bluuebunny/crossref_metadata_2025_split huggingface dataset:
The Proterozoic to Late Silurian Record of Pearya
Authors: Trettin H.P. 
Published: April 2015

Abstract
A geological province in northernmost Ellesmere Island, named Pearya by Schuchert (1923) and interpreted as the relict of a Precambrian borderland, is now regarded as an exotic continental fragment with an internal suture, i.e. as a composite terrane (Chapter 4). This chapter outlines its late Middle Proterozoic to Late Silurian record and briefly compares it with the records of the Franklinian and Caledonian mobile belts. Special emphasis is placed on Ordovician tectonic and plutonic events, which are important for the evaluation of Pearya’s relationships with these two regions.
Establishment of this history has been difficult because of sparse age control for the pre-Caradoc stratigraphic record, the effects of five orogenies, and partial ice cover. On first approach, Pearya is divisible into four major successions that differ in age and overall lithology (Fig. 9.2; for geographic names throughout this chapter see Fig. 9.1). Succession I includes sedimentary and(?) volcanic strata of uncertain age that have been deformed, metamorphosed in the amphibolite facies, and intruded by granitic plutons in late Middle Proterozoic time (1.0-1.1 Ga). Succession II, ranging in age from Late Proterozoic to Early Ordovician, consists mainly of “miogeoclinal” or “platformal” sediments (carbonates, quartzite, mudrock) with lesser proportions of mafic and siliceous volcanics, diamictite, and chert. Its concealed contact with succession I is tentatively interpreted as an angular unconformity. Succession III includes arc-type and(?) ocean floor volcanics, mudrock, chert, and carbonates, and has associated with it fault slices of ultramafic-mafic complexes of late Early Ordovician (Arenig) age. The faulted contact between
Middle-Upper Devonian Clastic Wedge of the Arctic Islands
Authors: Embry Ashton F. 
Published: April 2015

Abstract
Carbonate deposition dominated the Franklinian miogeocline from Late Cambrian until earliest Middle Devonian. Following a transgression in early Eifelian (within the costatus-costatus conodont Zone), quartzose clastics replaced carbonates as the dominant sediment type and, from that time until Early Carboniferous, clastic sedimentation was widespread across the Franklinian miogeocline. During this interval an enormous clastic wedge prograded southwestward, heralding the advance of Ellesmerian deformation.
Middle-Upper Devonian clastic sediments are widely preserved and are most widespread in the western Arctic, where they occur over much of Bathurst, Melville, Prince Patrick and Banks islands (Fig. 10.1). In the eastern Arctic the deposits occur mainly in a broad synclinorium which stretches from central Ellesmere Island to eastern Grinnell Peninsula. Isolated occurrences are present on northern Ellesmere Island in the Yelverton Pass region and in Tertiary grabens on Cornwallis Island (Fig. 10.1, Fig. 4 [in pocket]). Forty-two wells have penetrated the strata and numerous surface sections are described in the literature (Fig. 10.1, Fig. 1 [in pocket]). The maximum preserved thickness of the clastic wedge is about 4000 m, although thermal maturation levels of strata within and directly below the wedge suggest that original thicknesses may have been nearly twice this figure in some areas.
Regional mapping studies carried out by the Geological Survey of Canada in the 1950s and 1960s established a general stratigraphic framework for these clastic sediments (McLaren, 1963; Thorsteinsson and Tozer, 1962; Tozer and Thorsteinsson, 1964; Kerr, 1974). Embry and Klovan (1976) reviewed all previous work up to 1975 and presented
Devonian – Early Carboniferous Deformation and Metamorphism, North Greenland
Authors: Soper N.J. , Higgins A.K. 
Published: April 2015

