bluuebunny/crossref_metadata_2025_split huggingface dataset:
Petroleum
Authors: Johnson R.D. , McMillan N.J. 
Published: April 2015

Abstract
Petroleum has been discovered in commercial quantities in two major sedimentary basins of the Western Interior: Western Canada Basin and Beaufort-Mackenzie Basin. Western Canada Basin comprises the Phanerozoic sedimentary wedge lying between the Canadian Shield and the Cordillera; it includes the thrust-faulted rocks of the Foothills Belt but not the Rocky, Mackenzie, and Ogilvie mountains. This vast basin extends from the 49th parallel northward beyond the Arctic Circle (Fig. 6 A.1). Western Canada Basin is divided into the following regions: Alberta Basin, Williston Basin, Foothills Belt, and Northern Basins. Beaufort-Mackenzie Basin straddles the Arctic coastline north of Western Canada Basin; a summary description is given in this subchapter but its geology and economic potential are described more fully in the companion volume on the Arctic Region (Grantz et al., 1990).
The distribution of oil and natural gas in western Canada south of latitude 60°N is shown on two pocket figures (Maps 1558A, 1559A), which may be used to locate fields referred to in the text. The maps are coloured to show the geological age of the reservoirs. Marginal notes contain statistical data on the largest pools, including Initial Volume In Place (IVIP), initial recoverable oil (Initial Established Reserves (IER)), pool area, net pay, porosity, and discovery year. Pie diagrams show the initial volume and the initial reserves, and the initial reserves by age of reservoir (see also Fig. 6 A.2, 6A.3). For current statistical data on reserves and production for individual fields, the annual summaries published by the provincial regulatory
Geophysical and petrological Characteristics of the basement rocks of the Western Canada Basin
Authors: Burwash R.A. , Green A.G. , Jessop A.M. , Kanasewich E.R. 
Published: April 2015

Abstract
Precambrian basement underlying the Interior Plains is a lateral extension of the exposed Canadian Shield. From the trend and width of most of the major tectonic units of the western part of the shield it can be inferred that they extend some distance beneath the sedimentary cover. Recognition of these units on the exposed part of the shield has been based primarily on geological mapping combined with studies of structural style, metamorphic fabric and facies, geochronology, and geophysical characteristics. In those areas of the Shield with an extensive cover of Pleistocene deposits, geophysical surveys have served to trace the boundaries of distinctive rock units. In sedimentary platforms with moderate Phanerozoic cover, geophysical maps are the only practical means of tracing the boundaries of major units. Core samples from wells drilled to basement provide information on rock assemblages, metamorphic history, geochronology, and petrophysical characteristics, but yield little of the detailed structural information that can be obtained from outcrop.
The objectives of this chapter are to present the currently available geophysical and petrological data that characterize the major tectonic units of the basement beneath the Western Canada Basin. An attempt is made to draw a map of the basement within the framework of the structural geology of North America.
The western limit of the crystalline rocks of the Canadian Shield was first shown with reasonable accuracy on a map drawn by Sir John Richardson in 1851 (Kupsch, 1979). In his travels from Hudson Bay to the Interior Plains of western Canada, Richardson
Coal
Authors: Cameron A.R. 
Published: April 2015

Abstract
Over 95% of Canada’s known coal resources are found in the sedimentary basins of the Interior Platform and eastern Cordillera (Fig. 6B.1); a minor amount is found in the Moose River Basin of the Hudson Platform. This distribution is shown in Table 6B.1, which summarizes coal resources for all of Canada. Coal also occurs in the platforms and basins of western Northwest Territories, eastern and northern Yukon Territory and the Arctic Islands, but low exploration activity has limited calculation of regional resources. The coals range in rank from lignite to anthracite and in age from Early Carboniferous to Tertiary.
An interesting pattern of resource distribution by rank is shown by Table 6B.1. A large proportion is subbit-uminous and lignite - valuable as fuels for power generation and possible future feedstocks for gasification and liquefaction. High-volatile bituminous coals constitute a relatively small percentage of total resources. On the other hand, Canada is well endowed with medium- and low-volatile bituminous coals, and these are of special interest to the metallurgical market. Of Canada’s total resources of immediate interest probably 25% are in the medium/low-volatile bituminous category, virtually all of which are in Alberta and British Columbia.
Coal in western Canada has gone through periods of fluctuating fortunes paralleling the experience of the industry elsewhere in North America. During the late 1950s and early 1960s, production decreased markedly and many mines closed. In the late 1960s and the decade of the 70s, a resurgence in mining took place due to increased exports of
Geothermal Energy
Authors: Jessop A.M. 
Published: April 2015

