scholarly journals Eskimo languages in Asia, 1791 on, and the Wrangel Island-Point Hope connection

2006 ◽  
Vol 29 (1-2) ◽  
pp. 163-185 ◽  
Author(s):  
Michael E. Krauss
Keyword(s):  
Geographical Distribution ◽  
East Coast ◽  
The Arctic ◽  
North Coast ◽  
Language Varieties ◽  
Wrangel Island ◽  
The North ◽  
Point Hope ◽  
Arctic Coast ◽  
Cultural Interest

Abstract Merck’s statement about four “Sedentary Chukchi” (Eskimo) languages or language varieties along the coast of Chukotka in 1791 is thoroughly remarkable and worthy of careful interpretation. By his statement of their geographical distribution, the first three languages are very easy to identify, as 1) Sirenikski, 2) Central Siberian Yupik, explicitly including St. Lawrence Island, and 3) Naukanski. Merck’s language number four, “Uwelenski” he claims, startlingly, to be spoken along the Arctic Coast of Chukotka from Uelen as far as Shelagski Cape, 600 miles to the northwest. Serendipitously enough, Merck has 70 or so ”Uwelenski” words of cultural interest transcribed throughout his text. Careful studies of these words by this writer and also by Mikhail Chlenov show that “Uwelenski” is in fact a dialect of Central Siberian Yupik, thus part of a language continuum spoken from St. Lawrence Island to the Chaplino corner and the East coast of Chukotka, thence to the North coast of that mainland, treating Naukan as a “third Diomede” rather than as a mainland interruption. However there is no evidence that language number four, “Uwelenski,” actually a dialect of Merck’s language number two, was spoken beyond Kolyuchin Bay. Beyond that point, however, there was indeed a fourth Eskimo language. The second half of the paper concludes, from at least seven independent sources, that that fourth language was in fact none other than North Alaskan Inupiaq, spoken intermittently in pockets between Kolyuchin and Shelagski Cape, at least since the opening of Russian posts at Kolyma and into the nineteenth century, by north Alaskans from the Point Hope area, who also used Wrangel Island as a stopping place.

‘The last duty of an officer’: Lieutenant de vaisseau Joseph-René Bellot, 1826–1853, in the Franklin Search

Polar Record ◽  
2013 ◽  
Vol 50 (1) ◽  
pp. 1-30 ◽  
Author(s):  
William Barr ◽  
Nadine Forestier-Blazart ◽  
Jean-Claude Forestier-Blazart
Keyword(s):  
East Coast ◽  
The Arctic ◽  
North Coast ◽  
Northwest Passage ◽  
The North ◽  
Integral Component ◽  
Somerset Island

ABSTRACTLieutenant de vaisseau Joseph René Bellot, (1826–1853) participated, as second-in command, in Lady Franklin's private expedition in search of her missing husband on board Prince Albert, under the command of Captain William Kennedy in 1851–1852. Having wintered at Batty Bay on the east coast of Somerset Island, Kennedy and Bellot sledged south in the spring of 1852, to Bellot Strait, which they discovered. Having passed through the strait, they crossed Peel Sound, and continued west across Prince of Wales Island to Ommanney Bay, then back across Prince of Wales Island, north to Cape Walker, and back to Batty Bay via the north coast of Somerset Island and Prince Leopold Harbour. They discovered no trace of the missing Franklin expedition. In 1853 Bellot again volunteered to go to the Arctic, this time as supernumerary on board the supply ship Phoenix, Captain Edward Inglefield. From Beechey Island, Bellot volunteered to carry dispatches north up Wellington Channel to Captain Sir Edward Belcher who was in that vicinity. Having been driven out of sea on an ice-floe, Bellot disappeared during a gale, and it is assumed that he was blown off the ice into the water and was drowned. Memorials to Bellot may be found on Beechey Island, at Greenwich, England and at Rochefort, France, but probably the most enduring memorial to him is the name ‘Bellot Strait’, applied by Kennedy to the narrow strait between Somerset Island and Boothia Peninsula which represents an integral component of one variant of the northwest passage.

The Last Interglaciation in Northeast Siberia

1995 ◽  
Vol 43 (2) ◽  
pp. 147-158 ◽  
Author(s):  
Anatoly V. Lozhkin ◽  
Patricia M. Anderson
Keyword(s):  
General Circulation ◽  
General Circulation Models ◽  
The Arctic ◽  
The North ◽  
River Terraces ◽  
Atmospheric General Circulation ◽  
Winter Temperatures ◽  
Atmospheric General Circulation Models ◽  
Arctic Coast ◽  
Organic Deposits

AbstractAlluvial, fluvial, and organic deposits of the last interglaciation are exposed along numerous river terraces in northeast Siberia. Although chronological control is often poor, the paleobotanical data suggest range extensions of up to 1000 km for the primary tree species. These data also indicate that boreal communities of the last interglaciation were similar to modern ones in composition, but their distributions were displaced significantly to the north-northwest. Inferences about climate of this period suggest that mean July temperatures were warmer by 4 to 8°C, and seasonal precipitation was slightly greater. Mean January temperatures may have been severely cooler than today (up to 12°C) along the Arctic coast, but similar or slightly warmer than present in other areas. The direction and magnitude of change in July temperatures agree with Atmospheric General Circulation Models, but the 126,000-year-B.P. model results also suggest trends opposite to the paleobotanical data, with simulated cooler winter temperatures and drier conditions than present during the climatic optimum.

