An Dracula papillosa in uska species han Liliopsida nga ginhulagway ni Carlyle August Luer ngan Dodson. An Dracula papillosa in nahilalakip ha genus nga Dracula, ngan familia nga Orchidaceae. Waray hini subspecies nga nakalista.

Mga kasarigan

Dracula

Dracula papillosa


AEL Football Club () er en græsk fodboldklub belligende i byen Larisa. Klubben spiller til dagligt i den græske liga .

Fodboldklubber i Grækenland
Etableret i 1964

Athlitiki Enosi Larissa F.C.


65672 Merrick este un asteroid din centura principală de asteroizi.

Descriere
65672 Merrick este un asteroid din centura principală de asteroizi. A fost descoperit pe  la Observatorul Palomar de Carolyn S. Shoemaker și Eugene M. Shoemaker. Asteroidul prezintă o orbită caracterizată de o semiaxă mare de 2,39 ua, o excentricitate de 0,27 și o înclinație de 24,3° în raport cu ecliptica.

Vezi și
 Lista planetelor minore: 65001-66000
 Centura de asteroizi

Referințe

Obiecte astronomice descoperite în 1988
Centura de asteroizi

65672 Merrick


Der Welschlauf ist eine seit 1995 jährlich stattfindende Laufveranstaltung in der Südsteiermark. Neben der klassischen Strecke über die Marathondistanz gibt es ebenso einen Halbmarathon sowie einen Viertelmarathon über 10,8 km, welcher auch als Nordic-Walker-Bewerb ausgetragen wird.Der Lauf wird stets am ersten Samstag im Mai ausgetragen, wobei sich die Laufrichtung jährlich ändert. Der Name Welschlauf steht für "Wies-Ehrenhausen-laufen und schauen" sowie in Anlehnung der Strecke, welche die Welschregion mit der Schilcherregion verbindet.

Strecke

Die Marathonstrecke – je nach Laufrichtung – führt von Wies nach Ehrenhausen und weist ca.  bzw.  Höhenmeter auf. Für die anderen Distanzen findet ein späterer Einstieg in Leutschach bzw. Sulztal statt. Lange Teile der Strecke führen entlang der Südsteirischen Weinstraßen. Entlang der Laufstrecke befinden sich 21 Labestationen. Die Laufstrecke ist während der Veranstaltung (Gemeindestraßen zur Gänze, Landes- und Bundesstraßen teilweise) gesperrt und in beide Richtungen ganzjährig beschildert.

Besonderheiten
 Teamwertung: Beim Bewerb "Gretzl" starten 5 Läufer in ein und derselben Distanz und werden auch gemeinsam bewertet. Für die Siegerehrung am Lauftag gilt die Zeit des Langsamsten für das gesamte Gretzl.
 Maskierte Läufer: Eine Jury bewertet das am tollsten maskierte Team und den tollsten maskierten Einzelläufer.
 Bei einigen Labestationen werden nicht nur isotonische Getränke, sondern auch Wein aus der Region ausgeschenkt.

Statistik
Durch die jährliche Änderung der Laufrichtung sind die Zeiten nur bedingt vergleichbar.

Siegerliste Marathon (seit 1998)

Finisher 2017
 Marathon: 199
 Halbmarathon: 611
 Viertelmarathon: 524
 Nordic Walker – Viertelmarathon: 233
 Gemeindeduell: 525

Finisher 2016
 Marathon: 220
 Halbmarathon: 751
 Viertelmarathon: 622
 Nordic Walker – Viertelmarathon: 204

Weblinks
 Offizielle Website

Einzelnachweise

Marathon mit Halbmarathon
Laufveranstaltung in Österreich

Welschlauf


Héctor Eduardo Berríos Ibarra (Santiago, Chile, 18 de octubre de 1986) es un futbolista chileno. Juega de mediocampista y actualmente esta sin club

Clubes

Palmarés
 Campeonatos nacionales

Referencias
 Ficha en BDFA
 Ficha en Ceroacero
 Ficha en Soccerway

Futbolistas de Santiago de Chile
Futbolistas del Club de Deportes Melipilla en los años 2000
Futbolistas del Club Deportes Concepción en los años 2010
Futbolistas del Club Deportivo Universidad de Concepción en los años 2010
Futbolistas del Club de Deportes Cobresal en los años 2010
Futbolistas del Club de Deportes Iquique en los años 2010

Héctor Berríos


The richly textured landscape of the United States is a product of the dueling forces of plate tectonics, weathering and erosion. Over the 4.5 billion-year history of the Earth, tectonic upheavals and colliding plates have raised great mountain ranges while the forces of erosion and weathering worked to tear them down. Even after many millions of years, records of Earth's great upheavals remain imprinted as textural variations and surface patterns that define distinctive landscapes or provinces.

The diversity of the landscapes of the United States can be easily seen on the shaded relief image to the right. The stark contrast between the 'rough' texture of the western US and the 'smooth' central and eastern regions is immediately apparent. Differences in roughness (topographic relief) result from a variety of processes acting on the underlying rock. The plate tectonic history of a region strongly influences the rock type and structure exposed at the surface, but differing rates of erosion that accompany changing climates can also have profound impacts on the land.

There are twelve main geological provinces in the United States:  Pacific, Columbia Plateau, Basin and Range, Colorado Plateau, Rocky Mountains, Laurentian Upland, Interior Plains, Interior Highlands, Appalachian Highlands, Atlantic Plain, Alaskan, and Hawaiian. Each province has its own geologic history and unique features. This article will describe each province in turn.

