bluuebunny/crossref_metadata_2025_split huggingface dataset:
Continent-ocean transitions in western North America between latitudes 46 and 56 degrees
Authors: Monger J.W.H. , Clowes R. M. , Cowan D. S. , Potter C. J. , Price R. A. , Yorath C. J. 
Published: April 2015

Abstract
This chapter is intended to supplement rather than reproduce material presented in Transects B-1, B-2, and B-3 and their accompanying texts, although some overlap is unavoidable, particularly in summary descriptions of major lithological and structural packages that form the crust of this segment of the Cordillera. The chapter discusses results of recent studies by COCORP within the east-central part of the corridor of transect B-3A, and by LITHOPROBE within the corridors of B-2 and B-3A on and west of Vancouver Island and between B-2 and B-3 A in the east-central Cordillera (Fig. 1). The new results confirm the general principles on which the transects were constructed but constrain depths and attitudes of major lithological packages and structures and provide insights into processes within deeper parts of the crust.
Transects B-1, B-2, and B-3 lie in the segment of the Cordillera that includes the southern half of British Columbia and Alberta in Canada, and Washington, northern Idaho, and Montana in the United States (Fig. 1). Each transect emphasizes a somewhat different aspect of Cordilleran geology. Transect B-1 (Yorath and others, 1985c) extends through a region between latitudes 51°N and 56°N and longitudes 126°W to 133°W. It exploits relatively abundant data in the offshore region to illustrate complex interactions near the plate junction between the Explorer (northern subplate of the Juan de Fuca Plate), Pacific, and North American plates and extends eastward across the granitic and high-grade metamorphic terrane of the Coast Mountains to terminate in the volcanogenic and sedimentary terranes of
Continent-ocean transition in Alaska
Authors: Moore Thomas E. , Grantz Arthur , Roeske Sarah M. 
Published: April 2015

Abstract
Alaska is the eastern, subaerial part of a large subcontinent of distinctive tectonic character that serves as an isthmus between nuclear North America, with its fringing belt of allochthonous terranes, and the accreted terranes and volcanic belts that constitute northeastern Russia. Physiographically, this subcontinent, which we name Denalia, is a bulge in the continental platform in the vicinity of Alaska, the Chukotsk Peninsula, and the broad continental shelf of the Bering Sea. The bulge is convex to the south and is bounded on the east and west by constrictions in the width of the continental platform and on the north and south by the edge of the continental shelf (Fig. 1). Tectonically, Denalia is characterized by geologic youthfulness and complexity, an abundance of convergent and transcurrent faults, and absence of autochthonous cratonic rocks. It contains a profusion of lithotectonic terranes of diverse origin and age that were emplaced in late Mesozoic and Cenozoic time. In addition, it includes the superimposed Cenozoic Aleutian arc and subduction zone and the Queen Charlotte-Fairweather transform fault system. Parts of Denalia were created by pre-middle Mesozoic tectonic events, but these took place elsewhere, before the affected rocks were tectonically transported and incorporated into the landmass of Denalia. Except for a small area in the Porcupine Plateau region along the Alaska-Yukon boundary, the only Precambrian rocks that have been recognized in the subcontinent are in tectonically emplaced fragments, the largest of which is the Arctic Alaska terrane in the Brooks Range, Arctic Foothills, and Arctic Foothills
The polar continent-ocean transition in Canada (Corridor G)
Authors: Sweeney J. F. , Mayr U. , Sobczak L. W. , Balkwill H. R. 
Published: April 2015