Abstract
Geothermal sources in sedimentary basins are of moderate to low temperature, are associated with flat-lying or gently dipping sediments, extend over long distances, and take the shape of the layered host rocks. They contrast with geothermal fields on continental margins associated with subduction zones or of rift zones associated with crustal extension; these are the result of vigorous hydrothermal systems feeding on volcanic heat sources, are relatively localized, generally small, irregular in shape, and of diverse character.
Geothermal heat may be recoverable from almost any part of the sedimentary section because mobile water is present to some extent in all sediments with the exception of halite and other evaporite beds. However, the amount of water, its temperature, chemical character, pressure, and potential production rate may vary considerably from place to place, even in the same aquifer. Porosity and permeability of the rock are factors that affect the pressure drawdown and the lifetime of any production well. Thus, the economic geothermal potential must be individually evaluated at any proposed location.
Temperatures in sedimentary aquifers range from near zero to 150°C and possibly higher in very deep basins. The lower limit of utility is about 40°C, which corresponds to a depth of about 500 to 1500 m, depending on surface temperature and geothermal gradient. Geothermal gradient in sediments is often distorted by hydrological effects, and conductive heat is disturbed by convective heat transfer. Areas of relatively high surface elevation act as recharge zones, depressing subsurface temperature, and low areas act as discharge
Industrial Minerals of the Western Canada Basin
Authors: Guliov P. 
Published: April 2015

Abstract
The Western Canada Basin is a storehouse of vast industrial mineral wealth. All of the Phanerozoic systems are represented in the basin and most of them have contributed or have the potential of contributing useful industrial mineral commodities. Producing deposits and significant occurrences are scattered throughout the more populous southern region of the basin (Fig. 6D.1, 6D.2). Commodities of low value such as sand and gravel, brick clay, and expandable clays tend to be relatively common and widespread. Development of these therefore tends to be concentrated around urban centres close to markets. Others, such as refractory clays, gypsum, cement raw materials, and lime are processed or used in manufacturing end products, whose added value permits transportation over relatively long distances. Some commodities, potash and sulphur for example, have gained global significance.
Production of industrial minerals in the Western Canada Basin accounts for about 65% of the total value of Canadian production, of which about 75% is contributed by sulphur and potash (Table 6D.1). Reviews of industrial minerals have been published recently for Manitoba (Bannatyne, 1984a; Davies et al., 1962; Fogwill, 1983), for Saskatchewan (Guliov, 1984; Saskatchewan Energy and Mines, 1983) and for Alberta (Hamilton, 1976, 1984). An earlier summary of the industrial minerals of the western provinces was published by Douglas (1970).
Groundwater in the Interior Plains Region
Authors: Lennox D.H. 
Published: April 2015

Abstract
The Canadian Interior Plains lie between the Canadian Cordillera on the west and the Canadian Shield on the east and extend as far north as the Arctic Ocean. The Interior Plains Hydrogeological Region is defined as that part of the Canadian Interior Plains that lies to the south of the southern limit of discontinuous permafrost.
The Interior Plains Hydrogeological Region and adjacent areas to the north were divided by Bostock (1970) into seven physiographic subregions (Fig. 6F.1). The three largest of these, Manitoba, Saskatchewan, and Alberta plains, are separated from one another by two pronounced west-to-east downward steps in the terrain, the Missouri Coteau and Manitoba Escarpment. To the north of Alberta Plain lie three somewhat smaller subregions: Alberta Plateau, Peace River Lowland, and Fort Nelson Lowland. The smallest of the seven subregions, Cypress Hills, rises 700 m above the surrounding Alberta Plain just north of the International Boundary.
Surface elevations in the region range from 1500 m next to the Rocky Mountain Foothills belt to 150 m at the eastern boundary. The Manitoba Plain is very gently undulating to flat, with an average elevation of about 250 m above sea level (Bostock, 1970). Average elevation increases successively in the Saskatchewan and Alberta plains, as does the amount of local relief. This trend continues into the Alberta Plateau to the northwest. In the Alberta Plain the average elevation is 750 m and river valleys are entrenched to 100 m or more beneath the surrounding terrain. Elevations in some upland areas, such as the Neutral Hills and Porcupine Hills, exceed 1000 m (Fig. 6F.2).
Hudson Platform – Introduction
Authors: Norris A.W. 
Published: April 2015