Pacific Province
This region is one of the most geologically young and tectonically active in North America. The generally rugged, mountainous landscape of this province provides evidence of ongoing mountain-building.

The Pacific Province straddles the boundaries between several of Earth's moving plates:the source of the monumental forces required to build the sweeping arc of mountains that extends from Alaska to the southern reaches of South America. This province includes the active and sometimes deadly volcanoes of the Cascade Range and the young, steep mountains of the Pacific Border and the Sierra Nevada.

Sierra Nevada

Although the Sierra Nevada and Cascade Range form a nearly continuous barrier along the western edge of the United States, the two ranges really have very little in common. They have been and continue to be formed by quite different geological forces and processes.

The rocks that form the backbone of the Sierra Nevada are mostly granitic rocks that formed during the Mesozoic Era, when non-avian dinosaurs roamed the Earth. At that time, an arc-shaped chain of volcanoes, similar to the present-day Cascade volcanic arc, erupted where the Sierra Nevada now stands. Rising through older Paleozoic rock, molten rock erupted at the surface as lava, but most solidified deep within the earth, forming the gray granitic rocks familiar to any Sierra traveler.

Although from a distance the Sierran rock looks quite similar, it is actually made up of many individual rock bodies that formed from repeated intrusions of magma over many millions of years.

Even as they grew, erosion was wearing away these Mesozoic Era volcanoes. By Late Cretaceous time, about 70 million years ago, the once-deep granitic rocks began to be exposed at the Earth's surface. By a few tens of millions of years ago, so much of the upper part had worn away that the surface of the ancient range had a low relief of just a few thousand feet.

It wasn't until quite recently, geologically speaking, that the Sierra Nevada range as we know it today began to grow. During the Miocene Epoch, less than 20 million years ago, the continental crust east of the Sierra Nevada began to stretch in an east–west direction. The crust broke into a series of north–south-trending valleys and mountain ranges: the beginning of the Basin and Range province.

Less than five million years ago, the range that we now know as the Sierra Nevada began to rise along its eastern margin. Through a combination of uplift of the Sierran block and down-dropping of the area to the east, the Sierra rose upward. Rising far more steeply to the east than the west, the entire Sierra Nevada can be thought of as an enormous tilted fault block with a long, gentle slope westward to California's Central Valley and steep eastern slope.

Not long after the Sierra uplift began, the Earth cooled, marking the beginning of the Pleistocene (Ice Age) Epoch. Glaciers grew in the Sierra highlands and made their way down former stream channels, carving U-shaped valleys. The sheer walls and hanging valleys of Yosemite National Park are a product of this chilly past.

Cascades Volcanic Province
Where the Sierra Nevada ends, a chain of explosive volcanic centers, the Cascade volcanoes, begins. The Cascades Province forms an arc-shaped band extending from British Columbia to Northern California, roughly parallel to the Pacific coastline. Within this region, 13 major volcanic centers lie in sequence like a string of explosive pearls.

Although the largest volcanoes like Mount St. Helens get the most attention, the Cascades is really made up of a band of thousands of very small, short-lived volcanoes that have built a platform of lava and volcanic debris. Rising above this volcanic platform are a few strikingly large volcanoes that dominate the landscape.

The Cascades volcanoes define the Pacific Northwest section of the Ring of Fire, an array of volcanoes that rim the Pacific Ocean. As if volcanic hazards were not enough, the Ring of Fire is also infamous for its frequent earthquakes. In order to understand the origins of this concentrated band of Earth hazards, we have to slice deep into the Earth.

A slice of the Earth from the Pacific Ocean through the Pacific Northwest might look something like the adjacent image. Beneath the Cascades, a dense oceanic plate plunges beneath the North American Plate; a process known as subduction. As the oceanic slab sinks deep into the Earth's interior beneath the continental plate, high temperatures and pressures allow water molecules locked in the minerals of solid rock to escape. The water vapor rises into the pliable mantle above the subducting plate, causing some of the mantle to melt. This newly formed magma rises toward the Earth's surface to erupt, forming a chain of volcanoes (the Cascade Range) above the subduction zone.

A close-up look at the Cascades reveals a more complicated picture than the simple subduction zone shown in the image on the left. Not far off the coast of the North Pacific lies a spreading ridge; a divergent plate boundary made up of a series of breaks in the oceanic crust where new ocean crust is created. On one side of the spreading ridge new Pacific Plate crust is made, then moves away from the ridge. On the other side of the spreading ridge the Juan de Fuca Plate and Gorda Plate move eastward.

There are some unusual features at the Cascade subduction zone. Where the Juan de Fuca Plate sinks beneath the North American Plate there is no deep trench, seismicity (earthquakes) are fewer than expected, and there is evidence of a decline in volcanic activity over the past few million years. The probable explanation lies in the rate of convergence between the Juan de Fuca and North American Plates. These two plates converge at 3–4 centimeters per year at present. This is only about half the rate of convergence of 7 million years ago.

The small Juan de Fuca Plate and two platelets, the Explorer Plate and Gorda Plate are the meager remnants of the much larger Farallon oceanic plate. The Explorer Plate broke away from the Juan de Fuca about 4 million years ago and shows no evidence that it is still being subducted. The Gorda platelet split away between 18 and 5 million years ago and continues to sink beneath North America.