Abstract
As outlined above (Chapters 7, 8), the sedimentary subprovince of the Franklinian deep water basin (Hazen Trough) extends eastward from the Canadian Arctic Islands (Chapter 8C) into northern Greenland (Chapter 7), and the pulses of deformation which affected the Canadian sector (Hazen Fold Belt) in Late Silurian or Devonian to Early Carboniferous time (Chapter 12) likewise extended into Greenland producing an east-west striking mobile zone, known traditionally as the North Greenland fold belt. The fold belt has an exposed width of up to 100 km on the north coast of Greenland and is flanked to the south by the weakly deformed lower Paleozoic platform sequence described in Chapter 7.
Figure 11.1 shows that several distinct tectonic zones can be recognized in the fold belt, and Figure 11.2 illustrates how these are spatially related to the geometry of the deep water basin (Hazen Trough). A southern fold and thrust zone coincides with a region which was transitional between the platform and trough for much of the Cambrian and Ordovician. It is bounded to the south by the Navarana Fjord lineament, which represents the position to which the platform margin had retreated by Early Silurian time. The structure of the southern zone is of thin skinned fold and thrust type, with an approximately east-west strike and southerly vergence.
A northern orthotectonic zone is developed on the site of the trough proper with its thick fill of dominantly Lower Cambrian turbidites. It forms the mountainous regions of Johannes V. Jensen Land, Nansen Land,
Silurian – Early Carboniferous Deformational Phases and Associated Metamorphism and Plutonism, Arctic Islands
Authors: Trettin H.F. 
Published: April 2015

Abstract
In the Arctic Islands, intermittent and localized deformational phases of Late Silurian to Frasnian age were followed by the Ellesmerian Orogeny sens stricto of latest Devonian (Famennian) to Early Carboniferous age (Thorsteinsson and Tozer, 1970, p. 566), which affected the entire mobile belt. Regional metamorphism of greenschist and higher grades, and granitic plutonism were restricted to parts of northern Ellesmere and Axel Heiberg islands.
The structural events and associated phases of metamorphism and granitic plutonism will be described in historical order, and, within given phases, from the oceanic side toward the craton. The most important conclusions are summarized at the end of the chapter. For an overview of the orogen, see Figures 12A. 1 and 121.1, and for geographic names, Figure 1 (in pocket).
The most important event in the structural history of northern Ellesmere Island was the accretion of Pearya, which resulted in intensive deformation in Pearya and the Clements Markham Fold Belt, and possibly also in adjacent parts of the Hazen and Northern Heiberg fold belts (Fig. 12B.1). Preliminary geological maps for this region have been published by Trettin and Mayr (1981), Mayr et al. (1982a, b), Trettin (1982, 1987b), Trettin et al. (1982), and Trettin and Frisch (1987); other relevant references arequoted in Chapters 8 and 9.
Available evidence strongly suggests that Pearya is an exotic terrane that was part of the Caledonides, at least until late Middle Ordovician time (Chapter 9).The Ashgill Wenlock deep water facies of Pearya are broadly comparable to those of the Franklinian
Late Cretaceous and Tertiary Basin Development and Sedimentation, Arctic Islands
Authors: Miall A.D. 
Published: April 2015

Abstract
Macrofossils are extremely rare in Arctic Cenozoic sediments, apart from rare nondiagnostic gastropods and pelecypods, plus foraminifera, fish, scaphopods and land vertebrates recorded from the Strathcona Fiord area, Ellesmere Island (Westetal., 1977, 1981). These have only a local distribution and are therefore of limited chronostratigraphic value. Macroflora, particularly pine cones, occur in Neogene sediments and some are age diagnostic. Marine fossils are rare throughout the Cenozoic section, except for rare dinoflagellates, particularly in the Banks Island area, and foraminifera on Meighen Island. However, spores and pollen are abundant throughout the Cenozoic and in the Campanian-Maastrichtian sediments of similar facies that lie conformably beneath the Cenozoic section.
Palynostratigraphic studies therefore form the main chronostratigraphic basis for the largely nonmarine or brackish water facies that comprise the bulk of the Cenozoic section of the Innuitian region (plus Campanian to Maastrichtian in the eastern Arctic).
Many local, spot age determinations have been carried out on the Upper Cretaceous and Cenozoic section. The only thorough stratigraphic investigations are those by Doerenkamp et al. (1976) in Banks Island and Rouse (1977) in Remus Creek, Ellesmere Island, for the Maastrichtian to Early Oligocene interval. These workers established zones based on comparison with contemporaneous sections in the Northern Interior Plains, Beaufort-Mackenzie Basin, British Columbia, Alaska, Siberia and elsewhere. In addition, G. Norris and M. Head (pers. comm., 1983-1985) have examined the writer’s collections from Axel Heiberg and central Ellesmere islands, and G. Norris (pers. comm., 1987) examined the Eocene to Miocene section in the Meighen Island well
Middle and Late Tertiary Tectonic and Physiographic Developments
Authors: Trettin H.P. 
Published: April 2015