Abstract
Hudson Platform, in the central part of the Canadian Shield, covers an area of 971 250 km. Its margins have been greatly eroded, so that most of its sedimentary cover now resides in two linked cratonic basins, Hudson Bay Basin and Moose River Basin. Most of this area is covered by water of Hudson and James bays (608 650 km2). Onshore in the south, parts of the platform form Hudson Bay Lowland (323 750 km2) and in the north, Southampton, Coats, and Mansel islands form Southampton Plain (38 850 km2).
A northeast-trending positive area, Cape Henrietta Maria Arch (Sanford et al., 1968; the Patricia Arch of Nelson and Johnson, 1966) divides Hudson Platform into two Phanerozoic sedimentary basins, Moose River Basin in the southeast and Hudson Bay Basin in the northwest (Fig. 7.1, 7.2). These basins are largely defined by post-Devonian movements; their largely common histories involve periods in which they were depocentres alternating with periods in which they were parts of a vast, undifferentiated platform. Thus, the two basins are in part depocentres, in part syndepositional and post-depositional structural basins, and in part basins of preservation. The most reliable thickness measurements are those based on drilling. In Moose River Basin, which developed within the platform somewhat later than Hudson Bay Basin, Ordovician, Silurian, Devonian, Middle Jurassic, and Lower Cretaceous rocks have a total thickness of about 760 m in the central part.
St. Lawrence Platform – Introduction
Authors: Sanford B.V. 
Published: April 2015

Abstract
The St. Lawrence Platform borders the Canadian Shield in southeastern Canada and adjacent areas of the United States, and is in turn bounded on the south by the Appalachian Orogen (Fig. 10.1). The Upper Precambrian to Carboniferous (and locally Jurassic) rocks within the platform consist of carbonates, shales, evaporites, and sandstones that dip at low angles southward, either into Michigan Basin, or into Allegheny, Quebec, and Anticosti foreland basins that parallel the Appalachian structural front (Fig. 10.2, see also Sanford et al., 1979). The strata are for the most part undeformed but are locally folded and faulted. Deformation is most evident near the southeastern platform margin where the beds were complexly faulted and folded by overriding thrust slices during various episodes of Paleozoic orogeny.
This account provides a summary of the depositional and tectonic history of the region. Brief reference is made to events in the Appalachian Orogen, Hudson Platform, Interior Platform, and adjoining regions of the United States. For complete treatment of these regions, the reader is referred to the appropriate chapters of this volume, and to the companion volumes of the Decade of North American Geology series (Williams and Neale, in prep.; Sloss, 1988).
St. Lawrence Platform — Geology
Authors: Sanford B.V. 
Published: April 2015

Abstract
Precambrian rocks of the Canadian Shield extend into the subsurface to form the basement beneath Paleozoic rocks of St. Lawrence Platform and St. Lawrence Trough (Fig. 11.1), where they were in part involved in Taconian, Acadian, and Alleghenian orogenic deformation. The southeastern boundary of the Precambrian basement beneath the Appalachian Orogen is unknown, but is assumed to coincide roughly with the southeastern limit of anomalous concentrations of seismic events (Sanford et al., 1985; Fig. 10.2).
Evolution of St. Lawrence Platform and its periodic connections with the Hudson and Interior platforms were linked with Paleozoic plate-tectonic events at the eastern margins of the North American continent (which at that time included Greenland).
Two major tectonic cycles are recorded: Tectonic Cycle I, extending from late Precambrian to late Paleozoic time, and Tectonic Cycle II, extending from early Mesozoic to the present (Fig. 11.2).
St. Lawrence Platform – Economic Geology
Authors: Sanford B.V 
Published: April 2015

