bluuebunny/crossref_metadata_2025_split huggingface dataset:
The Lake Superior region and Trans-Hudson orogen
Authors: Anderson J. L. , Bauer R. L. , Chandler V. W. , Hanson G. N. , Kalliokoski J. , Morey G. B. , Mudrey M. G. , Ojakangas R. W. , Peterman Z. E. , Schulz K. J. , Shirey S. B. , Smith E. I. , Southwick D. L. , Schmus W. R. Van , Weiblen P. W. 
Published: April 2015

Abstract
Precambrian rocks in the Lake Superior region underlie all or parts of Minnesota, Wisconsin, and Michigan, an area along the southern margin of the Superior province of the Canadian Shield (Fig. 1). Except on the north, adjacent to Canada, the Precambrian rocks are overlapped by sedimentary strata of Paleozoic and Mesozoic age, which constitute a thin platform cover of relatively undisturbed rocks that thicken to the west, south, and east. Inliers of Precambrian rocks are exposed locally in southern Minnesota and Wisconsin, mainly in the flat valleys of major rivers, where erosion has cut below the Phanerozoic strata. The present landscape is subdued, and is inherited largely from Pleistocene continental glaciations, which produced a variety of erosional and depositional landforms. The glacier ice scoured the bedrock in the northern parts of the region, in much the same way as throughout most of Canada, and deposited materials of diverse lithology and provenance, as much as 200 m thick, over much of the remainder of the region. The Precambrian rocks in the region record an extended interval of crustal development and evolution that spans nearly 3 b.y. of earth history. This interval of geologic time is not continuously recorded in layered and intrusive units, but instead is punctuated by specific rock-forming and tectonic events that can be deduced from geologic relations and placed in a chronometric framework by isotopic dating. (Fig. 2, also see correlation chart for Precambrian rocks of the Lake Superior region, Morey and Van Schmus, 1986; and Bergstrom and Morey, 1985.)
The Wyoming province
Authors: Erslev E. A. , Frost C. D. , Karlstrom K. E. , Page N. J. , Zientek M. L. , Reed John C. , Snyder G. L. , Worl R. G. , Bryant Bruce , Reynolds M. W. , Peterman Z. E. 
Published: April 2015

Abstract
The Wyoming province is the region in Wyoming and adjacent states underlain by rocks of Archean age (Plate 2). It is an Archean craton bordered on the east and south by younger Precambrian provinces (Plate 1). Precambrian rocks are only exposed in the cores of the Laramide (Late Cretaceous to Early Tertiary) uplifts, and outcrops constitute less than 10 percent of the area underlain by Archean basement. Between uplifts, basement rocks are covered by thick Phanerozoic strata, so that extrapolations of geology from uplift to uplift are generally tenuous. Reconstructing the Archean history of the Wyoming province is further complicated by deformation associated with the late Mesozoic fold and thrust belt along the western margin. Although the Archean record is fragmentary, the basement uplifts generally afford excellent exposure.
The northern and northwestern margins of the Wyoming province are poorly constrained. Archean rocks are known as far north as the Little Rocky Mountains of Montana (Peterman, 1981). According to King (1976), Archean and Early Proterozoic dates are intermingled at the northwest margin of the province in a wide zone that exhibits a gradational change from Archean dates in central Montana to Early Proterozoic dates to the northwest, reflecting increasing influence of post-Archean thermal events.
The southwestern and southern margins of the Wyoming province are also poorly constrained. Archean rocks have been reported from several ranges in the Cordilleran orogenic belt, such as the Albion and Raft River Ranges (Armstrong and Hills, 1967) and possibly the Ruby Mountains of Nevada (A. W. Snoke, personal communication, 1986).
Transcontinental Proterozoic provinces
Authors: Anderson J. Lawford , Bender E. Erik , Anderson Raymond R. , Bauer Paul W. , Robertson James M. , Bowring Samuel A. , Condie Kent C. , Denison Rodger E. , Gilbert M. Charles , Grambling Jeffrey A. , Mawer Christopher K. , Shearer C. K. , Hinze William J. , Karlstrom Karl E. , Kisvarsanyi E. B. , Lidiak Edward G. , Reed John C. , Sims Paul K. , Tweto Odgen , Silver Leon T. , Treves Samuel B. , Williams Michael L. , Wooden Joseph L. 
Published: April 2015