Abstract
The post-Eurekan pre-Pleistocene history of the Arctic Islands is poorly known because the stratigraphic record of this interval is limited mainly to the northwestern margin of the Queen Elizabeth Islands (Chapter 15). The lack or scarcity of preserved sediments in other areas indicates uplifts, which, in interaction with erosion and eustatic sea level changes, gave rise to the present landscape (cf. Thorsteinsson and Tozer, 1970).
Middle or Late Tertiary positive movements were most pronounced within the Eurekan Orogen and a belt surrounding the Labrador Basin, and of lesser magnitude in the area south of the Eurekan Orogen. The uplift of the Eurekan Orogen represents isostatic adjustments to post-Eurekan erosion; the causes of the uplifts in the other areas are uncertain although a thermal model appears to be applicable to the mountains around Labrador Basin. The positive movements have been amplified to a minor extent by an overall drop in sea level since early Tertiary time (Vail and Hardenbol, 1979). The Holocene postglacial rebound will not be considered in this context because it merely tends to restore conditions that existed before the Pleistocene.
Crustal thickening during the Eurekan Orogeny resulted in high topographic relief that produced the syntectonic clastic sediments of the Eureka Sound Group (Chapter 15). Post-Eurekan erosion must have caused an isostatic disequilibrium that was compensated by upward movement. The presence of high mountain ranges and matching negative Bouguer anomalies shows that the crustal roots of the orogen have not yet been eliminated by these processes. It is generally
The Quaternary Record
Authors: Hodgson D.A. 
Published: April 2015

Abstract
Quaternary geology studies in most of the Arctic Archipelago inevitably have focused on the age and extent of Pleistocene glaciations. In the islands south of Parry Channel (Fig. 19.1), repeated advances of temperate glaciers spreading from continental dispersal centres have eroded and deposited a wide range of landforms. There, till is the most widespread surficial material; marine deposits, raised with a crust rebounding from the last glaciation, are also conspicuous. In the Queen Elizabeth Islands to the north, the mountainous eastern rim (Fig. 19.2) remains half glacierized and has attracted the interest of the glacial geologist as well as glaciologist; drift landforms are scarcer than to the south. In the western islands, drift is sparse and glacial studies are retarded in comparison with the rest of the archipelago. Suitably, this area has drawn some studies of Holocene and older nonglacial deposits and processes, including the thermal history of near-surface sediments.
The Quaternary of the archipelago is discussed at greater length in Fulton (1989), by Hodgson (1989) for the Queen Elizabeth Islands, by Funder (1989) for north Greenland, and, in three separate articles by Andrews (1989), Dyke and Dredge (1989), and Vincent (1989), respectively, for the islands south of Parry Channel.
The Quaternary climate of the Arctic Islands is poorly understood — in particular, the polar weather patterns that resulted when continental ice domes lay to the south. The present climate of most of the northern islands is dominated year-round by the anticyclonic air of the central Arctic Ocean, and thus
Geographic and Geological Exploration
Authors: Christie R.L. , Dawes P.R. 
Published: April 2015

Abstract
The region discussed in this chapter encompasses the Canadian Arctic and northern Greenland. A dividing seaway — Davis Strait, Baffin Bay, Nares Strait — forms a prominent route by which generations of explorers, from the Norsemen to the classical late 19th century voyages of geographic discovery, pushed north to explore the mysteries of “Ultima Thule”. Ardent pursuit of two geographic objectives, the Northwest Passage and the North Pole, resulted in the discovery and outline mapping of much of the region. Ship and sledge expeditions directed at specific scientific programs followed in the 20th century; these activities were superseded by aircraftsupported operations in the years following World War II.
Geographic and geological research continues, now supported by Canadian and Danish government agencies and private operators. Paradoxically, it was as recently as 1978 that the region’s (and the Earth’s) most northerly land was discovered: a Danish helicopter party that year landed on Oodaaq Ø, a small island at about 83°40N off the north Greenland coast.
This account of exploration in the Innuitian Region is divided into five roughly chronological sections: I. Paleoeskimo habitation and Norsemen, 2000 B.C. – A.D. 1500; II. Early mariners and the Franklin Search, 1576-1859; III. Exploration along the Polar Route, 1852-1909;IV. Geological exploration by ship and dog sledge, 1903-1947; V. The aircraft age of geological study, 19 47 to the present. Brief notes on the development of geological understandingof the region follow sections II to IV1.
Archeological finds indicatethat the Innuitian Region was inhabitated by paleo-eskimos as far
Summary and Remaining Problems
Authors: Trettin H.P. 
Published: April 2015

