Studies on Mesozoic and Cainozoic dinoflagellate cysts: Bull. British Mus. Nat. Hist. (Geol.), Supplement 3, p. 215-235. Wilson, L. R., and Webster, R. M., 1946, Plant microfossils from a Fort Union coal of Montana: American Jour. Botany, v. 33, p. 271-278. Wodehouse, R. P., 1933, Tertiary pollen II. The oil shales of the Eocene Green River Formation: Bull. Torrey Botanical Club, v. 60, p. 479-524. Wolfe, J. A., and Pakiser, H. M., 1971, Stratigraphic interpretations of some Cretaceous microfossil floras of the Middle Atlantic States: U. S. Geol. Surv. Prof. Paper 750-8, p. 35-47. 131 Woods, R. D., 1955, Spores and pollen - a new stratigraphic tool for the oil industry: MicrOpaleont., v. 1, p. 368-375. Yen, T. C., 1952, An Upper Cretaceous freshwater molluscan fauna of the porcellanite near Sage Junction, Wyoming: American Jour. Sci. v. 250, p. 344-359. ----- 1954, Age of the Bear River Formation, Wyoming: Geol. Soc. America Bull., v. 63, p. 757-764. APPENDICES mm «m an mm mm mm NM Nm am on em on am am swam N") am .oH won-4 \O qum ouswwm HHv-lv-O o—l «swam N.©HH N m.a~ m.eHH N o.mm n.NHH N s.~¢ H.0NH N n.mm m.¢NH N n.~¢ ¢.wHH N m.nm m.¢HH N n.¢m H.5HH N ~.¢m w.h~H N ~.wm m.m- N m.wm m.¢HH N o.n¢ ¢.nHH N n.nm m.ao~ N 0.0m moumawvuoou nuaemaanm onuqofianm nuwocfignm Humaoaaam anhooaaam mnwoouanm muueoaaam numouaanm nuNooHanm NuNcoaanm «nounaanm nnNOoaanm o-~¢o-nm 4mm ouaam wagon mannocoqumd mouuuommu>wocoo semauuoa Amenmmv ns>m~o mouoaauusmmmm on” . xaon mmmmmmmm Housman usvsauounsu xuooom Auduua>onxaomv woods uaoasuam pom unnooaoa «mafia: mouauqmwumoowuumowu anomamam Amsqxvmumv assuage“ nouauommoconoumamo ucoasumm van unsouaon domaaouom wouuuommauouum .mm afl awaqm Auownsmv msowumaoanoum nfl woodman mamcuomEOuom mouuuonmaouuaomm¢ camauuon pom acmxooo Ascmauuon can coaxoouv mamasscdmu mouwvuuauua96o< xoooom monocamuuuc> nouoauuuonuauo< tfltflcfltfl mudomm MHHAHNH Aasouu he Hmowuonmeafi<><>< h<>< >494 ><><><>< ><>< ><>< ><><><><><>< Havuh-h-¢>c>o1c> h-h-«)FIC>C>F10\ d'riq-Fid'd'q'ri moumsHvuooo nuNoeHHnm NunHNHHnm NuNMNHHnm HumHNHHam #:HHNHHAm «INOOHHnm ouNaoHHnm auNooHHnm HunHoHHnm cquoHHnm HIQMNHHAm HnNooHHnm N-NOOHHnm anMHoHHnm HummeHHnm HnHNNHHnm HuH¢NHHnm HuHNoHHnm onNooHHnm HnHmoHHnm H-NONHHnm ¢:MMNHHam mueHoHHnm HawHoHHnm H-NONHHnm 4mm madam whomNuHm Axoooomv usuoH=OHuou mouoHonomHua xoooom uoaHa mouHuomuonoHHuH pomsoo nocHa mouHuomquoH acuauumn Auoumao3 was :OmHHsv mouHuommusuHuau mouHuommHououm woodman maumHvuu mouoHHuuoHHmm ucoesuam vac uu300Hoa HuuuwuoHeHv usuoHHHmmmonoHuu mouHuoumHmoHHm nonsoo HHawEHHus moquHocvssaao ccHuH>oexHom HosHuH>oanomv mumsHsoo cummHunoEmsuo chouom Haouxoouv ouoocsuu meoHuuchuooz oHcouom Acomxooov moquHuo>mHoouuuso moUHuomebHvomoomH acmauuon paw coaxooo aHuwssH nouHuommHHNmN Amado uaHuomsamav mHHoaamm Auoasoumv :m:ud>moxo mHuomnHHHoN: uoasou usuaH90Huouovaumm nouHuoamesHN damauuoa Anamxooov moquHaHouHu am .mo .nm am mood msoHcosom moquHHconoHoHo :cmEuuon Accmauuoo was coaxooov «Hmaowwmweucos «HuomuHcHauuom swaHm Amuusznmumxv.mmmmmfl am .mo .mm -m omsom maouaoHHmm muommocHouHon Monaco a ..w. nomsoo mHHmuumsm moquHnummo xmoa msmoHsumHm mouHuomwouomuomoumumoo camauuon Auoasoov mHmaova> muommHumcouoo Housman Auoasoov maumosuuo>Hum> am woodman Huaoabumm was uusooHonv mausuodwm mouHuomuHaHumemoeoo mm NM on mm on mm Nm Hm on QN wN NN oN nN «N MN NN HN ON mH mH NH 0H mH Ooz 134 mm on on mm mm on an mm Nm Nm Nm Hm Hm Hm om me me we swam oH hooox NMQU‘O HH 0H 50‘ m d m ousmHm Inmmmtn WlfiLfi N'I’x'fx'fx'fln d’x‘f q a a momma N.