Abstract
Research on the Precambrian basement of North America over the past two decades has shown that Archean and earliest Proterozoic evolution culminated in suturing of Archean cratonic elements and pre-1.80-Ga Proterozoic terranes to form the Canadian Shield at about 1.80 Ga (Hoffman, 1988,1989a, b). We will refer to this part of Laurentia as the Hudsonian craton (Fig. 1) because it was fused together about 1.80 to 1.85 Ga during the Trans-Hudson and Penokean orogenies (Hoffman, 1988). The Hudsonian craton, including its extensions into the United States (Chapters 2 and 3, this volume), formed the foreland against which 1.8- to 1.6-Ga continental growth occurred, forming the larger Laurentia (Hoffman, 1989a, b). Geologic and geochronologic studies over the past three decades have shown that most of the Precambrian in the United States south of the Hudsonian craton and west of the Grenville province (Chapter 5) consists of a broad northeast to east-northeast-trending zone of orogenic provinces that formed between 1.8 and 1.6 Ga. This zone, including extensions into eastern Canada, comprises or hosts most rock units of this age in North America as well as extensive suites of 1.35- to 1.50-Ga granite and rhyolite. This addition to the Hudsonian Craton is referred to in this chapter as the Transcontinental Proterozoic provinces (Fig. 1); the plural form is used to denote the composite nature of this broad region.
The Transcontinental Proterozoic provinces consist of many distinct lithotectonic entities that can be defined on the basis of regional lithology, regional structure, U-Pb ages from zircons, Sr-Nd-Pb isotopic signatures, and regional geophysical anomalies.
A Broader View
Authors: Ball Theodore T. , Lang Farmer G. , Hamilton Warren B. 
Published: April 2015

Abstract
The preceding chapters, which deal with myriad facets of the Precambrian geology of the conterminous United States, necessarily emphasize local descriptions and details. In this chapter we consider some broader regional and global relations. Hamilton discusses some of the difficulties with conventional views of the early evolution of the crust, and speculates that the geology of Venus, as elucidated by the new Magellan imagery, may provide a model for terrestrial Archean tectonics. Farmer and Ball describe the Nd-Sm isotopic system and discuss the applications of Nd-Sm studies to the determination of model crustal ages and delineation of major crustal provinces. Finally, we summarize the development of the southern part of Laurentia, the Late Proterozoic to early Paleozoic supercontinent that was fragmented during the Paleozoic and Mesozoic to produce the North American craton.
Geologic processes have changed greatly as the Earth has progressively lost heat, and plate-tectonic models that work well for the Phanerozoic (where my own expertise mostly lies) become progressively less applicable to successively older Precambrian assemblages. These models nevertheless can be fitted with reasonable success to Proterozoic geology, as Hoffman has been the leader in demonstrating; his 1989a paper provided excellent syntheses of the geology and tectonic significance of the Proterozoic tracts of Canada and the United States in such terms. Accretionary wedges, ophiolites, fore-arc and back-arc basins, oceanic and continental magmatic arcs, and rifted-margin sedimentary wedges are all recognizable in Proterozoic assemblages although different in important ways from modern ones.
Archean rock and tectonic assemblages are markedly less yet like modern ones. Although an increasing consensus (as, Hoffman, 1989a; until recently, I concurred) holds that Archean geologic processes also were dominated by plate tectonics, major features now appear to me inexplicable in such terms.
Ordovician and Silurian
Authors: Cecile M.P. , Norford B.S. 
Published: April 2015

Abstract
Most Ordovician and Silurian rocks in western and northwestern Canada were deposited on the North American craton and its western continental margin. Strata of these ages have also been recognized in three allochthonous terranes in the Cordillera, described in the companion volume on the Cordilleran Orogen (Gabrielse and Yorath, 1991).
The continental margin is equated with the Cordilleran Miogeocline of western Canada. The miogeocline/craton boundary is along a hinge line west of which the rate of thickening of Paleozoic strata increases significantly. On the basis of initial 87Sr/86Sr ratios for Mesozoic and younger plutonic rocks (Armstrong, 1979) that intrude them, all autochthonous Ordovician and Silurian strata, of both platformal and basinal facies, are inferred to be underlain by attenuated continental crust, and are thus in the miogeocline. Oceanic rocks are virtually unknown, and if present are either buried beneath younger strata, masked by metamorphism, and/or transported northwestward by Mesozoic and Cenozoic strike-slip faults. The only strata of this age that may be oceanic are rocks of the Kootenay Terrane in southernmost British Columbia.
The Cordilleran Miogeocline formed in Late Proterozoic to Early Cambrian time (see Bond and Kominz, 1984). It is considered to be a continental margin of Atlantic type that was affected by several periods of renewed extensional tectonism, one of which occurred during late Early Ordovician and Middle Ordovician time.
The eastern part of this ancient continental margin and adjacent craton were characterized by shallow-water, carbonate platforms and/or land areas composed mostly of exposed older Paleozoic and Precambrian
Devonian
Authors: Moore P. F. 
Published: April 2015