Abstract
The Canadian Arctic transect corridor (Corridor G) extends across a wide range of geologic settings. In the south at Somerset Island, Archean crystalline rocks of the craton are exposed (Fig. 1). Northward across Cornwallis and Devon Islands the crystalline rocks are covered by Proterozoic and early Paleozoic platform deposits that were uplifted, eroded, and deformed in Silurian through Early Carboniferous time. Overlying these rocks between Devon and Ellef Ringnes Islands are late Paleozoic and Mesozoic strata of the Sverdrup Basin. These strata were locally deformed by evaporite diapirism and repeated episodes of mafic igneous intrusion and, east of Corridor G, were regionally deformed in latest Cretaceous and Paleogene time. Northwest of Ellef Ringnes Island the corridor traverses the latest Cretaceous and younger clastic terrace wedge that covers the continental margin of the Canada Basin. The corridor terminates at abyssal depths over the continental rise.
The corridor was selected to incorporate deep crustal seismic results between Cornwallis and northern Ellef Ringnes Islands (Sander and Overton, 1965; Hobson and Overton, 1967) and offshore refraction and reflection work along the east coast of Ellef Ringnes Island (Sobczak, 1982; Sobczak and Overton, 1984). Phanerozoic strata are almost completely represented along the corridor, and reflection seismic data (courtesy of Panarctic Oils Ltd., Calgary) locate stratigraphic horizons at several points. Borehole data are available for Cornwallis, Bathurst, Amund Ringnes, and Ellef Ringnes Islands, and there is regional coverage by gravity (Sobczak, 1978) and aeromagnetic (Coles and others, 1976) data, including detailed measurements in the Sverdrup Basin
Rifted continental margins of North America
Authors: Sawyer Dale S. 
Published: April 2015

Abstract
During the late 1970s, the study of rifted margins was changed fundamentally by the recognition that simple models of thinning of continental lithosphere could account for many features of the subsidence observed on rifted or passive continental margins (McKenzie, 1978). The 1980s have produced at least three major new foci of research in the study of such margins and continental rifting in general. These new directions have emerged partly as a result of new data acquisition, primarily deep penetration seismic reflection profiling and complementary long offset seismic reflection-refraction experiments on rifted margins worldwide, and partly as a result of the application of land geologic observations of continental rifts to the study of margins.
The first of these new directions was the recognition of the importance of low-angle normal faulting in continental rifting. This avenue of research has changed our expectations of the large-scale patterns of rifting and rifted margin formation. We had come to expect that most rifts should be symmetric and that, upon plate reconstruction, conjugate rifted margins would also show symmetry at the time of initiation of sea-floor spreading. A number of investigators (Wernicke, 1981Wernicke, 1985; Lister and others, 1986) observed asymmetry in the shallow structures in continental rifts, and extended this idea to the whole lithosphere scale. The new model, usually referred to as the simple shear or delamination model, concentrates shearing along narrow zones at low angle to the surface and through the continental lithosphere. Most of the strain during continental extension takes place within this
Transects of the ancient and modern continental margins of eastern Canada
Authors: Haworth Richard T. , Keen Charlotte E. , Williams Harold 
Published: April 2015

Abstract
The continental margin transect program evolved through a desire to define the specific characteristics of North America’s modern continental margins and to compare the modern margins with Paleozoic examples, now found within the continent. Thus, the features of modern margins can be used to locate and elucidate the structures of ancient analogues. Conversely, the exposed rocks of ancient margins provide an insight into the evolution and deep structures of modern examples. Ocean-continental transitions, rifting mechanisms, development of sedimentary basins, processes of continental breakup, and ancestral controls are all features that warrant comparison between modern and ancient examples.
The Atlantic coast has the best-known passive margin of North America. Inboard of it is the Appalachian Mountain chain, which records a clear history of late Precambrian rifting and the passive development of a Paleozoic continental margin. Transects across both these modern and ancient examples provide information on scale and detail that is useful for comparisons.
The modern continental margin of eastern Canada (Fig. 1a, 1b) has a wider variety of ages and styles than that of its eastern United States counterpart. Segments of the margin southeast of Nova Scotia and east of Labrador are typical of rifted margins, though of different ages. Between them lies the tortuous segments of the northern and eastern Grand Banks where rifting and subsidence occurred over a broad area of the continental shelf. In contrast, the southern boundary of the Grand Banks is a transform segment. Rocks of the Appalachian Paleozoic margin are best preserved and exposed
Proterozoic rocks east and southeast of the Grenville front
Authors: Chiarenzelli J. R. , Drake A. A. , Goldsmith Richard , Hall L. M. , Hinze W. J. , Isachsen Y. W. , Lidiak E. G. , McLelland James , Mosher Sharon , Ratcliffe N. M. , Secor D. T. , Whitney P. R. 
Published: April 2015