¢HH N m.om n.0NH N m.wm N.NNH N o.Hm w.oHH N m.oc C.NHH N H.Nm ¢.eHH N o.¢m N.NHH N w.om N.NHH N n.mm w.mHH N n.0m 0.0HH N o.mm N.mHH N H.¢¢ m.NNH N ¢.o¢ N.NHH N «.mm C.NHH N N.Nn N.mHH N m.¢q N.NHH N H.N¢ m.NNH N m.mm H.0HH N m.nm N.mHH N N.oN «.0HH N o.¢m moumchuooo anHNHHAm HuomoHHnm onNcoHHnm oquoHHnm «nmNNHHnm H-NONHHAA nnaooHHam HuHmoHHnm H-NMNHHnm NnNHNHHnm H-NHNHHnm NumNNHHnm «amNNHHnm muNooHHnm NnNHNHHAm HINONHHnm qnwONHHnm onNaoHHnm HuwHoHHpm quNmNHHnm .oz ovHHm Nomuon up HoaHmmv msvHuH: mauhnmovmohomwxcHe oaHmm nsHaabu mouHsoHHomHmoxm mHuuoz Aumccoumv usumumooHuHsa mouHuommOuomHaum cmauvum HHcommpoouu am known can uoouo HoaHE moquHHEEoosu .mu nouHaochNU usHGOmcmh was Noooom .vaoam .wsHmm movHommMHo «HHHOQOmmeo Noooom msoowuouo mouflmHuvoo >on HoaHomv Huonawp mouHuommchHHHmo pans: Amsaamv.mmmmmmmm am acmxooo «HHmuumac mouHocHuoosuu< soHHom camuummmmd zuHHom_ZNummozzwu camauuon can somxooo usumHsoHuou am cadauuon vac somxooo m=>ucm mHuomuouHsom mHnmm mo mmuHuommouumwNouH mmmbmm NHMHOZOZ cam o> :waHm mspcsuou mouHuommHmoosuuo> Housman msHomuHscss mouHuoanuuHsvsa on mm on mm Nm Hm om ma ma Na mo na ¢¢ m¢ Ha o¢ an .oz 135 co co we no no do «0 me no no No Ho Ho oo 00 mm mm mm swam ¢H NH NH HH oH oH HH «H mH NH oustm Inmm 0000000 0 000000 lnlfilnlnln «swam n.mHH N ¢.Nm m.mHH N N.Nq m.oHH N ¢.Nd N.NNH N N.NN N.NHH N N.Nq N.mHH N m.o¢ N.@NH N o.cN m.0HH N H.N¢ H.NNH N o.mm o.HNH N N.¢¢ m.¢NH N w.¢m a.HNH N m.Nm o.mHH N c.N¢ o.wHH N w.o¢ ¢.wHH N m.¢¢ N.NHH N H.Nm c.NHH N m.am m.NHH N N.Nm o.NHH N H.NN C.NHH N N.Nm C.NNH N m.¢q H.NHH N N.o¢ n.mHH N m.mq C.NNH N N.Nm mmumquuooo oquoHHAm nanoHHnm ouNeoHHnm HuNONHHnm manoHHnm muNaoHHnm HuwoNHHnm muNccHHnm onNaoHHnm NnoHoHHnm Hno¢oHHnm m-NMNHHnm HumooHHnm H-NMNHHnm H-NooHHnm mueHNHHnm HuONNHHnm ouNeoHHnm HummcHHnm HnHMNHHnm H-NONHHnm oanoHHnm ouNaoHHAm cuNaoHHnm .oz mvHHm ameam Awoacoumv ususaHa mouHaoHHomosvHouomHHsmdu maamHOUHNH u zmHHom.ZNmmmoHuz< mHuuoz mauxou .H swaHm nauseoumv usumHsoHuououum am Housman Hoouonv masvH>Hv moquHouHHHH nosaoum ususuHa mouHaoHHoaHum>mHo NHEUHDmOZQZ a zudHom EmummoHuz< acmmHHz AuowsHmmHoNV aseHHHum mouHuomuHouuH> oouon mmmmwmm mouHHsOHmo>Hnmmmm aoHHom cahuumsmuwuopom HHmEm :oHHoa oANuumsmHmoovom owumH :oHHom Oahu-MMMflM a mmmwm .au musicavmfiooaamam Honsoo mmmmmmmwm 2M .mu .m« mouHaoHHomodHuum .mm mouHoHsmosoz uumwumH:H cam somaosa .oHcouom HoHsouomv mmmwmm.am _mmmmmumm moquHouHuwH N .am .H N .Am am H .mm mouchHHomousuuumwaH «N mN NN HN oN mg no No we no «0 no No Ho 00 mm Nm Ooz 136 MM «M NM HN HN oN oN oN MM MM MM MM NM NM ommm HNM MH MN MN NN «N MN MN MN NN HN 0N MH NH MH MH ousuHm INN“ 000 00000000000 «swam N.MHH M.MNH M.NHH N.MHH ¢.NHH M.¢HH ¢.MNH m.NHH N.HHH C.NNH q.MNH M.NNH N.OHH M.MHH N.MHH m.HNH o.MHH M.MHH N.NHH M.