Abstract
The region described in this subchapter lies between the craton and the western edge of the carbonate platform built upon the Devonian continental shelf within one or two hundred kilometres of the continental margin. Sediments deposited west of the platform edge are described in the companion volume, “Geology of the Cordilleran Orogen in Canada” (Gabrielse and Yorath,1991). The depositional record described here starts with rocks deposited in Late Silurian time following a widespread regression accompanied by epeirogenic uplift, warping, and erosion. These rocks are the first of Kaskaskia sequence (Sloss, 1963). The record ends at the base of dark radioactive shales spanning the Devonian-Mississippian boundary and marking a major transgression. In the far north, this transgression is masked by a clastic wedge originating in the Ellesmerian Orogen of the Arctic Islands and northern Alaska.
Within the region, Devonian sediments cover an area of 2 500 000 km2. Thickness varies greatly from place to place. The thickest carbonate packets occur at the margin of the platform; close to Selwyn Basin, for example, the “Bear Rock sequence”, one of the five divisions of the Devonian analyzed here, alone constitutes over 2000 m of carbonate strata. In contrast, some bathymetric basins, such as the one occupying the Mackenzie Valley region during the Givetian, were starved of sediment.
Triassic
Authors: Gibson D.W. 
Published: April 2015

Abstract
Triassic rocks of the Interior Platform and eastern Cordillera of Canada have long been recognized as an interesting and variable sequence of marine strata occupying an elongate belt that extends from the United States border on the south to 69°N latitude and Beaufort Sea on the north (Fig. 4G.1, 4G.2). Triassic deposits are best developed in Western Canada Basin of British Columbia and Alberta, where they occupy three main physiographic provinces, Rocky Mountains on the west, Rocky Mountain Foothills, and Interior Plains to the east. Triassic rocks also occur in Liard River area of southern Yukon Territory and within northern Yukon Territory and District of Mackenzie in the British, Barn, Richardson, Selwyn, Wernecke, and northwestern Ogilvie Mountains. However, because much more published information on Triassic rocks in Western Canada Basin is available, and because of the greater development and economic importance of the system there, most of this report will be directed toward the region south of latitude 60°N.
Triassic rocks of the Rocky Mountains, Foothills, and Interior Plains comprise over 1200 m (Fig. 4G.1) of westward-thickening, siliciclastic and carbonate rocks and lesser amounts of evaporites. Contained marine faunas range in age from Griesbachian to Norian. The Triassic rocks of northern Yukon Territory display similar lithofacies but lack evaporites. The strata form a marine wedge deposited along a topographically low, tectonically stable continental shelf and shoreline, a continuation of Permian conditions at the passive western margin of the North American Craton. They form part of what is referred to as
Geomorphic Divisions
Authors: Stott D. F. , Klassen R. W. 
Published: April 2015

Abstract
Physiographically and geologically, western Canada consists of three great parts: a core of crystalline rocks forming the Canadian (Precambrian) Shield; a surrounding band of younger, essentially flat-lying, stratified rocks; and on the western side, a rim of highly deformed sedimentary, volcanic, and igneous rocks (Fig. 2C.1, 2C.2, 2C.3). The Canadian Shield has a slightly depressed centre, presently the site of Hudson Bay and Hudson Bay Lowland. The surrounding band of undeformed Phanerozoic rocks forms the Interior Plains on the western margin and St. Lawrence Lowland on the southern margin. These areas are characterized by lowlands, plains, and plateaux, which were substantially modified by glacial action during Pleistocene time. The outer belt of deformed rock forms the magnificent mountainous terrain of the Canadian Cordillera.
The classification of physiography in western Canada has evolved since the early writings of A.R.C. Selwyn and G.M. Dawson (1884) and a classic study by R.A. Daly (1912). The physiography of British Columbia was described by S.S. Holland (1964), and that of Canada by H.S. Bostock (1970a,b). These reports have been used extensively for the following summary. As part of the current syntheses of the Geology of Canada, W.H. Mathews (1986) has modified parts of the earlier classification of Cordilleran physiography, basing his study on landsat imagery and recent reports. The physiographic divisions set forth on Matthew’s geomorphic map are used in this section. A more detailed discussion of the geomorphology of the Cordillera may be found in the Cordilleran volume
Jurassic
Authors: Poulton T.P. , Braun W.K. , Brooke M.M. , Davies E.H. 
Published: April 2015

