bluuebunny/crossref_metadata_2025_split huggingface dataset:
The East Greenland Shelf
Authors: Larsen Hans Christian 
Published: April 2015

Abstract
Geologically, the East Greenland Shelf remained virtually unexplored for many years while the onshore East Greenland Mesozoic basin stratigraphy was intensely studied and served as a reference for the interpretation of the offshore East Greenland and northwest European margins. This development was a natural consequence of the excellent onshore basin exposure while polar pack ice is found almost year-around on the East Greenland shelf. The first geophysical information from the East Greenland shelf was published by Vogt (1970), Eldholm and Windisch (1974), Johnson and others (1975a, b), B. Larsen (1975), H. C. Larsen (1975, 1978), Henderson (1976), and Featherstone and others (1977).
Results of the first multichannel reflection seismic surveying on the shelf were reported by Hinz and Schlüter (1978, 1980). On the basis of this information and initial results from an aeromagnetic survey (H. C. Larsen and Thorning, 1979, 1980), a regional geological model for the East Greenland Shelf was proposed by H. C. Larsen (1980). This model involved early Tertiary oceanic crust thought to be present below parts of the outer shelf off central East Greenland and subsided continental crust thought to be present up to approximately 100 km seaward of the shelf break off southeastern Greenland. The actual position of the shelf edge was found to be controlled mainly by post-rift sedimentation rather than deep crustal features (H. C. Larsen, 1980). It was further suggested that Cenozoic basins might dominate the southern half of the shelf while Mesozoic and Paleozoic basins were likely to be present beneath the northern shelf.
The continental margin northwest of the Queen Elizabeth Islands
Authors: Sweeney J. F. , Sobczak L. W. , Forsyth D. A. 
Published: April 2015

Abstract
The polar continental margin described here lies between M’Clure Strait and the Lincoln Sea (Fig. 1). It clearly separates continental sequences of the Queen Elizabeth Islands from presumed oceanic crust beneath the deep Canada Basin and, near Axel Heiberg and Ellesmere Islands, from rocks of the submarine Alpha and Lomonosov Ridges.
Systematic studies in the region began in the late 1940s with Soviet air-lifted spot soundings over the outer continental slope and rise. In the 1950s and 1960s, the Alpha Ridge and adjacent parts of the outer continental shelf and slope were identified by multiparameter measurements from a series of drifting U.S. ice stations. In Canada, onshore geological studies began in 1955, and reconnaissance investigations of the polar shelf and slope were underway by 1960. The reader is referred to Weber (1983) and Weber and Roots (this volume) for further details of early studies.
Comprehensive reviews that include onshore geology adjacent to the polar margin begin with Fortier and others (1963) with later syntheses by Thorsteinsson and Tozer (1970), Trettin and others (1972), Trettin and Balkwill (1979), Hea and others (1980), Miall (1981), and Kerr (1981). Offshore, chiefly geophysical data over the polar shelf and slope are summarized by Trettin and others (1972), Sweeney and others (1978), Vogt and others (1982), Sweeney (1982), and Forsyth and others (1988).
From the information available up to the early 1980s, it was considered that the polar margin formed when the Canada Basin opened in Jurassic or Early Cretaceous time, that the crust
Canadian Beaufort Sea and adjacent land areas
Authors: Dixon J. , Dietrich J. R. 
Published: April 2015

Abstract
The Canadian Beaufort Sea extends from offshore Banks Island to 141 °W longitude (Fig. 1). It is rimmed to the south by the Yukon Coastal Plain, the outer Mackenzie Delta, including Richards Island, and Tuktoyaktuk Peninsula. The narrow coastal plain of northern Yukon is bounded to the south by the British Mountains and the Porcupine Plateau (Fig. 1). The broad Amundsen Gulf separates the Anderson and Horton plains of the Northwest Territories mainland from Banks Island and Victoria Island.
The continental margin beneath the Beaufort Sea can be divided into several physiographic regions. The shallow-water shelf is 50–100 km wide and is characterized by low, uniform slope gradients of 1–2 m/km. An abrupt increase in the sea-floor slope gradient marks the shelf edge. Water depths at the shelf break vary from 60 m near 141°W to almost 500 m west of Banks Island. Two channel-like features cut across the Beaufort shelf. Northeast of Herschel Island, the Mackenzie Trough (formerly Mackenzie Canyon) cuts obliquely across the shelf in a northwesterly direction (Fig. 1). Southwest of Banks Island, the broad Amundsen Gulf channel cuts across the shelf in a northwesterly direction. Both of these bathymetric troughs are 100–500 m deep and are geologically recent in origin. The continental slope seaward of the shelf edge is 20–50 km wide and is characterized by variable slope gradients of 5–30 m/km. The outer continental slope north of the Mackenzie Trough is marked by a steep, sea-floor escarpment with local slope gradients of up to 170 m/km (Fig. 1)
Geology of the Arctic Continental Margin of Alaska
Authors: Grantz Arthur , May S. D. , Hart P. E. 
Published: April 2015