¢HH o.MHH NNN NNN u:o~o~ c>paws «weir: 0MGNWHI‘O‘NMM ><><><><>< c>n~c>c>¢>ou~o 61¢56ld’d’d'F5F3F363F) moumchuooo HuMHMHHnm H-MHNHHHm HsN¢MHHnm QnHHNHHpm #:NNNHHAm MnMONHHnm ManoHHnm HuMONHHnm HnMHNHHAm H-NMMHHHm ouNeoHHnm N-MNNHHnm auMONHHnm auHMNHHnm HnMONHHnm NuMONHHnm nuNaoHHnm N-NHNHHnm quNHNHHAm MuNdMHHnm quNHNHHnm 1&me 4 .Am abHHocmoaoHoNu xsmovHuM AswaHmV manosHAuHuHsa aaHvHuomnmmouuHoHo NoncomHm Mam sonxooo HoN: «HHouoanovmamHno MNH aw oHHuoz mHHHaHmoum .N Housman mHuamwuoum uuuHaHooHuuHuoN can 0M mHuuoz Amocom can uoouuv msHs>umm moumeouHuumHHum NM MM «M MM NM HM OM MN MN NN MN .02 137 CM MM MM MN NN MN MN NN MM NM MN HM 0M NN MN MN MN swam N‘f NMd’o-IN 5000 0|!) @080 MONwO‘ ousmHm Q @0‘0‘00 [\QQN NQ 00000 [\NNN oumfim M.MNH N.NHH M.MHH N.MNH M.MNH M.MHH M.MHH M.MHH H.NNH N.MoH M.NNH M.MHH ¢.MNH ¢.NHH H.NHH M.MNH N.NHH ¢.NHH ¢.¢NH «.NNH M.MNH M.MHH M.MNH M.NNH NNN NNNNN NNNN xx N NNNNN NNNN M.NN M. aaHaHvHanM .a« N auHuuuooovounm unoou .Msoeo .ouvaaHmon muonmouuuoo am .wo .mu «HuHMoouum xoooom asoouuouo.asHsHMHuoaoooHcm 33:3 28 .323 $35: a .m No>ma AxouaomHm can somxooov asuosmonucm asHvHuoasmmmuwHo uoHvuo> was oxuwHo .vooao .HuuonH< muoumoo ccHuHeoousovo N .m» .2 H .nm oHMaouovsz somcomHm was samxooo oumvNEmHno .N .mo .mm muostomwon ¢ .nm aswmmuoumoaHn N .mm «m H .au mouvaoHuon MoH «OH MoH NoH HoH ooH Mo Mo Nm Mm Mm «a Mm Nm Hm om MM .02 138 mM OM OM MM NM NM MM MM ommm HNMN‘I’M NH HH OH ouamHm 0H OH OH 0H OH OH 0H 0H 0H m m m uuufim M.MNH N H.Mq 0.0NH N M.NM M.MHH N H.o¢ N.MNH N M.HM H.HNH N M.MM M.MHH N N.NM M.NNH N ¢.H¢ M.MHH N M.MN o.HHH N M.MM H.MHH N M.NM N.NHH N N.NN M.MNH N M.MM mmumaHvuoou HuNeMHHAm H-NMMHHnm M-NMMHHnm HuMONHHnm HuMMMHHnm M-NMNHHMm MINOMHHAM HuMMMHHam HuMONHHnm HquMHHMm M-NMMHHMm MuNMMHHam .oz ovHHM oHcaon was HHmz H QEMOM ouoHHHHs Mac mswaxooum_mmmmmmmmm 2M .mo .nm aanomsNuo> somxooo can unvaonoa mHmsoHHmuumsm mHmmoauommououm xomaomHm Mam camxooo uHHHMmum mHumNUOEOumoouHmm 32.3me 3 .m .8 .8 .m Hucon> achHmmesmM .2 ..u—o .Au .HIA ouvamHmon AouvcmHmonv assonmcooaH am unvaaHmoa oHHmuum ..HIA .323 533.. 5323.3..3: MHH NHH HHH OHH aoH MoH NOH MoH .Oz 140 APPE 113D IX B— 2 Fontenelle Creek Section: NH Sec. 5, T. 24 N. R. 115 ‘: ncoln County, Wyoming. Vertical Scale: 1" =50' (15.2 m) Samr 1 numbers noted at right of diagrammatic lithologic column, e. 601 ”2, etc. Phi etc. 8 These numbers are preceded by Pbll , e. g. Pb11601, Section described, measured and sampled by the author. X 1:: 31 mdsi H8199“; (ohms Maasback <1 up 2'0 becomes less ream rcswfi m rm w} 57. &‘ .sk H , lg ’5 \E‘k"°'z.‘\.w e «a <51; \5: 51k 10rd. 1an )‘osklshw-m-c EL'n-flbd SM? $151; 070))HK bur, . .. \oiurb)3252'm~ p\ rooigh hear .»~ » ~ ' 01-4 ”to? beam ssndq Kear¥ OE ,_- apha- mFe 51m ss,\ew\ e. __ - (ORC- "p10 1' but: £3.1- S‘n, Hk (05 as h3p\ \Sgos gro015 _Liu heari op («SH \a Wibd\ ' / 1?. «\MHR 1.9:ka qq 10b“: :xh'c —- \ ”‘15 5613\Hpmk Somewkaf reg": 309m.1030‘ 1L. 55) 5T¥amS€ p .32.ch wishgmp up Oh 10p of ya i” E - — 'Hq l0- 5h Jam/(=1? exp on dope. *5 2:1. ”‘1ka $5¢5k r’) —;_"_ . f: o 2:?“ is:- ... f": \s Mk ..1 a u. a :: Glb _Tq/BJB L566 U&\V‘S )‘;1 CV \oan ”P :_, ,. ;:;—_;- be“ \h m o 3:: ' fl MOSH“ (NA ’prob $\’\ TIT m :7: ’1' E1523 E —-_-:—_ g1. map-11,12. :“N — -.« _ _ _ 3.51m) 131k w1kr$ dkaq)bh1)?fi . :2§55>:¢P _“— —c1)Nngu\-\Evc meas.,spld lk-dkeg~1,3v15 mh, 5: Tan $5 abov '1 ‘2 i=1” '0 E U r—" .— ~- ;._ @LSHH,“ E...“ -—-~—-— 1155)”? 2:0 w/m- Sm Sc 11“!) 7— - _— —Q-—— inierfcr HP flow 20 urea M, C s‘ha cohc, Some In \aders APPENDIX B S trat igraphic Sections APPENDIX B—l Stowe Creek Section: Sec. 21, 22, T. 14 N. , R. 119 W. , Uinta County, Wyoming. Vertical Scale: 1" = 50' (15.2 m) Sample numbers noted at right of diagrammatic lithologic column, e. g. , 201, 202, etc. These numbers are preceded by Pbll __, e. g. , Pb11201, PbllZOZ, etc. Section described, measured and sampled by geologists of Chevron U.S ..A Inc. . _o-1___ — ;_ o 6. Luz.» + + s¥ . 