scholarly journals Late Pleistocene and recent archaeology and geomorphology of the south shore of Harney Lake, Oregon

2000 ◽  
Author(s):  
Keith Gehr
2018 ◽  
Author(s):  
Rebeka Smith ◽  
◽  
Thomas Badamo ◽  
David J. Barclay ◽  
Devorah Crupar ◽  
...  

Ocean Science ◽  
2017 ◽  
Vol 13 (1) ◽  
pp. 31-46
Author(s):  
Joao Marcos Azevedo Correia de Souza ◽  
Brian Powell

Abstract. The dynamical interaction between currents, bathymetry, waves, and estuarine outflow has significant impacts on the surf zone. We investigate the impacts of two strategies to include the effect of surface gravity waves on an ocean circulation model of the south shore of O'ahu, Hawaii. This area provides an ideal laboratory for the development of nearshore circulation modeling systems for reef-protected coastlines. We use two numerical models for circulation and waves: Regional Ocean Modeling System (ROMS) and Simulating Waves Nearshore (SWAN) model, respectively. The circulation model is nested within larger-scale models that capture the tidal, regional, and wind-forced circulation of the Hawaiian archipelago. Two strategies are explored for circulation modeling: forcing by the output of the wave model and online, two-way coupling of the circulation and wave models. In addition, the circulation model alone provides the reference for the circulation without the effect of the waves. These strategies are applied to two experiments: (1) typical trade-wind conditions that are frequent during summer months, and (2) the arrival of a large winter swell that wraps around the island. The results show the importance of considering the effect of the waves on the circulation and, particularly, the circulation–wave coupled processes. Both approaches show a similar nearshore circulation pattern, with the presence of an offshore current in the middle beaches of Waikiki. Although the pattern of the offshore circulation remains the same, the coupled waves and circulation produce larger significant wave heights ( ≈  10 %) and the formation of strong alongshore and cross-shore currents ( ≈  1 m s−1).


2001 ◽  
Vol 38 (11) ◽  
pp. 1601-1613 ◽  
Author(s):  
E A Christiansen ◽  
E Karl Sauer

The Saskatoon Low is a collapse structure that formed as a result of dissolution of salt from the Middle Devonian Prairie Evaporite Formation. In this study, the collapse has affected the Upper Cretaceous Lea Park, Judith River, and Bearpaw formations of the Montana Group; the Early and Middle Pleistocene Mennon, Dundurn, and Warman formations of the Sutherland Group; and the Late Pleistocene Floral, Battleford, and Haultain formations of the Saskatoon Group. Locally, the collapse is about 180 m, which is about equal to the thickness of the salt. The first phase of collapse took place after deposition of the Ardkenneth Member of the Bearpaw Formation and before glaciation or during a pre-Illinoian glaciation. The second phase of collapse occurred during the Battleford glaciation (Late Wisconsinan). Prior to deposition of the Battleford Formation, the Saskatoon Low was glacially eroded, removing the Sutherland Group and the Floral Formation. After the glacial erosion, up to 110 m of soft till of the Battleford Formation and up to 77 m of deltaic sand, silt, and clay of the Haultain Formation were deposited in the Saskatoon Low. Lastly, the South Saskatchewan River eroded up to about 40 m into the deltaic sediment and tills before up to about 15 m of Pike Lake Formation was deposited. The Haultain and Pike Lake formations are new stratigraphic units.


Traditio ◽  
1953 ◽  
Vol 9 ◽  
pp. 213-279 ◽  
Author(s):  
Giles Constable

The years between 1146 and 1148 were signalized in the annals and chronicles of Medieval Europe by Christian campaigns on all fronts against the surrounding pagans and Moslems. The most important of these was directed towards the Holy Land, against the Moslems, who had recently seized Edessa. It consisted of no less than five expeditions. The two largest armies, commanded by the Emperor Conrad III and King Louis VII of France, followed the same route overland across the Balkans to Constantinople; both met with crushing defeats in Asia Minor and finally reached the Holy Land, as best they could, by land and sea. A third force, under Amadeus III of Savoy, moved down Italy, crossed from Brindisi to Durazzo, and joined the army of Louis at Constantinople late in 1147. In August of the same year a naval expedition led by Alfonso of Toulouse left the South of France and arrived in Palestine probably in the spring of 1148. At the same time, a joint Anglo-Flemish naval force sailed along the north coast of Europe, assisted the King of Portugal in the capture of Lisbon, proceeded around the peninsula early in 1148, attacked Faro, and presumably reached the Holy Land later that year. Meanwhile, in the northeast, four armies co-operated in a campaign against the pagan Wends across the river Elbe: a Danish army joined the Saxons under Henry the Lion and Archbishop Adalbero of Bremen in an attack on Dubin; another, larger, army led by Albert the Bear of Brandenburg and many other temporal and spiritual lords advanced against Demmin and Stettin; a fourth expedition, finally, under a brother of the Duke of Poland attacked from the southeast. In 1148, on the south shore of the Mediterranean, a powerful fleet under George of Antioch extended the control of Roger II of Sicily over the entire littoral from Tripoli to Tunis. In the West, four campaigns were directed against the crumbling power of the Almoravides. The Genoese in 1146 sacked Minorca and besieged Almeria. During the following year, the Emperor Alfonso VII of Castile advanced south through Andalusia and captured Almeria with the aid of a strong Genoese fleet, which in 1148 sailed north and joined the Count of Barcelona in his campaign against Tortosa. In the previous year, Alfonso Henriques of Portugal had captured Santarem and secured the assistance of the Anglo-Flemish fleet for an attack on Lisbon, which fell late in 1147.


1969 ◽  
Vol 6 (4) ◽  
pp. 771-774 ◽  
Author(s):  
Douglas S. Rankin ◽  
Ravi Ravindra ◽  
David Zwicker

Previous work in the Gulf of St. Lawrence has yielded an unusually high upper-mantle compressional velocity. In the Gaspé area a more recent determination has yielded a value of 8.75 ± 0.20 km/s for an unreversed profile. The arrival time at a station on the north shore of the St. Lawrence River suggests that there is no major difference in velocity and depth relative to the south shore.


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