Abstract
Alaska faces the Canada Basin of the Arctic Ocean along an arcuate continental margin, gently concave to the north, that stretches unbroken from the Mackenzie Delta, near 137°W to Northwind Ridge of the Chukchi Borderland near 162°W. (These and other regional geographic features mentioned below can be found in Plates 1 and 11.) This margin, with an arc-length of about 1,050 km, marks one side of a continental rift along which the Canada Basin opened by rotation about a pole in the Mackenzie Delta region during middle Cretaceous time. The rift- margin structures, which lie beneath the inner shelf and coastal plain in the eastern Alaskan Beaufort Shelf and beneath the outer shelf in the western Beaufort and Chukchi Shelf, are now buried by a thick middle Lower Cretaceous to Holocene progradational continental terrace sedimentary prism.
We divide the Arctic continental margin of Alaska into three sectors of strongly contrasting geologic structure and physiographic expression. In the Barter Island sector (see Figs. 3 and 4) the structure is dominated by the effects of Eocene to Holocene convergence and uplift, and the continental slope is upwardly convex; in the Barrow sector the structure is dominated by the effects of middle Early Cretaceous rifting and continental breakup, and the continental slope is upwardly concave; and in the Chukchi sector the structure is controlled by an easterly trending middle Early Cretaceous rift, and the continental slope abuts the Chukchi Borderland.
Physiographically, the Alaska continental margin is expressed by the Alaska continental
The Arctic continental margin of eastern Siberia
Authors: Fujita Kazuya , Cook David B. 
Published: April 2015

Abstract
The Arctic Ocean margin of the North American plate in Asia forms a continental shelf up to 800 km wide, which underlies the East Siberia Sea (Fig. 1). The New Siberian Islands separate the East Siberian Sea from the Laptev Sea on the west, and Wrangel Island (Ostrov Vrangelya) separates the East Siberian Sea from the Chukchi Sea on the east. The area of the East Siberian Sea is about 1,500,000 km2, and it is connected to the Chukchi Sea by Long Strait (Proliv Longa) and to the Laptev Sea by several straits through the New Siberian Islands.
The shelf of the East Siberian Sea is shallow, less than 50 m deep, and flat. The shelf is cut by two valleys, a few tens of meters deeper than the surrounding shelf, which are extensions of the Indigirka and Kolyma rivers (Naugler and others, 1974). The continental slope of the East Siberian Sea is gentle (slope ~1°), and alluvial cones spread out into the adjacent abyssal plain from submarine canyons (Lastochkin, 1980). The shelf appears to be connected to the Arlis Plateau, but is separated from the Lomonosov Ridge by a sediment-filled trough (Dementiskaya and Hunkins, 1971) (Fig. 2).
Since the geology of the East Siberian Shelf is poorly known, most tectonic and geologic models are extrapolations of the geology of the New Siberian Islands. Wrangel Island, and northern Eurasia. Rather than present the details of these speculations, in this chapter we summarize the known geology of
Ridges and basins in the central Arctic Ocean
Authors: Weber J. R. , Sweeney J. F. 
Published: April 2015

Abstract
This chapter describes the physiography plus the geological and geophysical character of the central Arctic. The available information is chiefly from work done on several ice station transits of the area together with aeromagnetic and satellite magnetic investigations. The data provide crude constraints on the nature and ages of the main sea-floor features of the central Arctic Ocean.
The central area of the Arctic Ocean contains abyssal depths that are traversed by two subparallel submarine mountain ranges, the Lomonosov Ridge and the Alpha-Mendeleev Ridge complex. The wedge-shaped Makarov Basin separates these adjacent ranges, which are close to North America and are more than 500 km apart at their junction with the East Siberian continental margin (Fig. 1). Significant difference in overall morphology and geophysical properties between the Lomonosov and Alpha Ridges, despite their juxtaposition near North America, suggests a complex structural evolution for the central Arctic, whose origins are constrained loosely within the late Early Cretaceous-earliest Tertiary interval.
The Norwegian-Greenland Sea
Authors: Eldholm Olav , Skogseid Jakob , Sundvor Eirik , Myhre Annik M. 
Published: April 2015