Chapter 20 Paleogene history

1997 ◽  
Vol 17 (1) ◽  
pp. 388-417
Keyword(s):  
Early Cretaceous ◽  
The Arctic ◽  
North Coast ◽  
Western Coast ◽  
Central Basin ◽  
Oblique Collision ◽  
The North ◽  
Western Border ◽  
Paleozoic Rocks ◽  
West Spitsbergen

The Paleogene chapter of Svalbard history is a quite distinct one. It begins with an unconformity, albeit a sub-parallel one representing a late Cretaceous hiatus. Resting on Albian and older strata, the Van Mijenfjorden Group of six formations totals a thickness of about 2500 m in the Central Basin of Spitsbergen. The outcrop is ringed by Early Cretaceous strata in a broad syncline (Fig. 20.1). The strata are largely non-marine, coal-bearing sandstones, with interbedded marine shales and they range in age through Paleocene and Eocene.From latest Paleocene through Eocene time the West Spitsbergen Orogeny caused (Spitsbergian) deformation along the western border of the Central Basin, but it is most conspicuous in the folding and thrusting of Carboniferous through Early Cretaceous rocks. The orogen extended westwards to and beyond the western coast of central and southern Spitsbergen including Precambrian and Early Paleozoic rocks, which had already been involved in earlier tectogenesis. The eastward-verging thrusting extended beneath the Tertiary basin and reactivated older faults to the east.In the wider context Svalbard, adjacent to the north coast of Greenland, had been an integral part of Pangea from Carboniferous through Cretaceous time. The northward extension of the Atlantic opening reached and initiated the spreading of the Arctic Eurasia Basin at the beginning of the Paleogene Period. This led to the separation of Svalbard together with the Barents Shelf and northern Europe from Greenland by dextral strike-slip transform faulting. In the course of this progression, oblique collision between northeast Greenland and Svalbard caused

scholarly journals Aspects of the Glaciology of Meighen Island, Northwest Territories, Canada

1965 ◽  
Vol 5 (40) ◽  
pp. 399-410 ◽  
Author(s):  
K. C. Arnold
Keyword(s):  
Snow Accumulation ◽  
The Arctic ◽  
North Coast ◽  
Ice Cap ◽  
The North ◽  
Four Seasons ◽  
Northern Half ◽  
Northern Edge ◽  
Summer Temperatures ◽  
Made In

Abstract Meighen Island lies in the centre of the north coast of the Queen Elizabeth Islands and fronts on the Arctic Ocean. An ice cap of about 76 km.2 covers about one-tenth of the island. Its greatest thickness of 150 m. occurs under the summit, near the south end, which was 268 m. above sea-level in 1960. The northern half of the ice cap is less than 30 m. thick; and the total volume is of the order of 2,000 × 106 m.3. Precipitation is low in the northern Queen Elizabeth Islands, and Meighen Island lies in an area where summer temperatures are lowest. In the winters of 1959–60, 1960–61 and 1961–62, the snow accumulation was 12.6, 18.2 and 14.1 cm. of water equivalent. Some snowfall remained on the higher part of the ice cap in the cold summer of 1961; but the ice cap diminished in volume in each year; by 36 × 106, 72 × 106, 22 × 106 and 91 × 106 m.3 in the 1959, 1960, 1961 and 1962 ablation seasons. If the conditions of these four seasons were maintained the ice cap would disappear in about 100 yr. However, a radio-carbon dating of a saxifrage exposed by the retreat of the ice from a small nunatak near the northern edge gave a date of less than 100 yr., and it appears that the existence of the ice cap might be sensitively related to recent climatic change. Careful surveys were made in 1959, 1960 and 1961 in an attempt to detect movement in the ice cap. Unequivocal evidence is not available from these surveys; but the stake network has been maintained and another survey has recently been completed.

scholarly journals The Coastal Observing System for Northern and Arctic Seas (COSYNA)

Ocean Science ◽  
2017 ◽  
Vol 13 (3) ◽  
pp. 379-410 ◽  
Author(s):  
Burkard Baschek ◽  
Friedhelm Schroeder ◽  
Holger Brix ◽  
Rolf Riethmüller ◽  
Thomas H. Badewien ◽  
...  
Keyword(s):  
Real Time ◽  
The Arctic ◽  
Arctic Seas ◽  
The Public ◽  
The North ◽  
Data Products ◽  
The North Sea ◽  
Arctic Coast ◽  
The Impact