Abstract
This chapter describes the Grenville orogen as it is preserved in areas of outcrop as well as in the subsurface in the United States, Late Proterozoic continental rifting that fragmented that orogen, and Precambrian rocks within terranes accreted to the rifted eastern and southern margins of Laurentia (earliest Paleozoic North America). The accretion of terranes to the eastern and southern margins of Laurentia formed the Paleozoic Appalachian (Caledonide)-Ouachita orogen. Outliers of the Grenville orogen, variously deformed by Paleozoic orogenies, crop out within the western part of the Appalachian orogen.
Although protoliths as old as Archean have been identified along the northwestern margin of the Grenville orogen in Canada, as far as we know, no rocks in the areas covered by this chapter are older than Middle Proterozoic. Some rocks, however, indicate ties to older source areas. Quartzites from the Adirondack Lowlands contain detrital zircons with minimum ages of 1.65 Ga, 1.8 Ga, and 1.95 Ga (McLelland and others, 1988a). Recent work by Dunning and Cousineau (1990) and Olszewski and others (1990) on rocks of the Chain Lakes block, Maine-Quebec, and correlatives to the north in the Canadian Appalachians has shown that some zircons, possibly detrital, in diamic-tite are as old as 2.8 Ga. Sinha and Bartholomew (1984) report a discordia intercept of 1.87 ± 0.2 Ga for zircons, probably detrital, from layered gneiss of the Blue Ridge Grenvillian outlier in Virginia. Zartman and Hermes (1987) report a Late Archean inheritance in zircon from Permian granites in the southeastern New England Avalonian terrane; they attribute this to the under-plating of the Avalonian microplate by Archean crustal components, possibly of Africa, in the late Paleozoic during the collision of Gondwanaland with Avalonia.
Middle and Late Proterozoic stratified rocks of the western U.S. Cordillera, Colorado Plateau, and Basin and Range province
Authors: Christie-Blick Nicholas , Devlin William J. , Elston Donald P. , Horodyski Robert J. , Levy Marjorie , Miller Julia M. G. , Pearson Robert C. , Prave Anthony , Stewart John H. , Winston Don , Wright Lauren A. , Wrucke Chester T. 
Published: April 2015

Abstract
The distribution of Middle and Late Proterozoic sedimentary and metasedimentary cover that lies unconformably on Early Proterozoic and Archean crystalline basement has been known for decades, but recent work, employing techniques of paleomagnetic correlation, sedimentology, sequence stratigraphy, and analysis of tectonic subsidence has led to modifications of some long-accepted correlations and tectonic models. Within the context of both older classical studies and this new work, the stratigraphy, correlation, tectonic setting, fossil content, and mineral potential of Middle and Late Proterozoic rocks of parts of the Rocky Mountain, Colorado Plateau, and Basin and Range provinces of the United States are discussed.
A problem common to interpretation of all Proterozoic strata is a widespread lack of fossil control on age and paleoecology, which makes correlations inherently uncertain and interpretation of depositional environments more difficult. We present current hypotheses about these topics and stress the uncertainty of some of our conclusions. The apparent polar wander path for the North American craton, as derived from the Middle and Late Proterozoic sedimentary cover, is central to our modifications of stratigraphie correlation, especially of Middle Proterozoic rocks.
The reader is asked to view the work and summaries presented here in the light of ongoing scientific debate about strata that are chronically stubborn in yielding information. The authors of sections of this chapter include both those who have performed classical studies, which are the foundation of our present understanding, and younger geologists who have been busy refining and modifying early interpretations, using different methods of study. The treatment in this chapter is therefore variable depending on which generation of investigators is speaking.
Geological Exploration of the Interior Plains
Authors: Stott D.F. , Aitken J.D. 
Published: April 2015

Abstract
Geological exploration has greatly influenced the development of western Canada, particularly the growth of the petroleum and natural gas, coal, and mineral industries. During the late nineteenth century when railroads were being built across the plains, settlers were encouraged by geological reports on the favorable agricultural prospects and the availability of water and fuels. The prosperity of the prairie provinces, based on their rich natural resources, would not have been achieved without the determination, enterprise, and knowledge of dedicated explorers.
This abbreviated account outlines the history of exploration and contributions of some of the notable individuals, particularly during the early years. The more recent history involves many more people, and it is not possible to acknowledge each and every one. Additional details on recent investigations may be found in the following chapters.
This subchapter has been prepared from a variety of sources in addition to original reports. It draws on a history of the Geological Survey of Canada by Zaslow (1975) and accounts of the development of the petroleum industry in western Canada by Gray (1970), de Mille (1970), Gould (1976), and a group of authors whose papers appear in Hilborn (1968).
Carboniferous
Authors: Richards B.C. , Bamber E.W. , Higgins A.C. , Utting J. 
Published: April 2015