Abstract
Generation of oceanic crust at the boundary between the Greenland/North American and the northwestern part of the Eurasian plates has created the Norwegian-Greenland Sea. This relatively young ocean comprises a number of separate basins, plateaus, and ridges revealing that the break-up and separation of the two major plates have not, in geological terms, been a simple process.
In this context we define the Norwegian-Greenland Sea as the deep ocean between Europe and Greenland, bounded in the south by the Greenland-Iceland-Faeroe shallow transverse and in the north by the Spitsbergen Fracture Zone (Fig. 1). Geographically, the term Greenland Sea has been used for the ocean between Svalbard and northeast Greenland, but here we have adopted the geologically accepted usage in which it relates to the deep ocean between the Greenland-Senja and Spitsbergen fracture zones.
Passive continental margins consisting of well-developed shelves and slopes separate the Norwegian-Greenland Sea from the adjacent continental masses of Greenland, Svalbard and Fennoscandia. The two adjacent shallow seas, the North Sea and the Barents Sea were, prior to the formation of the deep ocean in early Cenozoic time, part of a much larger contiguous epicontinental sea between the continental masses.
The scientific exploration of the deep ocean, which started late in the last century, was until the 1950s focused on physical oceanography and marine biology. It was not before the mid-1960s that systematic research programs in marine geology and geophysics were initiated. These investigations were pioneered by regional surveys carried out by Lamont-Doherty Geological Observatory
Canada Basin
Authors: Grantz Arthur , May S. D. , Taylor P. T. , Lawver L. A. 
Published: April 2015

Abstract
The Canada Basin, 1,600 km long and 650 to 1,050 km wide, is an extensive area of moderately deep water lying in the Amerasia sector of the Arctic Ocean (Fig. 1 and Plate 1). Unlike many other ocean basins, it is poorly understood. The tectonic processes that formed it are thought to have played an important role in the structural development and configuration of Alaska and the northeastern USSR, and in the development of the large hydrocarbon resources that have been discovered around the margins of the basin.
The borders of the Canada Basin are North America on the east and south and a complex of submarine ridges and plateaus on the north and west that may have diverse origins. The submarine ridge features include the Northwind Ridge and Chukchi Cap of the Chukchi Borderland on the southwest, and the Mendeleev and Alpha Ridges on the northwest and north respectively. Much of the basin has an extensive continental rise that slopes westward from the Canadian Arctic Islands toward the deep Canada Abyssal Plain. This abyssal plain, which underlies the western Canada Basin, is its deepest part. The Mendeleev Abyssal Plain (Fig. 1) lies to the west of the northern part of the Canada Abyssal Plain and is separated from it by a scarp 300 m to more than 500 m high. This scarp and the Northwind Escarpment (the east face of Northwind Ridge) together form the west boundary of the Canada Abyssal Plain; and their continuity may have
Late Mesozoic and Cenozoic paleogeographic and paleoclimatic history of the Arctic Ocean Basin, based on shallow-water marine faunas and terrestrial vertebrates
Authors: Marincovich Louie , Brouwers Elisabeth M. , Hopkins David M. , McKenna Malcolm C. 
Published: April 2015

Abstract
The paleogeography and marine paleoclimate of the Arctic Ocean Basin have evolved considerably during the past 100 million years, since the beginning of the Late Cretaceous. The shallow-water marine faunas that are needed to understand much of this history have recently been found, so that paleontologic studies of the Arctic Ocean Basin and its margins are presently in their early stages. The paleogeographic history of the Arctic Ocean may be divided conveniently into four intervals, each characterized by different marine connections to the world ocean. The first interval extended through most of the Mesozoic, when the Arctic Ocean was a northern gulf of the Pacific Ocean and subsequently developed seaway connections to other oceans. The second interval was during the Late Cretaceous and early Paleogene, when the Arctic Ocean was more or less completely isolated geographically from the world ocean. The third interval lasted from the late Paleogene to the middle Pliocene, during which the Arctic Ocean was connected to the Atlantic but not to the Pacific; and the fourth interval, lasting to the present day, was ushered in at about 3.0–3.5 Ma by the opening of the Bering Strait. The marine paleoclimate of the Arctic Ocean during the Late Cretaceous and early Tertiary was remarkably warm and equable until the onset of gradual cooling that culminated in late Neogene and Pleistocene ice cover.
Late Cenozoic geologic evolution of the Alaskan North Slope and adjacent continental shelves
Authors: Dinter David A. , Carter L. David , Brigham-Grette Julie 
Published: April 2015