Abstract
This concluding chapter provides a brief, interpretative overview of the geological history of Innuitian Orogen and Arctic Platform with emphasis on unsolved major problems, and a summary of their resources. References quoted in previous chapters will not be repeated; for geographic names, see Figure 1 (in pocket).
The northern part of the Canadian Shield (including Greenland) consists of a number of relatively small continental plates of Archean age that were welded together into a single supercontinent in a series of Early Proterozoic orogenies. The outlines of the Archean cratons and intervening Early Proterozoic orogenic belts have not yet been established for the High Arctic, but an orogen 1.91.95 Ga old is recognized in southeastern Ellesmere Island and adjacent parts of Greenland (Chapter 6).
An extensive late Middle Proterozoic rifting event is indicated by mafic volcanic and intrusive rocks and associated coarse clastic sediments exposed on Melville Peninsula (Fury and Hecla Basin), northern Baffin Island and Bylot Island (Borden Basin), southeastern Ellesmere Island and adjacent parts of West Greenland (Thule Basin), and northeastern Greenland (Chapter 6). Radiometric ages suggest correlation with the extensive Mackenzie dyke swarm of the eastern Cordillera, dated at about 1.2 Ga. The rift deposits are succeeded by shallow marine clastic and carbonate sediments that also are represented on Victoria Island (Shaler Group). Age and correlation of the sedimentary units are problematic. Lithological relationships suggest that the sedimentary units in the Borden and Thule basins are correlative, but the former have yielded late Middle Proterozoic paleomagnetic ages, whereas
Geophysical Characteristics
Authors: Sobczak L. W. 
Published: April 2015

Abstract
The first measurements of gravity in Arctic Canada were made on Melville Island in 1819-1820 (Sabine, 1821). Gravity measurements in the Arctic did not resume until 1957 when five gravity control stations were established by the Canadian Government (Bancroft, 1958), and in 1958 about 200 gravity observations were made over Gilman Glacier in northeastern Ellesmere Island (Weber, 1961). The same year, as a contribution to the International Geophysical Year (IGY), a subtense bar and gravity traverse was carried out from Clements Markham Inlet on the Arctic coast across the United States Range to Archer Fiord on Kennedy Channel (Weber, 1961). In 1958 the Polar Continental Shelf Project (PCSP) was established, in the then Department of Mines and Technical Surveys, to coordinate most of the scientific studies carried out in the Arctic by the Canadian Government.
From 1960, under the aegis of the PCSP, systematic gravity surveys have been carried out in the Arctic by the Dominion Observatory (later renamed the Earth Physics Branch [EPB], of the Department of Energy, Mines and Resources, and now part of the Geological Survey of Canada) primarily over the relatively flat areas of the Innuitian Region and adjacent continental margin (Sobczak, 1963; Sobczak et al., 1963; Picklyk, 1969; Sobczak and Weber, 1970; Sobczak and Stephens, 1974; Sobczak and Sweeney, 1978). Except for small areas completed in the southern, central, and northern parts of Ellesmere Island, gravity surveys of the mountainous areas of Axel Heiberg and Ellesmere islands have been deferred until reliable elevations can be
Gravity from 64°N to the North Pole
Authors: Sobczak L. W. , Hearty D. B. , Forsberg R. , Kristoffersen Y. , Eldholm O. , May S. D. 
Published: April 2015