The Cascade Range made its first appearance 36 million years ago, but the major peaks that rise up from today's volcanic centers were born within the last 1.6 million years (during the Pleistocene). More than 3000 vents erupted during the most recent volcanic episode that began 5 million years ago. As long as subduction continues, new Cascade volcanoes will continue to rise.

Columbia Plateau

The Columbia Plateau province is enveloped by one of the world's largest accumulations of lava. Over  of the Earth's surface is covered by it, an area roughly the size of the country of Spain. The topography here is dominated by geologically young lava flows that inundated the countryside with amazing speed, all within the last 17 million years.

Over  of basaltic lava, known as the Columbia River basalts, covers the western part of the province. These tremendous flows erupted between 17 million years ago. Most of the lava flooded out in the first 1.5 million years: an extraordinarily short time for such an outpouring of molten rock.

The Snake River Plain stretches across Oregon, through northern Nevada, southern Idaho, and ends at the Yellowstone Plateau in Wyoming. Looking like a great spoon scooped out the Earth surface, the smooth topography of this province forms a striking contrast with the strong mountainous fabric around it.

The Snake River Plain lies in a distinct depression. At the western end, the base has dropped down along normal faults, forming a graben structure. Although there is extensive faulting at the eastern end, the structure is not as clear.

Like the Columbia River region, volcanic eruptions dominate the story of the Snake River Plain in the eastern part of the Columbia Plateau Province. The earliest Snake River Plain eruptions began about 15 million years ago, just as the tremendous early eruptions of Columbia River Basalt were ending. But most of the Snake River Plain volcanic rock is less than a few million years old, Pliocene age (5-1.6 million years ago) and younger.

In the west, the Columbia River Basalts are just that-almost exclusively black basalt. Not so in the Snake River Plain, where relatively quiet eruptions of soupy black basalt lava flows alternated with tremendous explosive eruptions of rhyolite, a light-colored volcanic rock.

Cinder cones dot the landscape of the Snake River Plain. Some are aligned along vents, the fissures that fed flows and cone-building eruptions. Calderas, great pits formed by explosive volcanism, and low shield volcanoes, and rhyolite hills are also part of the landscape here, but many are obscured by later lava flows.

Geologists usually associate volcanic eruptions with the boundaries between colliding or diverging plates. However, the focus of volcanism at Yellowstone in the Columbia Plateau Province is far inland from the subduction zone that lies along the Oregon and Washington coast. Evidence suggests that some concentrated heat source is melting rock beneath the Columbia Plateau Province, at the base of the lithosphere (the layer of crust and upper mantle that forms Earth's moving tectonic plates). In an effort to figure out why this area, far from a plate boundary, had such an enormous outpouring of lava, scientists established hardening dates for many of the individual lava flows. They found that the youngest volcanic rocks were clustered near the Yellowstone Plateau, and that the farther west they went, the older the lavas.

A probable explanation is that a hot spot, an extremely hot plume of deep mantle material, is rising to the surface beneath the Columbia Plateau Province. We know that beneath Hawaii and Iceland, a temperature instability develops (for reasons not yet well understood) at the boundary between the core and mantle. The concentrated heat triggers a plume hundreds of kilometers in diameter that ascends directly through to the surface of the Earth.

When the hot plume arrives at the base of the lithosphere, some of the lighter rock of the lithosphere rapidly melts. It is this molten lithosphere that becomes the basalt lavas that gush onto the surface to form the Columbia River and Snake River Plain basalts.

The track of this hot spot starts in the west and sweeps up to Yellowstone National Park. The steaming fumaroles and explosive geysers are ample evidence of a concentration of heat beneath the surface. The hot spot is stationary, but the North American plate is moving over it, creating a record of the rate and direction of plate motion.

Basin and Range

The Basin and Range Province includes much of western North America. In the United States, it is bordered on the west by the eastern fault scarp of the Sierra Nevada and spans over  to its eastern border marked by the Wasatch Fault, the Colorado Plateau and the Rio Grande Rift. The Basin and Range Province extends north to the Columbia Plateau and south as far as the Trans-Mexican Volcanic Belt in Mexico, though the southern boundaries of the Basin and Range are debated.

The Basin and Range province has a characteristic topography that is familiar to anyone who ventures across it. Steep climbs up elongate mountain ranges alternate with long treks across flat, dry deserts. This basic topographic pattern extends from eastern California to central Utah, and from southern Idaho into the state of Sonora in Mexico. The forces which created this distinct topography lie deep beneath the surface.

Within the Basin and Range Province, the Earth's crust (and upper mantle) has been stretched up to 100% of its original width. The entire region has been subjected to extension that thinned and cracked the crust as it was pulled apart, creating large faults. Along these roughly north–south-trending faults mountains were uplifted and valleys down-dropped, producing the distinctive alternating pattern of linear mountain ranges and valleys of the Basin and Range province.

Although there are other types of faults in the Basin and Range province, the extension and crustal stretching that have shaped the present landscape produce mostly normal faults. The upthrown side of these faults form mountains that rise abruptly and steeply, and the down-dropped side creates low valleys. The fault plane, along which the two sides of the fault move, extends deep in the crust, usually an angle of 60 degrees. In places, the relief or vertical difference between the two sides is as much as .