Abstract
The Alaskan Arctic Coastal Plain and its submerged extensions to the north and west, the Beaufort and Chukchi continental shelves, are underlain by a broad, low-relief bedrock surface, the North Beringian Marine Abrasion Platform, which dips gently seaward from the Arctic foothills of the Brooks Range northward to the continental shelf break of the Arctic Basin (Fig. 1). During late Cenozoic time the sea repeatedly transgressed and receded across the North Beringian Platform in response to glacioeustatic sea level fluctuations. A thin veneer of unconsolidated, interfingering marine and nonmarine deposits mantles the bedrock surface and records the succession of geologic environments that have prevailed there during the last 3 m.y. All of these unconsolidated deposits are presently assigned to the Gubik Formation, which has a maximum measured thickness of about 60 m onshore, and thickens to perhaps a few hundred meters in places beneath the Beaufort shelf. In this chapter, we summarize and discuss the depositional history of the Gubik Formation and its bearing on the late Cenozoic geologic and climatic history of the Arctic region. The discussion begins with the onshore exposures, which have been studied in detail over many years, and for which a coherent stratigraphic framework has begun to emerge, and then moves to the offshore deposits, which, though thicker and better preserved, have only recently become the target of stratigraphic investigations.
The marine deposits of the Gubik Formation on the Arctic Coastal Plain have intrigued researchers since the early years of this century, when Leffingwell
The late Neogene and Quaternary stratigraphy of the Canadian Beaufort continental shelf
Authors: Blasco S. M. , Fortin G. , Hill P. R. , O’Connor M. J. , Brigham-Grette J. 
Published: April 2015

Abstract
This compilation of the late Neogene and Quaternary geology of the Canadian Beaufort continental shelf is the result of a nine-year cooperative effort between the Geological Survey of Canada and the Canadian Beaufort Sea oil industry. At depths beyond 100 m below seabed the deeper, more generalized stratigraphy is based on the interpretation of the first two seconds of conventional deep multichannel seismic reflection data (on an approximately 5-km grid) correlated with the shallow sections of several exploration wells (Fortin, 1990). The detailed surficial geology of the upper 100 m of sediment below seabed is based on the interpretation of some 15,000 line km of high-resolution, analogue, and shallow digital multichannel seismic reflection data, including boomer, small airgun, airgun array, and Flexichoc sources (Hunter and Blasco, 1980; Quinn and others, 1987). These shallow profiles were correlated with sedimentological, chronological, biostratigraphic and geotechnical analyses of more than 300 sediment cores recovered from the sea floor across the shelf using conventional gravity, piston, and wireline sampling techniques (Le Tirant, 1979). Sampling procedures included both continuous and interval coring, and sampled depths varied from less than 1 m to more than 100 m below seabed. Limited shallow-borehole well-log information, including velocity, density, and resistivity measurements, were also incorporated (Stirbys, 1990).
Sedimentary basins and petroleum resource potential of the Arctic Ocean region
Authors: Haimila N. E. , Kirschner C. E. , Nassichuk W. W. , Ulmichek G. , Procter R. M. 
Published: April 2015

Abstract
This chapter examines the petroleum potential of the sedimentary basins along the continental margins of the North American Plate in the Arctic Ocean region, including those beneath the continent itself and those beneath its fringing continental terraces. Basins within the Canadian Arctic Islands of North America and in the Baffin Bay regions are considered in other volumes of this series. The large petroleum potential of some of the sedimentary basins of the Arctic Ocean margin of the North American Plate, particularly those on the continental shelf, is already well established. The petroleum resource potential of the abyssal plains of the Arctic Ocean is poorly understood but is thought to represent only a minor portion of the total potential of the region.
The basins in the periphery of the Arctic Ocean Basin are mainly continental terrace wedges on foundered passive continental margins and successor basins on extended continental shelves. The Kronprins Christian Basin on the East Greenland Shelf is separated from European basins by the Mid-Atlantic Ridge north of Iceland (Fig. 1). The rest of the basins along the edge of the North American continent area, from east to west, are the Wandel Sea Basin in Greenland, the Lincoln Sea Basin, the various sub-basins of the Canadian Arctic Coastal Plain and Shelf, the Mackenzie Delta–Beaufort Sea Basin in Canada, and the Kaktovik Basin, the Demarcation Subbasin, the Dinkum Graben, and the Nuwuk Basin off Alaska. West of Alaska and north of Siberia the broad continental shelf contains upper Paleozoic-Mesozoic successor
Arctic Ocean ice cover; Geologic history and climatic significance
Authors: Clark David L. 
Published: April 2015