Abstract
The Jurassic System in western Canada is of interest particularly for the evidence it brings to bear on the early history of the mid-Jurassic to mid-Cretaceous Columbian orogeny, and for its economic significance. Its sediments contain the record of eustatic and epeirogenic events related partly to the early stages of the opening of the North Atlantic Ocean in the east, and the history of collision of allochthonous terranes in the west with the westerly drifting continent. Superimposition of the effects of the early phases of the Columbian Orogeny and the related foredeep on the older pre-orogenic sediments of Western Canada Basin, and the demise of Williston Basin as a depocentre are seen in the Jurassic succession of the western Plains and Rocky Mountains. Late events of the Ellesmerian tectonic phase in Brooks-Mackenzie Basin are recorded in northern Yukon Territory and adjacent Northwest Territories.
Jurassic sedimentary rocks form significant hydrocarbon reservoirs and source rocks in western Canada. The immense coal reserves of the southern Canadian Rocky Mountains occur in an Upper Jurassic-Lower Cretaceous succession; the Jurassic of southern Manitoba hosts two of Canada’s major gypsum mines; and some of the phosphate deposits, currently subeconomic, in southeastern British Columbia are Jurassic in age.
Cretaceous
Authors: Stott D.F. , Caldwell W.G.E. , Cant D.J. , Christopher J.E. , Dixon J. , Koster E.H. , McNeil D.H. , Simpson F. 
Published: April 2015

Abstract
Cretaceous rocks extend through the mid-continent from northern Yukon Territory and District of Mackenzie southward along Mackenzie and Rocky Mountains and eastward across the Plains of Alberta, Saskatchewan, and Manitoba to the Canadian Shield. They underlie Mackenzie Delta and Plains in the District of Mackenzie. Exposures of Cretaceous rocks are found in the southern Plains along many of the major river systems. One of the celebrated localities is at Dinosaur Park, southeastern Alberta, designated a World Heritage Site. Elsewhere in the Plains, Cretaceous rocks are mainly covered by Pleistocene drift, except in the Cypress Hills and along the Manitoba Escarpment on the eastern side of the basin.
Many investigations of Cretaceous rocks have been carried out over a period of more than 125 years. Studies of oil sands, heavy oil areas, and coal-bearing areas, regional and economic studies, and detailed surface and subsurface studies have contributed to understanding the history of these rocks. More than 100 000 boreholes have been drilled in the southern part of the Western Canada Basin. Well control is relatively sparse in the District of Mackenzie where, too, outcrops are lacking in large areas. Drilling in the Eagle Plains, Mackenzie Delta, and along the Mackenzie Valley has provided much needed data. Recent coal exploration in the foothills and mountains of British Columbia and in the Plains of Alberta and Saskatchewan has contributed greatly to the overall knowledge of the Cretaceous rocks.
Tertiary
Authors: Stott D.F. , Dixon J. , Dietrich J.R. , McNeil D.H. , Russell L.S. , Sweet A.R. 
Published: April 2015

Abstract
The depositional environments existing at the end of the Cretaceous Period continued into the Paleocene Epoch as the Laramide Orogeny continued to affect the western margin of the basin. Thick sequences of sediments derived from the Cordilleran Orogen were deposited in the Beaufort Sea in the north, while continental Paleocene beds were widely distributed in the south, spreading eastward from the rising Rocky Mountains across the Interior Platform.
The thickest Tertiary sediments in the southern part of Western Canada Basin are preserved along the eastern side of the Rocky Mountain Foothills and within the adjacent Alberta Syncline (Fig. 4J.1). These strata originally extended much more widely across the Interior Plains, but occur now only as erosional remnants, the largest being the Cypress Hills of southern Alberta and Saskatchewan (Fig. 4J.2) and their eastern extension along the Saskatchewan-United States border from Wood Mountain to Turtle Mountain in Manitoba. Tertiary sediments of the eastern Canadian Cordillera and Interior Plains are almost wholly continental, contrasting with the thick marine and nonmarine section encountered in the region of Mackenzie Delta and Beaufort Sea.
Tertiary sediments are extensively developed in Mackenzie Delta, Arctic Coastal Plain, and on the Arctic Continental Shelf. Limited exposures are found in the Caribou Hills on the eastern side of Mackenzie Delta (Fig. 4J.3), along the western margin of the delta, in the Richardson Mountains, and in a small area near Babbage River on Yukon Coastal Plain. Other occurrences are found in Bonnet Plume Basin, Brackett Basin near Norman Wells, and
Tectonic Framework
Authors: Aitken J.D. 
Published: April 2015