3 8* WW5: s an. 9i“... Pi .5 fl” 7 - 1 Mock h 'p ‘Hfi :11: SE: .2le 3b “5v " :3, 9w sttsi, pHy, Pale. 9N l)?“ by! dk 3.111) \olk "I '1 -’~' .13: 7.43 \ t ' "lugghfid R. V,’ redqula I _ ¥f U" _I—zs‘i od‘n . , rash? \od (33' TOKAX ° 5 0. (I). < 59?“; hd bed Mod g4, '__'_I;,;I;I 112.55, mo hd, tui’I SK Cd‘lQ — - — 91,511. sh, hd spk’rxl, dK cw :4“ Sh, 83:1, Sl SH ,m :L/Lgss °§1PX$$ U. $\C93\{1CI """" Jaafirm’ odhd echo Pl-PDS ., ...vo _ flcvd aeseHch, 55f, Oféwgle beni‘I lwo 'g Ufi. eH—s + “We... (_\_1 __‘.__. 5%... 55:... ::_— .2; £51” "‘1 io dK. ~3qu SH’Y "0 _Ti , . ; T’ ,4_‘ U E : 7 W 541—; 0 3+ ex. A r: '0', ___i '0 \{Ihd $3 :4“ ; :..:.'-: 0d V ( an: d b\ lcal 135.9% m 9, :2; ;;;_.'*_T: flshI5\+\II brn—qy {—11- ‘o J_L—J—s—::: _ ' EF___U g """"" m E bm — — — -— \ 39s———rz'z —’—'—— fii‘ékbf fr; qgtbgld 'UP _ _ 9': , N/ _ _ _ _ 2:0 ‘8 _—_-_ H 9w "’1——?—0‘* ad hd \t .19.. a... : b\K_ K“! _ "_“‘ O —. T —" ~23| — — — < 8 fia‘f“? _——_—-_~ 7A1 g.-£:.f a ?h' b‘ I‘EOSA intbdyt‘i LE '2' :I—nog/O/SEK Chet) r _g‘f- ‘ g 111: .. N _ _———_ :—:—:_w E‘ :_—::- 0 .— 10 __ '.—.‘.—'.— I4_I 35 mod hdI ‘HnK Edd? qr,+m EE’L}, 5“; mod hdI‘ blKI S P\c_\/ .'__'. I2. ssrrn+oganI PO". mas, 315mm, H: qdvqel 0 week, l’r nZJF/‘EP 5\+\I AK. 0 _ ) ~ 15.35%“. ICBrb ) Sltfbh “d ,_ IIEI—o..sgls&&d,¢ 9v, +Ihkbdd sl (foil. Dmva 104.13%: sH-q ‘59-“ c” s tT—:: “ssh; 4,2 \ I 9,—_. gag}, Mod ha. ‘Unn bddI ~ 9:...991 mm 9 99 99 N _.. ‘1 ‘” '_: hIIstI \IeA- qxf §_,‘ ....1: ——.*:_ $.- S3 I Z—Z':_ _._.,; ':-.~ if“ 2%.. .bpngs ° "‘ 1:: .—'— 7:: gigs?“ 2H \5 bd men.— a; :1: m g icvd [o—C—Hofl _—:_ I— 717: :‘Z'b hd (ii-us scat Pas at E _—__Z: i. chist sum], red _ g” .. ..L 2_. s +s‘t s\ 54., qel— gq 0.: "“1919 ‘99 3.922.399 .19.. 99‘9 2. \+ + w H. + b K E‘aibbsh ‘g/ H3. 3‘5": ‘ -' Lu. 139 141 APPENDIX B-3 Smiths Formation Type Section: N., R. 118 W., Lincoln County, Wyoming. Vertical Scale: NW%, NE% Sec. 27, T. 29 1" = 50' (15.2 m) Sample numbers noted at right of diagrammatic lithologic column, e.g., 681, 682, etc. e.g., Pb11681, Pb11682, etc. W. W. Rubey and sampled by the author. SNflTlfS 1. sh, tan ch, %}5, hd' ‘Fos abn‘k bu+ ofiicuif +o collect 7.5h, *an Cl.“ “KO. Unit 5 u? two/«Pas noied Q‘s, t-Ke Unit 8 55hr 200' 5 0m. gégig< Ioo' Cone-fig more. or \ess hd layers 0; bf" 635+ pavh‘c. lbr'xl i9 up hfl‘i $05 Cofln 319—]? no; . gas?) u5~Msgm a“. u. n mi Unios.’c .‘ob .' 70. (:4 ’_ r mannu :Ompehamg C - - mam 15h,+an old. in exp ls,H- (a CV, SAL! ALB j wit‘r; mac: “Kc. * “inns fiizgngfi rs 2.}: tip, red 50“ in up +wo- flaw-As, 2rd3 fi’c +6“ CJV 30” ‘n to»: H:- 3q-F r can cue. SS |/I. «CT ”“2 3p?“ at mid o$ Unzi- DRANEY Ls | Note: J.Khrne3 4: 3 +h sifi; v H 3“. «9&5 agu‘kogback These numbers are preceded by Pbll , Section described and measured by .ssflwd,‘ 9Q Som2that ow; ...... (r. at base. 0" H2 that makes prom rtdc) LL- cvd I- be‘ won». 500' ....... ..ea 685 [_O_. shhblk cl.‘ cuff-cw \nd Fe. cone. 2.st boars) no ‘05 ‘Foufid 664 683 A FORMATION mom. Units 1 to 11 constitute the "lower shale member" of Rubey (1973). Unit 12 is the lower 5 feet of Rubey's "upper sandstone member" which forms a ledge that makes a prominent ridge at the type locality. APPENDIX C Sample Information Stowe Creek Section Lithology Sample Type Feet (Meters) Collection Accession Above Base £9, £2. Gannett Egg. 83 spot 1 -62 (-18.9) Chev.