Abstract. The Coastal Observing System for Northern and Arctic Seas (COSYNA) was established in order to better understand the complex interdisciplinary processes of northern seas and the Arctic coasts in a changing environment. Particular focus is given to the German Bight in the North Sea as a prime example of a heavily used coastal area, and Svalbard as an example of an Arctic coast that is under strong pressure due to global change.The COSYNA automated observing and modelling system is designed to monitor real-time conditions and provide short-term forecasts, data, and data products to help assess the impact of anthropogenically induced change. Observations are carried out by combining satellite and radar remote sensing with various in situ platforms. Novel sensors, instruments, and algorithms are developed to further improve the understanding of the interdisciplinary interactions between physics, biogeochemistry, and the ecology of coastal seas. New modelling and data assimilation techniques are used to integrate observations and models in a quasi-operational system providing descriptions and forecasts of key hydrographic variables. Data and data products are publicly available free of charge and in real time. They are used by multiple interest groups in science, agencies, politics, industry, and the public.

scholarly journals II.—The true date of the English Discovery of the American Continent under John and Sebastian Cabot

Archaeologia ◽  
1871 ◽  
Vol 43 (1) ◽  
pp. 17-42
Author(s):  
Richard Henry Major
Keyword(s):  
East Coast ◽  
North Coast ◽  
American Continent ◽  
Terra Firma ◽  
The North ◽  
Great Achievement ◽  
Entire Collection ◽  
To Come ◽  
First Time ◽  
Sound Judgment

While there remain any in this utilitarian age who value accuracy in history, the date of the discovery of the continent of America by English vessels will not be regarded as unimportant. It is well known that Columbus, whose great achievement of 1492 has placed him on a pinnacle of renown which neither rivalry nor detraction can ever eclipse or undermine, was himself preceded in the actual discovery of terra firma by John and Sebastian Cabot. It was not till 1498 that that prince of navigators lighted on the north coast of South America, whereas it is a fact beyond all question that in 1497 John Cabot, accompanied by his son Sebastian, was on the east coast of North America. The question is, whether in that year they discovered that coast for the first time, or whether in 1494 it had been already seen by them, though possibly not explored. Both these suppositions have had their advocates at different periods, but in later years the materials for forming a sound judgment on the question have much increased under our hands, and I should not be occupying your time now if I were not of opinion that the entire collection of documents in our possession is sufficient to enable us to come to a decided conclusion.

scholarly journals Quaternary River Diversions in the London Basin and the Eastern English Channel

2007 ◽  
Vol 51 (3) ◽  
pp. 337-346 ◽  
Author(s):  
D. R. Bridgland ◽  
P. L. Gibbard
Keyword(s):  
North Sea ◽  
East Coast ◽  
Middle Pleistocene ◽  
North Coast ◽  
English Channel ◽  
East Anglia ◽  
The North ◽  
Course Changes ◽  
The North Sea ◽  
The Last Glacial

ABSTRACT The principal river of the London basin, the Thames, has experienced a number of course changes during the Quaternary. Some, at least, of these are known to result directly from glaciation. In the early Quaternary the river flowed to the north of London across East Anglia to the north coast of Norfolk. By the early Middle Pleistocene it had changed its course to flow eastwards near the Suffolk - Essex border into the southern North Sea. The Thames valley to the north of London was blocked by ice during the Anglian/Elsterian glaciation, causing a series of glacial lakes to form. Overflow of these lakes brought the river into its modern valley through London. It is thought that this valley already existed by the Anglian in the form of a tributary of the north-flowing River Medway, which joined the old Thames valley near Clacton. Also during the Anglian/Elsterian glaciation. British and continental ice masses are thought to have joined in the northern part of the North Sea basin, causing a large lake to form between the east coast of England and the Netherlands. It is widely believed that the overflow from this lake caused the first breach in the Weald-Artois Ridge, bringing about the formation of the Strait of Dover. Prior to the glaciation the Thames, in common with rivers from the continent (including the Rhine and Meuse), flowed into the North Sea Basin. It seems that, after the lake overflow, these rivers together drained southwards into the English Channel. Whether this southern drainage route was adopted during all later periods of low sea level remains to be determined, but it seems certain that this was the case during the last glacial.