Abstract
The Arctic Ocean is unique among the world’s oceans because of its perennial ice cover. The geologic and climatologic factors that contributed to development of the Arctic Ocean ice cover are understood in a general way, even though the precise mechanism and time during the Cenozoic that the first ice cover formed are not known. Data concerning climatological processes that encouraged development of an Arctic Ocean ice cover have developed from the general understanding of the paleogeographic sequence of events since the last major time of ice-free conditions during the Cretaceous and early Cenozoic. The lack of facts concerning the precise time, and to some extent the mechanism, of ice cover origin is largely the result of an inadequate data base in the Arctic Ocean. For example, no long sediment core with middle Cenozoic sediment that may represent the time of the initial ice-cover development has been collected. Unfortunately, no research ship with capability for recovery of long sediment cores has been designed for work in the area of year-round Arctic pack ice. Therefore, the only sediment record for the central Arctic Ocean is that recovered from drifting ice stations such as the U.S. T-3 program and the Canadian LOREX and CESAR projects. Offshore drilling on the continental slope of Alaska and Canada has penetrated a more complete Cenozoic section. The sediment is largely non marine and, in the shallow Beaufort Sea area, consists of thick deltaic sediment. Detailed paleoclimato- logic study of this sediment has not been accomplished, but
Gas hydrates of the Arctic Ocean region
Authors: Kvenvolden Keith A. , Grantz Arthur 
Published: April 2015

Abstract
Sediments of the Arctic Ocean region may trap enormous quantities of natural gas in and beneath gas hydrates. These solid, ice-like substances, composed mainly of methane and water, are found in two distinct environments: (1) offshore, in sediment of the outer continental margin, and (2) onshore, in and below areas of thick permafrost. Most offshore gas-hydrate occurrences have been inferred from marine seismic-reflection records where an anomalous acoustic reflector correlates with the base of the gashydrate zone. Onshore, most gas-hydrate occurrences have been inferred from well-log responses. In only a few cases have gas hydrates actually been sampled. This chapter focuses on the known and inferred gas hydrates of the North American Arctic and estimates the amount of methane that may be associated with sediments in the Arctic Basin.
Paleomagnetic and plate-tectonic constraints on the evolution of the Alaskan-eastern Siberian Arctic
Authors: Harbert William , Frei Leah , Jarrard Richard , Halgedahl Susan , Engebretson David 
Published: April 2015

Abstract
The tectonic development of the Arctic Basin is constrained by several independent sets of data. These include paleomagnetic Apparent Polar Wander Paths for the North American and Eurasian Plates, paleomagnetic data from Arctic Alaska, and magnetic isochrons in the Arctic, Atlantic, and Pacific Oceans. In this chapter we use each set of data to constrain plate-tectonic models describing the development of the Amerasia Basin, northern Alaska, and the northeast USSR. First, we use Apparent Polar Wander Paths for the Eurasian and North American Plates to show the existence of a gap between these two plates in the Arctic Basin region before the formation of oceanic crust in the North Atlantic and Arctic oceans (the Late Carboniferous to Early Cretaceous, about 310 to 120 Ma). We then review and present new paleomagnetic data from the North Slope of Alaska to constrain the timing and geometry of the opening of the Canada Basin. The new data shows that counterclockwise rotation of -70° has occurred since Barremian time, providing strong evidence supporting a rotational opening of the Canada Basin. Next, we review plate-tectonic models describing rifting in the Arctic and North Atlantic Basins and correlate tectonic events in the Arctic Basin with these motions. We correlate periods of strong convergence between the continental plates from ~70 to ~56 Ma (Maastrichtian to Paleocene) with compressional deformation between the Chukotsk Peninsula and northern Alaska and movement along the Denali Fault. transform motion between these plates from ~56 through 50 to 38 Ma (lower to upper Eocene)