-SC—l 2611201 Bear River Em. 8h " 105 (32.0) " 2 2611202 * " " 139 (42.4) " 3 2611203 lignite " 150 (45.7) " 4 2611204 marl " 181 (55.2) " 5 2611205 * sh " 202 (61.6) " 6 2611206 " " 225 (68.6) " 7 2611207 * " " 250 (76.2) " 8 2611208 * " " 293 (89.3) " 9 2611209 * marl " 310 (94.5) " 10 2611210 * sh " 320 (97.5) ’ " 11 2611211 * 1 6 to 12 inch (15 to 30 centimeter) interval collected in a pit up to 23 feet (76 centimeters) below the surface. * Productive samples which were used as the data base in this study. Note: Samples 6/22/77 I-l to 6/22/77 I-6 were collected on the north side of Fontenelle Creek; all other samples in this section (6/22/77 I-7 to 6/22/77 I-34, 6/23/77 I-l to 6/23/77 I-10 and 9/17/77 1-1 to 9/17/77 1-9) were collected south of the creek. 142 143 215221331 Sample Type Feet (Meters) Collection Accession Above Base £2. 32. sh spot 330 (100.6) Chev.~SC-12 Pb11212 * " " 340 (103.6) " 13 Pb11213 * n n 377 (114.9) " l4 Pb11214 * n N 422 (128.6) " 15 Pb11215 * u H 441 (134.4) " l6 Pb11216 * u H 455 (138.7) " 17 Pb11217 * n n 474 (144.5) " 18 Pb11218 * n N 493 (150.3) " 19 Pb11219 * n H 508 (154.8) " 20 Pb11220 * sh-marl " 528 (160.9) " 21 Pb11221 * sh " 550 (167.6) " 22 Pb11222 * " " 588 (179.2) " 23 Pb11223 sltst " 658 (200.6) " 25 Pb11225 n n 675 (205.7) " 26 Pb11226 sh " 745 (227.1) " 27 Pb11227 sltst " 871 (265.5) " 28 Pb11228 * sh " 957 (291.7) " 29 Pb11229 * n n 978 (298.1) " 30 Pb11230 * n H 1007 (306.9) " 31 Pb11231 * fl " 1065 (324.6) " 32 Pb11232 * n N 1071 (326.4) " 33 Pb11233 n H 1099 (335.0) " 34 Pb11234 * n H 1179 (359.4) " 35 Pb11235 * n H 1245 (379.5) " 36 Pb11236 n n 1268 (386.5) " 37 2611237 144 Lithology §gmplg_Type Feet (Meters) Collection Accession Above Base N_o. liq. sh spot 1280 (390.1) Chev.-SC-38 Pb11238 * Aspen Shale sh " 1337 (407.5) " 39 Pb11239 " " 1378 (420.0) " 40 Pb11240 " " 1422 (433.4) " 41 Pb11241 * Fontenelle Creek Section Gannett grp. sltst spot -106 (-32.3) 6/22/77 I-l Pb11601 Bear River Em, mdst " 48 (14.6) " 2 Pb11602 * ls composite 75-100 6/22/77 I- 3 Pb11603 (22.9-30.5) sh & 1s spot 93 (28.3) " 4 Pb11604 mdst " 102 (33.1) " 5 Pb11605 ls " 105 (32.0) " 6 Pb11606 mdst " 106 (32.3) " 7 Pb11607 bent. & sh " 139 (42.4) " 8 Pb11608 sh " 153 (46.6) " 9 Pb11609 " " 168 (51.2) " 10 Pb11610 " " 188 (57.3) " 11 Pb11611 ls " 200 (61.0) " 12 Pb11612 sh " 208 (63.4) " 13 Pb11613 " " 228 (69.5) " 14 Pb11614 bent. " 248 (75.6) " 15 2611615 sh & ls composite 268-274 " 16 Pb11616 (81.7-83.5) 145 Lithglggx Sample Type Feet (Meters) Collection Accession Above Base £2, E2, 18 spot 276 (84.1)6/22/77 I-17 Pb11617 sh " 282 (86.0) " 18 Pb11618 * H " 305 (93.0) " 19 Pb11619 H H 318 (96.9) " 20 Pb11620 u H 338 (103.0) " 21 Pb11621 * H " 358 (109.1) " 22 Pbll622 * u H 366 (111.6) " 23 Pb11623 H H 386 (117.7) " 24 Pb11624 * n H 407 (124.1) " 25 Pb11625 n H 412 (125.6) " 26 Pb11626 u H 418 (127.4) " 27 Pb11627 n H 437 (133.2) " 28 Pb11628 * n H 457 (139.3) " 29 Pbll629 * n H 477 (145.4) " 30 Pb11630 * n H 497 (151.5) " 31 Pb11631 * H " 517 (157.6) " 32 Pb11632 * H " 547 (166.7) " 33 Pb11633 * H " 557 (169.8) " 34 Pb11634 n H 569 (173.4)6/23/77 I- l Pb11635 * bent. " 572 (174.3) " 2 P911636 sh " 589 (179.5) " 3 Pb11637 * n H 609 (185.6) " 4 Pb11638 n H 629 (191.7) " 5 Pb11639 * H H 646 (196.9) " 6 Pb11640 as " 668 (203.6) " 7 Pb11641 146 Lithology Sample Type Feet (Meters) Collection. Accession Above Base £3. £2, sh spot 692 (210.9)6/23/77 I- 8 Pb11642 " " 727 (221.6) " 9 Pb11643 " " 736 (224.3) " 10 Pb11644 Aspen Shale porcel. 