Abstract
The principal economic deposits of the Paleozoic formations of St. Lawrence Platform are non-metallic, the most important being limestone and dolostone, salt, oil and gas, shale, gypsum, and sandstone in that order. Carbonate rocks also have some potential as hosts to metallic deposits, such as lead, zinc, and cadmium.
Proterozoic Sedimentary Rocks
Authors: Aitken J.D. 
Published: April 2015

Abstract
Over vast areas of the undeformed platform of southwestern Canada, the sedimentary cover of the ancient North American Craton is entirely of Phanerozoic age. In northwestern Canada, on the other hand, thick Proterozoic strata intervene between Phanerozoic deposits and crystalline basement (Fig. 4A.1). Even there, the preserved sediments contain only a fraction of the record of geological events that is preserved in the Foreland Belt of the Cordillera.
Precambrian crystalline rocks beneath the sedimentary cover of the Interior Platform are dealt with in a separate chapter (Burwash et al., Chapter 3 in this volume). This brief treatment is largely a condensation of two chapters (“Middle Proterozoic”, and “Upper Proterozoic”) of the companion volume, “Geology of the Cordilleran Orogen in Canada” (Gabrielse and Yorath, 1991); it considers not only the Proterozoic sedimentary record of the undeformed basins and platforms, but also the more complete record preserved in the Eastern Cordillera.
H. Gabrielse and M.E. McMechan have provided welcome assistance with fact and interpretation.
Evolutionary Models and Tectonic Comparisons
Authors: Aitken J.D. 
Published: April 2015

Abstract
This chapter attempts comparisons among the various sectors of the Phanerozoic platforms and basins of North America (Fig. 13.1) and among the various sectors of the frontal parts of the outboard orogens, whose behaviour has profoundly influenced the sedimentary record of the former. The syntactical difficulties of making comparisons among more than two entities are formidable; accordingly, a graphical summary is also provided (Fig. 13.2). Each column of the graphical summary is a generalization of an entire transect of a platform, basin, or frontal orogen; it thus contains numerous half-truths and serves mainly to highlight coincident and non-coincident events. The graphical summary should not be treated as a source of data.
Cambrian and Lower Ordovician - Sauk Sequence
Authors: Aitken J.D. 
Published: April 2015

Abstract
The Western Canada Basin provides exceptional opportunities for the study of Cambrian and Lower Ordovician rocks. In the southwest, these rocks are part of the Cordilleran Miogeocline, the wedge of sedimentary and minor volcanic rocks deposited on a passive margin of western North America that came into being at about the beginning of the Cambrian (Fig. 4B.1). In the northeast, they form the purely sedimentary and much thinner cover of the Interior Platform. Although it is clear that a hinge line marked the transition from platform to miogeocline, the position of the hinge is difficult to locate precisely, even for small chronostratigraphic units, because of the vagaries of preservation and the uneven distribution of thickness data. In any event, the position of the hinge line was not fixed. The best approximation of its long-term average position is the eastern limit of Mesozoic deformation.
The unit chosen for analysis here is the Sauk Sequence of L.L. Sloss (1963, 1976), the record of a long period of almost continuous sedimentation on the cratons, limited below by a widespread unconformity near the base of the Cambrian and above by a widespread unconformity near the base of the Middle Ordovician. Sub-sequences I, II, and III are demarcated by relatively subtle breaks at the base of the Middle Cambrian and the base of the Franconian.
The present synthesis provides a descriptive summary, and emphasizes the striking differences seen between cross-sections from platform to miogeocline drawn through the southern Rocky Mountains, the northern Rocky Mountains, the
Precambrian Successions in the Northernmost Part of the Canadian Shield
Authors: Frisch T. , Trettin H.P. 
Published: April 2015