As the rocky ranges rise, they are immediately subject to weathering and erosion. The exposed bedrock is attacked by water, ice, wind and other erosional agents. Rock particles are stripped away and wash down the mountain sides, often covering young faults until they rupture again. Sediment collects in the adjacent valleys, in some places burying the bedrock under thousands of feet of rock debris.

Clarence Dutton famously compared the many narrow parallel mountain ranges that distinguish the unique topography of the Basin and Range to an "army of caterpillars marching toward Mexico", which is a helpful way to visualize the overall appearance of the region. The Basin and Range province should not be confused with The Great Basin, which is a sub-section of the greater Basin and Range physiographic region defined by its unique hydrological characteristics (internal drainage).

Great Basin

The Great Basin is the geographical and hydrological region comprising most of Nevada, southern Oregon and Idaho, western Utah, and a little of eastern California. Characterized by internal drainage, this region's surface water sources evaporate or percolate before they can flow to the ocean.

The Basin and Range province's dynamic fault history has profoundly affected the Great Basin's water drainage system. Most precipitation in the Great Basin falls in the form of snow that melts in the spring. Rain that reaches the ground, or snow that melts, quickly evaporates in the dry desert environment. Some of the water that does not evaporate sinks into the ground to become ground water. The remaining water flows into streams and collects in short-lived lakes called playas on the valley floor and eventually evaporates. Any water that falls as rain or snow into this region does not escape out of it; not one of the streams that originate within this basin ever find an outlet to the ocean. The extent of internal drainage, the area in which surface water cannot reach the ocean, defines the geographic region called the Great Basin.

The Great Basin's internal drainage results from blockage of water movement by high fault-created mountains and by lack of sufficient water flow to merge with larger drainages outside of the Great Basin. This internally-drained area occupies approximately , including most of Nevada, a large part of Utah, and portions of Idaho, California, and Oregon. Much of the present-day Great Basin would drain to the sea, just as it did in the recent Ice Ages, if there were more rain and snowfall.

Colorado Plateau

The Colorado Plateau is roughly centered on the Four Corners region of the southwestern United States. The province covers an area of 337,000 km2 (130,000 mi2) within western Colorado, northwestern New Mexico, southern and eastern Utah, and northern Arizona. About 90% of the area is drained by the Colorado River and its main tributaries: the Green, San Juan, and Little Colorado.

The sculptured beauty and brilliant colors of the Colorado Plateau's sedimentary rock layers have captured the imaginations of countless geologists. This is a vast region of plateaus, mesas, and deep canyons whose walls expose rocks ranging in age from billions to just a few hundred years old.

Ancient Precambrian rocks, exposed only in the deepest canyons, make up the basement of the Colorado Plateau. Most are metamorphic rocks formed deep within the Earth while continental collision on a grand scale produced the nucleus of the North American continent well over a billion years ago. Igneous rocks injected millions of years later form a marbled network through parts of the Colorado Plateau's darker metamorphic basement.

These deeply-formed rocks were uplifted, eroded, and exposed for eons. By 600 million years ago, North America had been beveled off to a remarkably smooth surface. It is on this crystalline rock surface that the younger, more familiar layered rocks of the Colorado Plateau were deposited.

Throughout the Paleozoic Era, the Colorado Plateau region was periodically inundated by tropical seas. Thick layers of limestone, sandstone, siltstone, and shale were laid down in the shallow marine waters. During times when the seas retreated, stream deposits and dune sands were deposited or older layers were removed by erosion. Over 300 million years passed as layer upon layer of sediment accumulated.

It was not until the upheavals that coincided with the formation of the supercontinent Pangea began about 250 million years ago that deposits of marine sediment waned and terrestrial deposits dominate. The Mesozoic Era sedimentary deposits are striking. Great accumulations of dune sand hardened to form sweeping arcs in cross-bedded sandstone. Eruptions from volcanic mountain ranges to the west buried vast regions beneath ashy debris. Short-lived rivers, lakes, and inland seas left sedimentary records of their passage.

One of the most geologically intriguing features of the Colorado Plateau is its remarkable stability. Relatively little rock deformation (e.g., faulting and folding) has affected this high, thick crustal block within the last 600 million years or so. In contrast, the plateau is surrounded by provinces that have suffered severe deformation. Mountain building thrust up the Rocky Mountains to the north and east and tremendous, earth-stretching tension created the Basin and Range Province to the west and south.

Although the Basin and Range and Colorado Plateau may seem to have little in common, their geological stories are intimately intertwined. In the early part of this Era (Paleogene Period), both regions had low elevations of probably less than 1 kilometer. Geologists are still gathering evidence and debating what came next.

Beginning about 20 million years ago, during the Miocene Epoch, both the Basin and Range and Colorado Plateau regions were uplifted as much as 3 kilometers. Great tension developed in the crust, probably related to changing plate motions far to the west. As the crust stretched, the Basin and Range Province broke up into a multitude of down-dropped valleys and elongate mountains. Yet for some reason not fully understood, the neighboring Colorado Plateau was able to preserve its structural integrity and remained a single tectonic block. Eventually, the great block of Colorado Plateau crust rose a kilometer higher than the Basin and Range.

As the land rose, the streams responded by cutting ever deeper stream channels. The most well-known of these streams, the Colorado River, began to carve the Grand Canyon less than 6 million years ago. The forces of erosion have exposed the vivid kaleidoscope of rock layers that make the Colorado Plateau a mecca for rock lovers.