2 ft. chan. 769-771 9/17/77 I- 1 Pb11645 (234.4-235.0) n H 784-786 H 2 2611646 (239.0-239.6) " " 794-796 " 3 Pb11647 (242.0-242.6) " " 814-816 " 4 Pb11648 (248.1-248.7) sh & sltst " 852-854 " 5 Pb11649 (259.7-260.3) ss " 864-866 " 6 Pb11650 (263.3-264.0) porce1. " 884-886 " 7 Pb11651 (269.4-270.1) sltst " 984-986 " 8 Pb11652 (299.9-300.5) sh " 1004-1006 " 9 Pb11653 (306.0-306.6) Smiths Formation Type Section sh spot 335 (102 1)6/15/77 1- 1 2611681 0 n 350 (106.7) H 2 2611682 n n 375 (114.3) H 3 2611683 n n 400 (121.9) H 4 2611684 n n 425 (129.5) H 5 Pb11685 " n 450 (137.2) H 6 2611686 H H 480 (146.3) H 7 Pb11687 147 Lithology Sayle Type Feet (Meters) Collection Accession Above Base g9. fig, sh spot 505 (153.9)6/15/77 I- 8 Pb11688 * n n 530 (161.5) H 9 2611689 * PLATES Figure 10, 11 148 PLATE 1 (All figures X1000 unless otherwise stated) Page Acanthotriletes varispinosus Pocock .......... . ...... ... 29 Aeguitriradites spinulosus (Cookson and Dettmann) Cookson and Dettmann; X500.. ........................... . 29 Appendic13porites potomacensis Brenner........ ........ .. 30 Appendicisporites problematicus (Burger) Singh .......... 30 Appendici3porites sp ..... .................. ......... .... 30 BiretiSporites potoniaei Delcourt and Sprumont .......... 31 Camarozonosporites ambigens (Fradkina) Playford ......... 32 Cicatricosisporites hallei Delcourt and Sprumont ........ 32 Cicatricosisporites minor (Bolkhovitina) Pocock......... 33 Cicatricosisporites venustus Deak; proximal view (Figure 10) and distal view (Figure 11) ..... -.-. ........ 33 150 PLATE 2 (All figures X1000 unless otherwise stated) Figure Page 1 Cicatricosisporites subrotundus Brenner ..... . .......... . 33 2 Cingutriletes clavus (Balme) Dettmann ......... .......... 34 3 ConcavisPorites jurienensis Balme......... ....... ....... 35 4 Concavissim15porites variverrucatus (Couper) Brenner.... 36 5 ConcavissimiSporites punctatus (Delcourt and Sprumont) Brenner ...... . ............ .............................. 35 6 DeltoidOSpora psilostoma Rouse; X500 ............... ..... 38 7 Coronatispora valdensis (Couper) Dettmann.......... ..... 36 8 CostatoPerforOSporites fistulosus Deak.................. 37 9 Cyathidites minor Couper.......... ................... ... 38 10 Cyathidites australis Couper......... .............. ..... 37 11 DeltoidOSpora sp. cf. 2, juncta (Kara-Murza) Singh...... 38 12 Gleicheniidites senonicus Ross.. .......... ..... ......... 40 13 Foraminisporis wonthaggiensis (Cookson and Dettmann) Dettmann... ....... O. ...... ...... ...... ......OOOOOOOOOOOO 39 151 PLATE 2 Figure 10 11 12 13 152 PLATE 3 (All figures X1000 unless otherwise stated) Gleicheniidites Sp. cf. 9. circinidites (Cookson) Dettmannoo0 .............. 00000000000000.000000000000000 Klukisporites pseudoreticulatus Couper .............. .... Kuylisporites lunaris Cookson and Dettmann............. "Koilisporis excavatus" (Brenner) Pannella; manuscript name in Pannella (1966, p. 48, pl. 4, fig. 3) ..... ..... Lyc0podiumSporites austroclavatidites (Cookson) Potonie ..... 