Abstract
The Carboniferous System in Western Canada Basin (Fig. 4E.1-4E.3) is a thick succesion of strata deposited on the downwarped and downfaulted western margin of the ancestral North American plate, the central to western cratonic platform, and southern Yukon Fold Belt. This succession, representing the upper Kaskaskia sequenceand lower Absaroka sequence of Sloss (1963), comprises two main lithofacies assemblages. The lower assemblage is basinal shale and generally thickens southwestward or basinward (see Fig. 4 E . 9 - 4 E . 1 3) . Upward and northeastward, it passe into an upper assemblage of platform and ramp carbonates (Fig. 4E.4, 4E.5, 4E.9-4E.13) and sandstone-dominated siliciclastic facies, deposited in deep-water slope to continental settings. Both assemblages consist of numerous formations, some separated by regional disconformities. Subaerial erosion during the Late Carboniferous, Permian, and subsequent periods removed large parts of the succession, particularly in the Interior Plains, the region west of the Rocky Mountain Front Ranges, and the Cordillera between southwestern District of Mackenzie and northern Yukon Territory. Where the Carboniferous remains, it is generally unconformably overlain byeither Permian or Mesozoic strata.
Carboniferous formations are preserved in twomain regions. The southern one, which includes much of the eastern Cordillera andsouthern to western Interior Plains, extends from southwestern Manitoba to southwestern District of Mackenzie. The northern area includes the eastern Cordillera ofnorthern Yukon Territory and northwestern District of Mackenzie (Fig. 4E.1). Betweenthese regions, erosional remnants are present in the Mackenzie and Selwyn Mountains of east-central Yukon and west-central District of Mackenzie.
Permian
Authors: Henderson C.M. , Bamber E.W. , Richards B.C. , Higgins A.C. , McGugan A. 
Published: April 2015

Abstract
Permian rocks are preserved throughout most of the eastern Cordillera and locally, in the Peace River-Liard River area, on the Interior Platform (Fig. 4F.1, 4F.2, 4F.3). They are absent from the remainder of the Interior Platform and from most of the Mackenzie Mountains through truncation at several disconformities beneath Mesozoic strata.
Permian sediments were deposited mainly along the margin of the North American plate in a Permian depositional basin, here named Ishbel Trough, extending from the 49th parallel to the Ancestral Aklavik Arch in northern Yukon Territory. The trough occupies approximately the same position as the Carboniferous Prophet Trough (Richards et al., Subchapter 4E in this volume). In the Peace River-Liard River area, Permian sediments were also deposited on the western cratonic platform. The western margin of Ishbel Trough has not been identified. It (Fig. 4F.2, 4F.3) may have been in the area presently occupied by Cariboo Terrane (Struik and Orchard, 1985; Struik, 1986), which lacks Permian strata and may have been partly subaerially exposed during the Permian Period. A marginal basin to the west of Cariboo Terrane (Barkerville Subterrane of Kootenay Terrane; Monger and Price, 1979) contains a remnant of Permian strata (Sugar Limestone). The eastern margin of Ishbel Trough was a broad hinge-line along the western margin of the cratonic platform. In northeastern British Columbia and southwestern District of Mackenzie the hinge coincided with a zone of normal faulting, but generally the position of the eastern trough margin is unclear, because of eastward truncation of Permian strata (Fig. 4F.2, 4F.3).
Metallic Deposits
Authors: Aitken J.D. , Stott D.F. 
Published: April 2015

Abstract
The main metallic mineral deposits, with the important exception of Pine Point, lie within the eastern Cordillera and most are not being produced currently. Ferrous deposits of sedimentary origin and placer gold, both of low commercial interest at present, occur within the Plains. The metallic mineral deposits are outlined only briefly; additional detail may be found in the companion volumes on “Geology of the Cordilleran Orogen in Canada” (Gabrielse and Yorath, 1991) and “Mineral Deposits of Canada” (Geology of Canada, no. 8, Thorpe and Eckstrand, in prep.).
Hudson Platform – Geology
Authors: Norris A.W. 
Published: April 2015