Abstract
Although gravity observations were made prior to 1960, systematic regional gravity coverage in the Arctic began in earnest in the early 1960s on land and sea ice with the advent of helicopters and reliable portable gravimeters, and was extended in the 1970s over the oceans with ships and reliable marine gravimeters. As a result, about half of the polar area north of 64°N latitude is now covered with regional (spacings 12 km or less) gravity observations for which the data are readily available to the public. Permanently ice-covered regions of the Arctic Ocean, as well as mountainous and glacier-covered areas, are still largely unmapped. Except for a few pre-World War II gravity stations from regions within the Soviet Union (USSR), no gravity data from the USSR are displayed on Plate 3.
The observed gravity field of the whole Arctic region north of 60°N was first discussed by Sobczak (1978), who presented maps (scale 1:7,500,000) showing the gravity field derived from mean values based on observed (1/2° latitude × 2° longitude) and predicted (1° latitude × 1° longitude) free-air anomalies and a residual gravity field derived by removing the satellite gravity field (Goddard Earth Model 8, GEM 8) from the observed and predicted fields. These maps indicate anomalous gravitational features of wavelengths in excess of 100 km.
Bowin and others (1982) presented a comprehensive free-air gravity anomaly atlas of the world, including a map of the Arctic region north of 70° at a scale of about 1:14,000,000.
The intent of the present
Magnetic anomalies
Authors: Coles R. L. , Taylor P. T. 
Published: April 2015

Abstract
Extensive magnetic surveys have been made over the Arctic Ocean since 1946. The survey techniques have varied, as have the methods and forms of data presentation. This chapter reviews the magnetic anomaly information from the Arctic Ocean region and discusses the significant contributions made by magnetic surveys to the understanding of this region of the earth’s crust. The magnetic anomaly field is the only geophysical parameter in the Arctic that has been reasonably uniformly measured. It is critical to the study of Arctic structure and evolution.
Geothermal observations in the Arctic region
Authors: Langseth M. G. , Lachenbruch A. H. , Marshall B. V. 
Published: April 2015

Abstract
A fundamental goal of geothermal studies in the Arctic region is to determine the rate of heat flow from deep in the earth’s crust. Research during the past 25 years has shown heat flux is closely related to the tectonic evolution of a geological province. When combined with other geological and geophysical data, accurate heat-flow measurements can set constraints on crustal temperatures, age and evolution of the lithosphere, and the distribution of radiogenic heat in the crust. At an even more fundamental level, accurate measurements help determine the total rate of heat loss from the Earth and define the global variation of heat flow and its correlation with other long-wavelength geophysical features.
In addition to the fundamental scientific interest, the subsurface thermal regimes of continents and continental margins of the Arctic are of practical concern for natural resource development. Mean annual surface temperatures on land are well below freezing, which results in a permafrost layer hundreds of meters thick in some places; for example Judge and others (1981) reported a permafrost thickness of 726 m on Cameron Island in the Canadian Arctic Archipelago. The ice-bearing permafrost presents many obstacles to the development of resources and the maintenance of facilities in the Arctic, and as a consequence, a considerable effort has been made by the Canadian and United States governments and industry to evaluate the subsurface thermal regime from an engineering perspective. These efforts have provided many drill holes for subsurface temperature and thermal properties data. Many of these holes will provide
Seismic reflection and refraction
Authors: Jackson H. R. , Forsyth D. A. , Hall J. K. , Overton A. 
Published: April 2015

Abstract
The ice cover of the Arctic Ocean restricts research vessels, limiting the number of miles of seismic reflection and refraction lines in the area. Figures 1 and 2 show the distribution of the lines, andTables 1 and 2 provide references keyed to those figures. This paper describes the distribution, collection, and processing of the seismic reflection and refraction data available in the deep basins and major ridges in the Arctic Ocean and briefly discusses the salient geological results by region. In addition, the position of seismic surveys on the continental margins and adjacent landmasses of the North American plate have been compiled for completeness. These peripheral areas are documented with recent review papers Table 1) including Eldholm and others (this volume) and Larsen (this volume).
Most of the seismic reflection information in the Arctic Ocean has been collected on drifting ice stations; thus, the direction of the lines is controlled by the whims of nature. The data set presented here is incomplete due to the inaccessibility of information collected by Soviet scientists. No seismic profiling has been run from the northern margin of Greenland, and only three refraction surveys and one reflection line exist on the Canadian Polar margin from Greenland to the Beaufort Sea. Most of the reflection lines in the Canada Basin were acquired with power sources of insufficient strength to penetrate the sedimentary section. Even with this meager collection of erratically spaced and variable quality information, important trends can be seen, interesting features