0000000000000000000000 ....... 00000000000000 Neoraistrickia truncata (Cookson) Potonie... ..... ....... Ornamentifera echinata (Bolkhovitina) Bolkhovitina ...... Psilatriletes radiatus Brenner ......................... Osmundacidites wellmanii Couper......................... Pilosisporites trichoPapillosus (Thiergart) Delcourt and Sprumont 0000000 000000000000000000 00000000000 00000000 Stereisporites antiquasporites (Wilson and Webster) Dettmann ......... .... ................ ........ ........... Todisporites minor Couper ............................ ... 42 41 43 44 44 46 45 45 46 46 153 Figure 10 11 12 154 PLATE 4 (All figures X1000 unless otherwise stated) _P_ag_e Trilobosporites minor Pocock ............................ 47 Triporoletes reticulatus (Pocock) Playford; X500 ........ 48 UndulatiSporites undulapolus Brenner... .............. ... 48 Verrucosi8porites rotundus Singh........ ...... .......... 49 Verrucosisporites sp .................................... 49 Laevigat05porites ovatus Wilson and Webster ............. 50 Schizosporis parvus Cookson and Dettmann;.X500 .......... 51 Abigg-type pollen; X500....... .......................... 51 SchiZOSporis reticulatus Cookson and Dettmann; X500..... 51 Araucariacites australis Cookson; X500 .................. 52 Araucariacites limbatus (Balme) Habib; X500 ............. 52 Callia1a5porites dampieri (Balme) Dev ................... 52 10 11 12 13, 14 15 16 17, 18 19 20 156 PLATE 5 (All figures X1000 unless otherwise stated) Cedripites cretaceus Pocock; X500 ....................... Classopollis classoides Pflug, emend., Pocock and Jansonius; single grain (Figure 2) and tetrad (Figure 3) gycadOpites sp .......................................... Eucommiidites minor Groot and Penny ..................... Eucommiidites troedssonii Erdtman.. ..................... EquisetOSporites multicostatus (Brenner) Norris ......... ExesisPorites tumulus Balme.... ...................... ... GinkgocycadOphytus nitidus (Balme) de Jersey.... ........ Inapertur0pollenites sp. 3 .............................. Inaperturopollenites sp. 1 .............................. InaperturOpollenites sp. 2......................... ..... Laricoidites magnus (Potonie) Potonie, Thomson and Thiergart; X500 ....... . ........... . .............. . ...... Laricoidites gigantus Brenner; X500 ..................... Monosulcites sp ......................................... Perinopollenites sp. cf. P. elatoides Couper ......... ... Phyllocladidites sp.; X500.............................. Page 53 54 54 55 55 56 56 57 59 58 60 60 61 61 62 157 PLATE'S Figure 18 19 20, 21 22, 23 24 25, 26 27 28 29 158 PLATE 6 (All figures X1000 unless otherwise stated) Pinus - Picea-type pollen; X500 ............... . ...... ... Large Podocarpus-type pollen; X500........ Small Podocarpus-type pollen; X500 ............ . ......... Rugubivesiculites rugosus Pierce; X500..... ...... ...... Vitreisporites pallidus (Reissinger) Nilsson....... ..... Clavatipollenites minutus Brenner ....................... Liliacidites dividuus (Pierce) Brenner .................. Liliacidites peroreticulatus (Brenner) Singh ....... ..... Liliacidites textus Norris........... Cupuliferoidaepollenites minutus (Brenner) Singh ........ Psilatricolpites parvulus (Groot and Penny) Norris; single grains (Figures 15, 16) and tetrad (Figure 17)... Psilatricolpites sp..... ....... ... Nyssapollenites albertensis Singh.. ..................... Retitricolpites georgensis Brenner ...................... Retitricolpites prosimilis Norris.... StriatOpollis paraneus (Norris) Singh .............. ..... Retitricolpites vulgaris Pierce............... ....... ... Tricolpites crassimurus (Groot and Penny) Singh ......... Tricolpites micromunus (Groot and Penny) Singh .......... Tricolpites sp.... ............ ...... Page 63 63 63 64 64 65 65 66 66 66 67 67 71 68 68 69 68 7O 70 70 Figure 1-3 160 PLATE 7 (All figures X750 unless otherwise stated) Aster0pollis asteroides Hedlund and Norris; single grains (Figures 1, 2) and cluster of grains (Figure 3); x1000.00.000000000000000.00000 ooooo coco-000000000000 Spinidinium vestitum Brideaux........ .............. ..... DinOpterygium Sp. A ...... ....................... ..... ... Spiniferites 8p. cf. S. cingulatus (0. Wetzel) Sarjeant................................ ................ Pareodinia sp. cf. 2. ceratophora Deflandre............. Deflandrea Sp. 1 ............ . ......... . ................. Deflandrea 3p. 2...... ............ ...................... 71 72 73 73 75 75 76 161 PLATE 7 162 PLATE 8 (A11 figures X750 unless otherwise stated) Page Palanperidinium cretaceum Pocock ............ . .......... 77 Hexagonifera sp. cf. 5. chlamydata Cookson and EisenaCk 00000 000000 00000000000000 00000000000 000000000 000 77 Odontochitina costata Alberti, emend. Clarke and verdiero000000000000000000000000000000000000 00000 0 000000 78 Pseudoceratium ? sp.; X500.............................. 79 Muderongia sp. 1; X500 ........ . ...... . ....... . ...... .... 80 Muderongia sp. 2; X500 ................ . ......... . ....... 81 163 PLATE 8 164 PLATE 9 (All figures X750 unless otherwise stated) Figure Page 1 ChlamydOphorella nyei Cookson and Eisenack ..... ......... 82 2 Oligosphaeridium anthophorum (Cookson and Eisenack) Davey ............. . ....... . ...... . ....... ........ ....... 82 3, 4 Oligosphaeridium complex (White) Davey and Williams; single Specimen (Figure 3) and detached Operculum composed of 4 plates (Figure 4) ......................... 83 5 Tanyosphaeridium sp. A.... ........... . ....... . .......... 83 6 Cleistosphaeridium multispinosus (Singh) Brideaux....... 84 7 Cyclonephelium sp. A... ................ .... ...... . ...... 85 8, 9 Baltisphaeridium sp.; X1000... .......................... 85 10, 11 Micrhystridium bifidum Davey; X1000 ....... . .......... ... 86 12 Micrhystridium fragile Deflandre; X1000.... .......... ... 86 165 PLATE 9 10 166 PLATE 10 (A11 figures X1000 unless otherwise stated) Micrhystridium inconspicuum (Deflandre) Deflandre ....... Micrhystridium Sp. cf. M. densispinium Valensi.......... Micrhystridium Sp. cf. M, piliferum Deflandre ........... Veryhachium Sp. cf. 1, eurogaeum Stockmans and Williere forma 1 Wall and Downie... ...... . .............. Leiofusa jurassica Cookson and Eisenack ...... . .......... PterospermOpsis australiensis Deflandre and Cookson..... Palaeostomocystis fragilis Cookson and Eisenack; X500... 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