Rocky Mountain System

The Rockies form a majestic mountain barrier that stretches from Canada through central New Mexico. Although formidable, a look at the topography reveals a discontinuous series of mountain ranges with distinct geological origins.

The rocks making up the mountains were formed before the mountains were raised. The cores of the mountain ranges are in most places formed of pieces of continental crust that are over one billion years old. In the south, an older mountain range was formed 300 million years ago, then eroded away. The rocks of that older range were reformed into the Rocky Mountains.

The Rocky Mountains took shape during a period of intense plate tectonic activity that formed much of the rugged landscape of the western United States. Three major mountain-building episodes reshaped the west from about 170 to 40 million years ago (Jurassic to Cenozoic Periods). The last mountain building event, the Laramide orogeny, (about 70-40 million years ago) the last of the three episodes, is responsible for raising the Rocky Mountains.

During the last half of the Mesozoic Era, the Age of the Dinosaurs, much of today's California, Oregon, and Washington were added to North America. western North America suffered the effects of repeated collision as slabs of ocean crust sank beneath the continental edge. Slivers of continental crust, carried along by subducting ocean plates, were swept into the subduction zone and scraped onto North America's edge.

About 200–300 miles inland, magma generated above the subducting slab rose into the North American continental crust. Great arc-shaped volcanic mountain ranges grew as lava and ash spewed out of dozens of individual volcanoes. Beneath the surface, great masses of molten rock were injected and hardened in place.

For 100 million years the effects of plate collisions were focused very near the edge of the North American plate boundary, far to the west of the Rocky Mountain region. It was not until 70 million years ago that these effects began to reach the Rockies.

The growth of the Rocky Mountains has been one of the most perplexing of geologic puzzles. Normally, mountain building is focused between 200 and 400 miles inland from a subduction zone boundary, yet the Rockies are hundreds of miles farther inland. Although geologists continue to gather evidence to explain the rise of the Rockies, the answer most likely lies with an unusual subducting slab.

At a 'typical' subduction zone, an oceanic plate typically sinks at a fairly high angle (see above). A volcanic arc grows above the subducting plate. During the growth of the Rocky Mountains, the angle of the subducting plate may have been significantly flattened, moving the focus of melting and mountain building much farther inland than is normally expected.

It is postulated that the shallow angle of the subducting plate greatly increased the friction and other interactions with the thick continental mass above it. Tremendous thrusts piled sheets of crust on top of each other, building the extraordinarily broad, high Rocky Mountain range.

As of 60 million years ago, the Rockies were like Tibet: a high plateau, probably  above sea level. Since then, erosion stripped away the high rocks, revealing the ancestral rocks beneath, and forming the current landscape of the Rockies. Periods of glaciation occurred from the Pleistocene Epoch (1.8 million–70,000 years ago) to the Holocene Epoch (fewer than 11,000 years ago). The ice ages left their mark on the Rockies, forming extensive glacial landforms, such as U-shaped valleys and cirques.

Laurentian Upland

Every continent has a core of very ancient metamorphic rocks. The Superior Upland Province is the southern extension of the Laurentian Upland Province, part of the nucleus of North America called Canadian Shield. The basement rocks of the Laurentian Upland Province were metamorphosed about 2500 million years ago in a mountain-building collision of tectonic plates called the Kenoran Orogeny.

The rocks of the Superior Upland are mostly Precambrian metamorphic rocks and overlying Paleozoic rocks (Cambrian) covered by a thin veneer of glacial deposits left behind when glaciers melted at the end of the Pleistocene Ice Age. If we could strip away all of the younger rocks deposited on top of buried Precambrian basement, you would see a landscape of low relief. The topography of the Precambrian rocks is very subdued, with barely 500 feet difference between the highest point and the lowest. Clearly, this region was exposed to a very long period of erosion in the very distant past which beveled the original mountainous surface to a gently undulating surface. The present surface is not much different. Hills rise just a few hundred feet above the surrounding countryside. The highest of these, such as Rib Hill, Wisconsin, are made up mostly of resistant quartzite or granite.

The structure of Superior Upland rock is quite complex. Folds and faults, most dating back to Precambrian time, record several episodes of mountain-building. The plate collisions that formed the core of our continent left behind a striking structural trend. Ridges and valleys are strongly aligned along this northeast–southwest trend. Lake Superior is an example of this northeast–southwest structural trend. Ridges of erosion-resistant rock rise above valleys and carved into weaker rock units.

The effects of repeated glaciation have left their mark on the Superior Upland. The present glacial topography is the product of the most recent glaciation that ended just 10,000 years ago. During the Late Wisconsin, the last glaciation of the Pleistocene Epoch, a massive continental ice sheet grew first in the north, then gradually expanded southward. Several thick finger-like lobes of glacial ice engulfed the region as they moved through the Superior basin. Rocks of all sizes were plucked and scoured from farther north and carried along by the icy mass. When the continental ice sheets melt, they left behind an assortment of rock called glacial drift that covers much of the Superior Upland landscape.

Interior Plains
The Interior Plains is a vast region that spreads across the stable core of North America. This area had formed when several small continents collided and welded together well over a billion years ago, during the Precambrian. Precambrian metamorphic and igneous rocks now form the basement of the Interior Plains and make up the stable nucleus of North America. With the exception of the Black Hills of South Dakota, the entire region has low relief, reflecting more than 500 million years of relative tectonic stability.