Abstract
This chapter summarizes information on the northernmost parts of the Shield relevant to the understanding of the early history of the Innuitian region; a systematic description of the Canadian Shield and Greenland can be found in another volume of this series (Hoffman et al., in prep.). From a stratigraphic point of view, the Shield is divisible into crystalline basement, metamorphosed in Archean and/or Early Proterozoic time, and unconformably overlying sedimentary and volcanic successions of Proterozoic age that are only slightly deformed.
The following section describes briefly the crystalline basement rocks at the margin of the Arctic Platform, proceeding from southwest to northeast. Regional metamorphic facies of the Canadian part have been compiled by Fraser et al. (1978).
Victoria Island. Granodiorite on the northeast side of the Minto Arch yielded a’ K-Ar age of 2391 ± 125 Ma (recalculated from Lowdon et al., 1963), suggesting that it may be part of the original Slave Province. This interpretation is supported by the inferred Early Proterozoic age of unconformably overlying sediments (Campbell, 1981; see below). A later thermal event, however, is apparent from the 1645 ± 20 Ma K-Ar age on a pegmatitic granite in the Wellington High (W.A. Gibbins, quoted by Campbell and Cecile, 1979).
Boothia Peninsula, Somerset Island and Prince of Wales Island. The Precambrian core of the Boothia Uplift (Fig. 4.2, 4.3) consists of quartzofeldspathic, pelitic, calcareous, and mafic rocks metamorphosed largely in the transitional granulite facies (Blackadar, 1967; Brown et al., 1969). Structural trends are northerly on
Cambrian to Silurian Basin Development and Sedimentation, North Greenland
Authors: Higgins A.K. , Ineson J.R. , Peel J.S. , Surlyk F. , Sønderholm M. 
Published: April 2015

Abstract
The Franklinian Basin extended from northern Ellesmere Island across North Greenland, where its sedimentary infill is exposed from Inglefield Land and Washington Land in the west to Kronprins Christian Land in the east (Fig. 7.1–7.3). The segment of the basin exposed in North Greenland is approximately 800 km long and has a maximum preserved north-south width of 200 km. The thickness of the sedimentary column reaches about 8 km; the main part of the succession is of Cambrian-Silurian age, but it may extend down into the latest Precambrian and up into the earliest Devonian. A distinction into a shelf sequence and deep water trough sequence can be recognized in northern Ellesmere Island and in North Greenland, and the variations in facies with time in the two regions show close parallels. Correlation on group or formation level is often possible across Nares Strait (Peel and Christie, 1982; Peel et al., 1982). Detailed knowledge of the North Greenland sequences, however, permits an integrated account of shelf and trough development in the North Greenland segment of the Franklinian Basin.
A craton composed of Archean and Upper Proterozoic crystalline basement rocks, overlain by Middle and Upper Proterozoic sedimentary and volcanic rocks, lies to the south of the Franklinian Basin (Chapter 6). This is now exposed intermittently along the margin of the Inland Ice, and more extensively in eastern North Greenland (Fig. 7.1). In the early Paleozoic, this craton was fringed to the north by an east-west trending shallow marine shelf, Two main facies belts
Cambrian to Early Devonian Basin Development, Sedimentation, and Volcanism, Arctic Islands
Authors: Trettin H.P. , Mayr U. , Long G.D.F. , Packard J.J. 
Published: April 2015

Abstract
Two first-order depositional provinces are distinguished — a southeastern shelf, which encompasses nearly all of the Arctic Platform and a large part of the Franklinian mobile belt, and a northwestern deep water basin. The latter, in turn, is divisible into a southeastern sedimentary subprovince, and a northwestern sedimentary and volcanic subprovince. The unstable boundary between deep water basin and shelf migrated cratonward from late Early Cambrian to Early Devonian time.
In the preceding chapter, the Cambrian to Silurian depositional history of North Greenland has been divided into seven evolutionary phases that are applicable to both shelf and deep water basin as they are based, to some extent, on shifts of their mutual boundary. This organization was feasible because in Greenland only northern parts of the shelf province, which have been affected markedly by the cratonward expansion of the basin, are exposed.
Separate schemes for shelf and basin, however, are required in the Arctic Islands where both provinces are more extensive and more complex stratigraphically. It is most convenient to discuss the stratigraphy of Franklinian Shelf and Arctic Platform in terms of informal time-rock slices, and that of the deep water basin in terms of unrelated, variably diachronous, informal rock units. The basic differences in the stratigraphic record of the two provinces reflects the fact that different geological processes are important in them. Eustatic fluctuations in sea level, for example, affect primarily the shelf; tectonic events in “outboard” orogenic belts affect primarily the basin.
The different classifications chosen in Chapters 7