The Spread of Elminius Modestus Darwin In North-West Europe

1958 ◽  
Vol 37 (2) ◽  
pp. 483-520 ◽  
Author(s):  
D. J. Crisp
Keyword(s):  
East Coast ◽  
Irish Sea ◽  
North Coast ◽  
Long Distance ◽  
North West ◽  
The North ◽  
Competition For Space ◽  
South East England ◽  
The Irish Sea ◽  
Balanus Balanoides

Material collected prior to 1940 indicates that Elminius modestus was not present on British coasts at that time.Elminius increased in abundance in south-east England from 1946 to 1950 and extended its range as far as the Humber, where it halted.Its advance westwards along the south coast was similarly halted at Portland, but by 1948 independent colonies had been established in several of the river systems of Devon and Cornwall, in Milford Haven, and in the Bristol Channel.The first populations in the Irish Sea were in Morecambe Bay. From there Elminius spread rapidly south and west along the north coast of Wales, and more slowly north and west towards Galloway, eventually bridging the sea to the Isle of Man.Detailed observations showed that Elminius advanced along the uniformly favourable north coast of Wales as a definite front moving at a rate of approximately 20–30 km per year. Around Anglesey where tidal currents were stronger it appeared simultaneously in many scattered centres.A distinction is drawn between marginal dispersal taking place under the influence of normal agencies at the boundary of an existing population, and remote dispersal due to an artificial or freak transport over a long distance. In the case of Elminius the maximum distance that is likely to be bridged by marginal dispersal in the absence of strong residual drifts is about 30 miles.Elminius probably first appeared near Southampton, and was introduced into the Thames estuary area probably by remote dispersal. Thence it spread along the east coast and was transported to Holland. Its extension into south Devon, the Bristol Channel, the Irish Sea, and to the French coast must also be attributed to remote dispersal.The main ecological effects of Elminius result from competition for space with Balanus balanoides. Since Elminius breeds in summer, its dominance has a profound effect on the composition of the summer plankton, greatly increasing the number of barnacle nauplii, presumably at the expense of other larvae.

scholarly journals The Walrus

Oryx ◽  
1950 ◽  
Vol 1 (1) ◽  
pp. 10-14
Author(s):  
Colin Matheson
Keyword(s):  
Distinct Species ◽  
The Arctic ◽  
North Coast ◽  
Hudson Bay ◽  
Pacific Walrus ◽  
The North ◽  
The Pacific ◽  
Western Shore ◽  
Far Eastern ◽  
Siberian Coast

The Walrus is confined to the northern circumpolar regions, its range northward apparently extending to the limit of perpetual ice. Now rare in Iceland, Odobenus rosmarus is stated to be still not unfamiliar in Hudson Bay, Davis Strait, and Baffin Bay north to Ellesmere Land, the coasts of Greenland, Spitsbergen, Novaia Zemlia, and the western part of the north coast of Siberia; in all of which regions, however, persecution has greatly diminished its numbers. The species does not extend along the far eastern part of the north Siberian coast, and Walrus are not met with again until the north-eastern extremity of Siberia is reached. Here the Pacific Walrus, which differs somewhat from that of the Atlantic side and is regarded as a distinct species, Odobenus obesus, is reported from Cape Chelagskai, in longitude 170° E., along the Siberian coast as far as northern Kamschatka south to latitude 60°, also on some of the islands in the Bering Sea, and on the opposite coast of Alaska south to about latitude 55° and eastward to Point Barrow. Here again a long gap along the Arctic coast of North America, from Point Barrow in longitude 158° W. to the western shore of Hudson Bay in longitude 97° W., separates the Pacific from the Atlantic Walrus.

scholarly journals The Coastal Observing System for Northern and Arctic Seas (COSYNA)

2016 ◽  
Author(s):  
B. Baschek ◽  
F. Schroeder ◽  
H. Brix ◽  
R. Riethmüller ◽  
T. H. Badewien ◽  
...  
Keyword(s):  
Real Time ◽  
The Arctic ◽  
Arctic Seas ◽  
The Public ◽  
The North ◽  
Data Products ◽  
The North Sea ◽  
Arctic Coast ◽  
The Impact

Abstract. The Coastal Observing System for Northern and Arctic Seas (COSYNA) was established in order to better understand the complex interdisciplinary processes of northern seas and the arctic coasts in a changing environment. Particular focus is given to the German Bight in the North Sea as a prime example for a heavily used coastal area, and Svalbard as an example of an arctic coast that is under strong pressure due to global change. The automated observing and modelling system COSYNA is designed to monitor real time conditions, provide short-term forecasts and data products, and to assess the impact of anthropogenically induced change. Observations are carried out combining satellite and radar remote sensing with various in situ platforms. Novel sensors, instruments, and algorithms are developed to further improve the understanding of the interdisciplinary interactions between physics, biogeochemistry, and the ecology of coastal seas. New modelling and data assimilation techniques are used to integrate observations and models in a quasi-operational system providing descriptions and forecasts of key hydrographic variables. Data and data products are publically available free of charge and in real time. They are used by multiple interest groups in science, agencies, politics, industry, and the public.

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