Throughout the Paleozoic and Mesozoic Eras the mostly low-lying Interior Plains region remained relatively unaffected by the mountain-building tectonic collisions suffered by the western and eastern margins of the continent.

During much of the Mesozoic Era, the North American continental interior was mostly well above sea level, with two notable exceptions. During part of the Jurassic (208-144 million years ago), rising seas flooded the low-lying areas of the continent. Much of the Interior Plains eventually lay submerged beneath the shallow Sundance Sea.

Sediments eroding from the rising Rocky Mountains to the west washed into the sea and deposited as layered wedges of fine debris. As sand, mud, and clays accumulated, the Sundance Sea retreated northward. Preserved within the multi-hued sandstones, mudstones, and clays that made up the shoreline, are the remains of countless dinosaurs that roamed the Sundance coast.

The fossil assemblages concealed within the sedimentary layers of the Morrison Formation are among the world's richest. In some areas, bones of many dinosaurs are concentrated in a very small area, indicating that they were carried during floods, then deposited together beside a stream.

Once again, during the Cretaceous Period (144-65 million years ago), record high sea levels flooded the continental interior with shallow seas.

The Interior Plains continued to receive deposits from the eroding Rocky Mountains to the west and Appalachian and Ozark/Ouachita Mountains to the east and south throughout the most recent Era, the Cenozoic. The flatness of the Interior Plains is a reflection of the platform of mostly flat-lying marine and stream deposits laid down in the Mesozoic and Cenozoic Eras.

Appalachians, Interior Highlands, and Atlantic Plains

The rocks of the Appalachian, Ouachita,  Ozark Mountains are old and share a common origin. They largely consist of sedimentary rocks of Paleozoic age that were deposited on the sea floor and are presently folded and faulted. The Appalachians also have volcanic rocks and slivers of ancient sea floor. These mountains were once part of a mighty uplifted mountain range that stretch from the Appalachian Highlands through Texas.

During the earliest Paleozoic Era, the continent that would later become North America straddled the equator. The Appalachian region was a passive plate margin, not unlike today's Atlantic Coastal Plain Province. During this interval, the region was periodically submerged beneath shallows seas. Thick layers of sediment and carbonate rock was deposited on the shallow sea bottom when the region was submerged. When seas receded, terrestrial sedimentary deposits and erosion dominated.

During the middle Ordovician Period (about 440–480 million years ago), a change in plate motions set the stage for the first Paleozoic mountain building event (Taconic orogeny) in North America. The once quiet, Appalachian passive margin changed to a very active plate boundary when a neighboring oceanic plate, the Iapetus, collided with and began sinking beneath the North American craton. With the birth of this new subduction zone, the early Appalachians were born.

Along the continental margin, volcanoes grew, coincident with the initiation of subduction. Thrust faulting uplifted and warped older sedimentary rock laid down on the passive margin. As mountains rose, erosion began to wear them down. Streams carried rock debris downslope to be deposited in nearby lowlands.

This was just the first of a series of mountain building plate collisions that contributed to the formation of the Appalachians. Mountain building continued periodically throughout the next 250 million years (Caledonian, Acadian, Ouachita, Hercynian, and Alleghenian orogenies). The Pangean supercontinent began to take shape. Microplates, smaller bits of crust too small to be called continents, were swept in, one by one, to be welded to the growing mass.

By about 300 million years ago (Pennsylvanian Period) Africa was approaching North American craton. The collisional belt spread into the Ozark-Ouachita region and through the Marathon Mountains of Texas. Continent vs. continent collision raised the Appalachian-Ouachita chain to lofty, Himalayan-scale ranges. The massive bulk of Pangea was completed near the end of the Paleozoic Era (Permian Period) when Africa (Gondwana) plowed into the continental agglomeration, with the Appalachian-Ouachita mountains near the core. From about 280-230 million years ago, (Late Paleozoic Era until the Late Triassic) the continent we now know as North America was continuous with Africa, South America, and Europe.

During the Late Triassic, Pangea began to be torn apart when a three-pronged fissure grew between Africa, South America, and North America. Rifting began as magma welled up through the weakness in the crust, creating a volcanic rift zone. Volcanic eruptions spewed ash and volcanic debris across the landscape as these severed continent-sized fragments of Pangea diverged. The gash between the spreading continents gradually grew to form a new ocean basin, the Atlantic. The rift zone known as the mid-Atlantic ridge continued to provide the raw volcanic materials for the expanding ocean basin.

North America was slowly pulled westward away from the rift zone. The thick continental crust that made up the new east coast collapsed into a series of down-dropped fault blocks that roughly parallel today's coastline. At first, the hot, faulted edge of the continent was high and buoyant relative to the new ocean basin. As the edge of North America moved away from the hot rift zone, it began to cool and subside beneath the new Atlantic Ocean. This once-active divergent plate boundary became the passive, trailing edge of westward moving North America. In plate tectonic terms, the Atlantic Plain is known as a classic example of a passive continental margin.

During the rifting, South America tore away from North America and headed southward. The ocean flooded into the opening between the two continents, forming the Gulf of Mexico. A record of this rifting event remains as an indelible mark on the landscape called Mississippi Embayment. It is this embayment that ripped the dramatic gap between the southern Appalachians and the Ouachita-Ozark Highlands.

