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North Horn Formation
The North Horn Formation is a widespread non-marine sedimentary unit with extensive outcrops exposed in central and eastern Utah. The formation locally exceeds 1100 m in thickness and is characterized by fluvial, lacustrine, and floodplain dominated lithologies, representing a terrestrial, high energy, depositional environment.〔Fouch, T. D., Lawton, T. F., Nichols, D. J., Cashion, W. B., Cobban, W. A. (1983). Patterns and timing of synorogenic sedimentation in Upper Cretaceous rocks of central and northeast Utah. In Reynolds, M. W., and Dolly, E. D., eds., Mesozoic paleogeography of west central United States. Society of Economic Paleontologists and Mineralogists. Pp. 305-336.〕〔Lawton, T. F. (1986). Fluvial systems of the Upper Cretaceous Mesaverde Group and Paleocene North Horn Formation, central Utah: A record of transition from thin-skinned to thick-skinned deformation in the foreland region. Paleotectonics and Sedimentatio in the Rocky Mountain Region, United States. AAPG Special Volumes, M 41. Pp. 423-442.〕〔Lawton, T. F., Talling, P. J., Hobbs, R. S., Trexler, J. H. Jr, Weiss, M. P., Burbank, D. W. (1993). Structure and stratigraphy of Upper Cretaceous and Paleocene strata (North Horn Formation), eastern San Pitch Mountains, Utah – sedimentation at the front of the Sevier orogenic belt. United States Geological Survey, Bulletin 1787-II, Pp. 1-33.〕 The sediments date from Late Cretaceous (Maastrichtian) to early Eocene in age and include the K-Pg extinction event boundary; however, this boundary is extremely difficult to locate and there is no strong stratigraphic evidence available that indicates a specific marker bed such as an iridium rich clay layer.〔Difley, R., Ekdale, A. A. (2002). Faunal implications of an environmental change before the Cretaceous-Tertiary (K-T) transition in central Utah. Cretaceous Research, 23:315-331.〕〔Myung-Suk, Y., Cross, A.T. (1997). Palynostratigraphy of Upper Cretaceous-Lower Tertiary strata, Price Canyon, Utah. Review of Palaeobotany and Palynology 97, p.53-66〕 Thus far, the only visible evidence is represented in the form of faunal turnover from dinosaur to mammal-dominated fossil assemblages. Taxa from the Cretaceous part of the formation include squamates, testudines, choristoderes, crocodyliforms, shark, fishes, amphibians, mammals, dinosaurs, eggshell fragments, trace fossils, molluscs, plant macrofossils, such as wood fragments, and palynomorphs.〔Gilmore, C.W. (1946). Reptilian fauna of the North Horn Formation of central Utah. United States Geological Survey Professional Paper, 210-C, 53 p〕〔Cifelli, R.L., Czaplewski, N.J., Rose, K.D. (1995). Knowledge of Paleocene Mammals from the North Horn Formation, Central Utah. The Great Basin Naturalist. Vol. 55:4. Pp. 304-314〕〔Cifelli, R.L., Nydam, R.L., Eaton, J.G., Gardner, J.D., Kirkland, J.I. (1999). Vertebrate Faunas of the North Horn Formation (Upper Cretaceous-Lower Paleocene), Emery and Sanpete Counties, Utah. In Gillette, D.D. (ed.) Vertebrate Paleontology in Utah. Utah Geological Survey Miscellaneous Publication 99-1: 377-388〕 Characteristic dinosaur taxa include the ceratopsian ''Torosaurus utahensis'', the titanosaurid sauropod ''Alamosaurus sanjuanensis'', and the theropod ''Tyrannosaurus rex'';〔Sampson, S.D., Loewen, M.A.(2005). Tyrannosaurus rex from the Upper Cretaceous (Maastrichtian) North Horn Formation of Utah: biogeographic and paleoecologic implications. Journal of Vertebrate Paleontology 25:2, 469-472〕 however, the most frequently occurring taxon in the Cretaceous strata of the North Horn Formation is the teiid squamate ''Polyglyphanodon''.〔 Fauna recorded from Paleocene strata within the formation appear to be far more diverse and over 70 different taxa have been identified, including frogs, numerous multituberculate, protoeutherian, periptychid, arctocyonids and phenacodontid mammals, crocodyliforms, choristoderes, trace fossils, and palynomorphs.〔〔〔
==Stratigraphy and sedimentology==
The North Horn Formation is a non-marine, stratigraphic unit located in east and central Utah which unconformably overlies the Late Cretaceous Price River Formation west of the San Rafael Swell, and the Tuscher Formation east of the swell.〔 The formation is overlain by the late Paleocene-early Eocene Flagstaff Formation, also called the Flagstaff Limestone.〔〔 The North Horn type section is located on North Horn Mountain in Emery County, Utah.〔Spieker, E. M. (1946). Late Mesozoic and early Cenozoic history of central Utah. United States Geological Survey. Professional Paper 205-D, 117-159〕 Laterally, the North Horn Formation nearly spans a 140 km long east-west transect that extends from the Wasatch Plateau on the west and the Book Cliffs, near Green River, on the east, separated in the middle by the San Rafael Swell.〔 The North Horn Formation varies greatly in thickness and lithology, representing a time transgressive stratigraphic sequence, which means that the age of the base and top of the formation changes as one moves laterally. West of the San Rafael Swell, near Price Canyon, Utah, the basal contact for the North Horn Formation is Maastrichtian (latest Cretaceous) in age 〔〔〔 whereas its base is Paleocene in age on the eastern side of the swell.〔 Some of the most complete sections of the North Horn Formation are exposed west of the San Rafael Swell at North Horn Mountain in which the local stratigraphy sometimes exceeds in thickness. Further to the east, towards Green River, Utah, stratigraphic sections are significantly thinner compared to sections in the west with thicknesses varying between as little as .〔〔
The formation is divided into three informal units based on broad but distinct lithological characteristics. These units include the lower variegated unit at the base, a middle coal unit (in which the K-Pg boundary is located), and the upper variegated unit at the top. The units themselves are further divided into a total of eight sub-units, or lithofacies, based on facies scale lithological features.〔〔〔 A detailed sedimentary study of the North Horn Formation was conducted by Lawton et al.〔 These units, from oldest to youngest, include a thick basal conglomerate unit that consists of an upward fining conglomerates and sandstone and lacks any interbedded shale, followed by the lower redbed unit, a thick sequence dominated by red sandy siltstone, conglomerate, and pebbly sandstone. The third unit is the sheet sandstone unit and is composed of sheetlike sanstone beds that are interbedded with gray and carbonaceous siltstones. Some limestone beds are present but are uncommon. The fourth unit is characterized by thick coal beds and coal-streaked siltstone deposits and are referred to as the coal-bearing unit. This unit is overlain by a thick sequence of primarily calcareous siltstone beds, called the calcareous siltstone unit. The big mountain unit consists of nearly 230 m of interbedded conglomerates and trough cross bedded sandstones, followed by a thick set of strata composed of sandstone, pebbly sandstone, and conglomerates which make up the coal canyon unit. The uppermost unit is the upper redbed unit, which is nearly a thick and is composed of red brown mottled siltstone and sandy siltstone.
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