Abstract
This subchapter is concerned only with the tectonics affecting the Phanerozoic sedimentary cover of the Interior Platform, western basins, and eastern Cordillera and with those Upper Proterozoic deposits genetically related to them. Interpretation of the sedimentary and tectonic history of pre-Late Proterozoic time is subject to uncertainties much greater than those of Phanerozoic history, and Phanerozoic rocks are the principal focus of this volume. Precambrian tectonics as determined from stratified rocks is dealt with in Subchapter 4A, and the geology of the sparsely sampled and remotely sensed crystalline basement in Chapter 3. Furthermore, this subchapter is concerned only with those sedimentary successions that were deposited upon or in immediate connection with North America; the extremely complex history of the accreted terranes to the west is beyond the compass of this volume, and in any case is not recorded by the strata of the Western Canada Basin. The accreted terranes are fully treated by Gabrielse and Yorath (1991). In this subchapter only the most critical sources are cited; all significant literature is cited in Chapter 4.
The region of concern here has generally been treated as the Western Canada Basin, a term useful only in designating a geographic area underlain entirely by sedimentary rocks. Most of the “basin”, as conventionally outlined, was a tectonic and sedimentary platform (“shelf” of some authors) during the divergent-margin phases of sedimentation, a part of it was a platform during the convergent-margin phases, and it has been a tectonic platform for most of Tertiary time. where
Quaternary
Authors: Stalker A. MacS. , Vincent J.-S. 
Published: April 2015

Abstract
The Quaternary spans approximately the last two million years (Fig. 4K.1). In Canada, it is associated with glaciation, and the Interior Plains display a glacial record that may be unrivalled for detail and completeness. This review gives a synopsis of the period; a fuller account is found in Chapter 2 (Klassen, 1989; Vincent, 1989) of the Quaternary volume of this series (Fulton, 1989). That account also includes additional references, figures, and tables.
The Quaternary record of the Interior Plains is relatively rich, but still very incomplete. First, although much is known about the glaciations and some of the interglaciations, most of nonglacial time is probably unrecorded. Second, much of the region, and especially parts of northern Alberta, northeast British Columbia, and southern parts of the Northwest Territories, have not been mapped. This lack of information renders correlation between the better known southern Plains and the region near the Arctic coast extremely difficult. Third, the available information indicates little about climate and environment during most of the Quaternary Period.
Tectonic Evolution and Basin History
Authors: Aitken J.D. 
Published: April 2015

Abstract
The sedimentary cover of the North American craton in western Canada (see Fig. 5.5, in pocket) is in large part related to processes at the continental margins. It is in part the proximal deposits of continental terrace wedges, laid down on subsiding, divergent margins (miogeoclines), and in part the deposits of foreland basins depressed by the load of crustal and sedimentary rocks tectonically thickened at convergent margins. Evidence from the Omineca Belt of the Cordillera suggests that it may, in late Paleozoic to mid-Jurassic times, have been a back-arc basin, but that record cannot be read from the sediments of the Western Canada Basin. Certain disconformities and instances of stratigraphic condensation are probably related to the flexural bulge inboard of the foreland basin. An analogous, though less pronounced flexural bulge due to the sediment load at and inboard of divergent margins is expected, but has nowhere been identified beyond question.
On the other hand, the view of the authors, based on current information presented in this volume, is that the development of circumscribed Phanerozoic basins and arches well within the craton (Fig. 2D.2, 2D.3, 2D.4, 5.1) was independent of activity, whether convergent or divergent, at the continental margins. Contemporaneity of some events deep inside the craton with events at the margins may be apparent, rather than real, and plausible mechanisms for linkage of epicratonic movements with activity at the margins have not been proposed. The several arches and basins that were active during both convergent and divergent phases provide the