Weathering and erosion prevailed, and the mountains began to wear away. By the end of the Mesozoic Era, the Appalachian-Ouachita Mountains had been eroded to an almost flat plain. Sediments eroded from these highlands were carried east and southward by streams and gradually covered the faulted continental margin, burying it under a wedge, thousands of feet thick, of layered sedimentary and volcanic debris. Today most Mesozoic and Cenozoic sedimentary rock layers that lie beneath much of the coastal plain and fringing continental shelf remain nearly horizontal or tilt gently toward the sea.

During the Cenozoic, the geology of the different regions diverged. The Appalachians started to uplift, while the Ouachita and Ozarks did not. The uplift rejuvenated the streams, which rapidly responded by cutting downward into the ancient bedrock. Some streams flowed along weak layers that define the folds and faults created many millions of years earlier. Other streams downcut so rapidly that they cut right across the resistant folded rocks of the mountain core, carving canyons across rock layers and geologic structures.

Alaska

Most of Alaska consists of terranes accreted by collisions with island arcs carried in over the last 160 million years. These terranes were caused by the subduction of the Farallon, Kula, and Pacific plates sequentially. Currently, the Pacific plate is subducting beneath Alaska, producing the Aleutian arc series of volcanoes through the Alaskan Peninsula and Aleutian Islands.

One of the sutures left by terrane addition is the Denali Fault, which curves through south-central Alaska. The Denali Fault bends just north of Denali. The combination of the subduction of the Pacific plate and the bend in the Denali Fault causes Denali to be the highest mountain in North America.

Hawaii

The State of Hawaii consists of a chain of islands, or archipelago. The archipelago developed as the Pacific plate moved slowly northwestward over a hotspot in the Earth's mantle at a rate of approximately  per million years. Thus, the southeast island (Hawaii) is volcanically active whereas the islands on the northwest end of the archipelago are older and typically smaller, due to longer exposure to erosion. The age of the archipelago has been estimated using potassium-argon dating methods. From this study and others, it is estimated that the northwesternmost island, the Kure Atoll, is the oldest at approximately 28 million years (Ma); while Hawaii, is approximately 0.4 Ma (400,000 years). The only active volcanism in the last 200 years has been on Hawaii and on the submerged but growing volcano to the extreme southeast, Kamaʻehuakanaloa (formerly Loihi).

Almost all of the magma of the hotspot has the composition of basalt, and so the Hawaiian volcanoes are composed almost entirely of this igneous rock. There is very little coarser-grained gabbro and diabase. Nephelinite is exposed on the islands but is extremely rare. The majority of eruptions in Hawaii are Hawaiian-type eruptions because basaltic magma is relatively fluid compared with magmas typically involved in more explosive eruptions, such as the andesitic magmas that produce some of the spectacular and dangerous eruptions around the margins of the Pacific basin.

References

Geology of the United States


O Dia é Nosso é um filme brasileiro de 1941, dirigido por Milton Rodrigues, a partir dos diálogos de José Lins do Rego e com produção de Adhemar Gonzaga.

Elenco
Genésio Arruda ...Guarabira
Oscarito ...Dr. Lemos
Paulo Gracindo ...Campos
Nelma Costa... Enfermeira Laura
Roberto Acácio ...Dr. Luís
Manoel Rocha ...Dono do hotel
Sadi Cabral ...Vendedor de bilhetes
Pinto Filho ...Orador
Palmeirim Silva
Ferreira Maia
Alda Verona
Paulo Celestino
Carlos Barbosa
Júlia Vidal

Ligações externas

Filmes do Brasil de 1941
Filmes de comédia do Brasil
Filmes em preto e branco
Filmes de comédia da década de 1940
Filmes em língua portuguesa

O Dia é Nosso


María Antonia Bolívar Palacios (Caracas, Venezuela, 1 de noviembre de 1777 – Caracas, 7 de octubre de 1842) fue la primera hija del matrimonio formado por María de la Concepción Palacios y Blanco y Juan Vicente Bolívar y Ponte, por lo tanto, hermana mayor de Simón Bolívar.

Biografía

Infancia y vida familiar
Su padre murió en 1786. Su madre tuvo que hacerse cargo de la crianza de ella y de sus tres hermanos (Juan Vicente, Juana y Simón). En 1792 murió María de la Concepción y los niños quedaron a cargo del abuelo materno Feliciano Palacios de Aguijare y Arrizaría-Sojo y Gil de Arriara, pero María Antonia, que estaba próxima a cumplir quince años de edad, contrajo matrimonio el 22 de octubre de ese mismo año, con su primo en tercer grado, hijo de su tía abuela María Petronila Palacios y Sojo, Pablo Clemente y Palacios, quien tenía 21 años. Su esposo era un hombre enfermizo con una ya incipiente demencia.

Fue en casa de María Antonia, donde el entonces adolescente Simón Bolívar se refugió el 23 de julio de 1795 cansado del carácter huraño de su tutor y tío Carlos Palacios. Pablo Clemente, tío político de Simón, solicitó a la Real Audiencia de Caracas que aprobara que el adolescente permaneciera en su casa, pero Carlos Palacios se negó a esta petición. María Antonia Bolívar alegó ante la Audiencia que había visto a su hermano «solo por las calles y paseos, a pie y a caballo, en junta con muchachos que no son de su clase». El 5 de agosto Simón es sacado por la fuerza de la casa de su hermana y restituido a la casa de su tutor.