Abstract
The Phanerozoic rocks of Moose River Basin are separated from those of Hudson Bay Basin by a northeast-trending Precambrian basement high, the Cape Henrietta Maria Arch (Fig. 8.1; see also Fig. 7.1). Because of the close similarity of facies and faunas, both basins were almost certainly connected with the Williston, Michigan, and Appalachian basins to the south during various intervals of Paleozoic time. The character of Ordovician and Silurian outliers on the Canadian Shield (Caley and Liberty, 1957), at Clearwater Lake (Kranck and Sinclair, 1963), Waswanipi (Clark and Blake, 1952), Lake Timiskaming (Hume, 1925), Mattawa, Lake Nippissing, and others, tends to support this hypothesis.
The northern boundary of Hudson Bay Basin is Bell Arch, trending northwestward through Southampton Island and bordering Foxe Basin of the southeastern Arctic Platform (see Fig. 7.1). The Phanerozoic rocks of Hudson Platform are separated from Williston and Elk Point basins to the southwest by Precambrian rocks of Severn Arch. To the south, Fraserdale Arch separates Moose River Basin from St. Lawrence Platform and Michigan Basin.
A basin concept for the offshore regions of Hudson Bay, inferred from sea-magnetometer profiles, was firmly established by Hood (1964). On the basis of refraction seismic data, Hobson (1964a, b) confirmed a basin of major proportions beneath Hudson Bay. Seismic profiles suggest that about 2000 m of Phanerozoioc strata are present in Hudson Bay Basin, and 600 to 800 m in the deeper parts of Moose River Basin.
Two structural provinces of the Canadian Shield, Superior and Churchill, border and
Hudson Platform – Economic Geology
Authors: Sanford B.V. , Norris A.W. , Cameron A.R 
Published: April 2015

Abstract
Hudson Platform underlies an area of 971 250 km2, more than half of which is covered by the waters of Hudson Bay, James Bay, Hudson Strait, and Foxe Basin. the region has potential for a variety of economic commodities, including petroleum and natural gas, oil shale, lignite, lead and zinc, and industrial minerals such as salt, gypsum, and limestone.
The principal emphasis over the years has been placed on exploration for oil and gas, first in the onshore areas of Moose River Basin, and in more recent years in the onshore and offshore regions of Hudson Bay Basin. Lignite deposits that have long been known to occur along the extreme southern margins of Moose River Basin have also been investigated from time to time for about a century, but have not been exploited commercially. Promising industrial mineral deposits including salt, gypsum, clay, sand, and limestone are known in widely separated parts of the platform, but have remained undeveloped owing to their great distance from densely populated regions of the country.
Introduction to Interior Platform, Western Basins, and Eastern Cordillera
Authors: Stott D.F. , Aitken J.D. 
Published: April 2015

Abstract
The Interior Platform, underlain by Phanerozoic sedimentary rocks, is the northwestern part of the North American Craton, the stable interior region of the continent (Fig. 2A.1; see also Fig. 1.1). Essentially flat-lying rocks of the Interior Platform extend into the eastern Cordillera where they are thrust-faulted and folded (see Fig. 5.5, in pocket), but have undergone little or no metamorphism nor plutonism during the orogenic phases. This area of undeformed and deformed sedimentary rock commonly is called the Western Canada Basin. The Interior Platform is linked to Michigan Basin and St. Lawrence Platform of southeastern Canada through the central U.S.A. and merges with Arctic Platform in the north. It is separated from Hudson Platform by a broad expanse of the Canadian Shield.
The area of nearly horizontal bedrock, forming the Interior Plains physiographic province, comprises plains and plateaux covered by a thick mantle of glacial drift. It is a region of grassland, forest, and tundra, some 2 000 000 km2 in area, that embraces parts of the prairie provinces of Manitoba, Saskatchewan, and Alberta, the northeast corner of British Columbia, and much of the western District of Mackenzie, Northwest Territories. In the southern region, clastic, carbonate, and evaporite strata of Paleozoic age rest on a basement of Precambrian crystalline rocks. The Paleozoic sediments are overlain by a relatively thick blanket of Mesozoic and Tertiary clastic rocks. The southern part of Interior Platform is the main oil-producing region of western Canada; it has been extensively drilled and its geology is well