En 1793 nació su primera hija Josefa Clemente Bolívar y, posteriormente, Pablo Secundino Clemente Bolívar (1795), Anacleto Clemente Bolívar (13 de julio de 1796), Valentina Clemente Bolívar (1801) Juana Teresa Clemente Bolívar (1802) y Concepción Clemente Boliviar (1805). A fines de octubre de 1803, Simón Bolívar, dolido por el reciente fallecimiento de su esposa, se va a Europa y se lleva con él a los niños Anacleto y Pablo Secundino y los inscribe en un colegio de Soreze, en Francia.

Etapa independentista
En 1814, cuando cae la Segunda República de Venezuela huye hacia Curazao junto con su esposo y todos sus hijos (Anacleto y Pablo Secundino habían regresado de Francia en 1809). También la acompaña su hermana Juana Bolívar Palacios junto con sus hijos Jorge, Fernando y Benigna. Las dos hermanas y sus hijos son auxiliadas por el mercader sefardita Mordechay Ricardo. En 1816, estando aún en Curazao, se casa su hija Valentina con Gabriel Camacho. En 1817 sale hacia Cuba. En todos estos años, desde La Habana dirige cartas a la Real Audiencia de Caracas pidiendo el desembargo de sus bienes. Lo logra ese mismo año y en 1819 el propio Rey Fernando VII de España le concede una pensión. En 1820 sus hijos Anacleto y Valentina (ésta junto con su esposo) regresan a Caracas. El 19 de septiembre de 1821 fallece su esposo y poco después, María Antonia, acompañada por sus hijos Josefa y Pablo, viaja a Filadelfia donde visita a su sobrino Fernando Simón Bolívar Tinoco que cursa estudios en esa ciudad. Regresa a Caracas ese mismo año y se dedica a la administración de los bienes de la familia.

Posición ante la Independencia
María Antonia Bolívar no fue partidaria de la Independencia. En 1813, mientras su hermano, en Trujillo, lanzaba el Decreto de Guerra a Muerte ella escondía y protegía a consumados realistas en su casa en Caracas. En 1814, cuando la capital estaba a punto de caer en manos realistas, Bolívar ordenó la evacuación de la ciudad. María Antonia se negaba a irse, pero su hermano la convenció de que al caer Caracas no tendrían clemencia con ella. Así fue que salió de Venezuela a Curazao, con sus hijos, y con su hermana Juana. En 1816, desde Curazao, le escribió una carta al rey de España donde le pedía que no la penalizara por llevar el apellido Bolívar porque ella seguía siendo fiel a la monarquía.

A pesar de esto, la relación entre Simón y María Antonia era cordial. Ambos mantuvieron estrecho contacto epistolar mientras aquel se encontraba dirigiendo la Guerra de Independencia del Perú.

Fallecimiento
Después de la muerte del Libertador, María Antonia Bolívar se dedicó a la vida hogareña y a la administración de los bienes de la familia. También solicitó tenazmente al gobierno venezolano que se repatriaran los restos de Bolívar. Vivió sus últimos años en una casa de Hacienda, propiedad de la familia, ubicada en Macarao en las afueras de Caracas (hoy en ruinas). Murió el 7 de octubre de 1842, dos meses antes de que trajeran los restos de su ilustre hermano.
Le sobrevivieron sus seis hijos. Pablo Secundino, quien tuvo cuatro hijos naturales, un varón y tres mujeres. Una de ellas, Elena de Jesús Clemente se casó con Manuel Montufar, quien fue el introductor del telégrafo en Venezuela. Valentina y Gabriel Camacho tuvieron siete hijos, cuatro mujeres y tres varones. Uno de ellos, Juan Vicente Camacho Clemente, fue diplomático del gobierno peruano. Anacleto Clemente se había casado en 1821 con Rosa Rodríguez del Toro y no dejó descendencia. La causa de su muerte es desconocida. Juana se casó en 1817 y tuvo 6 hijos murió en 1860 mientras que su hermana Concepción a la edad de 18 años con José María Beltrán y Belgrano y tuvieron 8 hijos, se desconoce la fecha o causa de su muerte.

Restos mortales
A fines de julio de 2010, y en el marco de la investigación llevada a cabo por el gobierno de Venezuela para determinar si los restos que están en el Panteón Nacional en Caracas son verdaderamente de Simón Bolívar, se procedió a la exhumación de los restos de María Antonia que se encuentran en la Catedral de Caracas para extraerles una pieza dental y comparar el ADN mitocondrial con el obtenido en los restos de Bolívar. Los resultados fueron dados a conocer a fines de julio de 2011 y se determinó que los restos en la cripta de la Catedral de Caracas corresponden a María Antonia Bolívar ya que su ADN mitocondrial coincide con el de su hermano. En la Catedral de Caracas también reposan los restos de los padres de Bolívar, de su otra hermana, Juana Nepomucena Bolívar, y su esposa María Teresa del Toro y Alayza.

Varios

Fue María Antonia Bolívar la que acogió en su casa a la ya anciana Negra Matea, considerada la Primera Maestra del Libertador, y quien la acompañará durante su estadía en Curazao y Cuba. También, sin base comprobada se dice que el nieto de María Antonia, Miguel Simón Camacho, nacido en 1824, era realmente hijo natural de Simón Bolívar y lo criaron como si hubiera sido hijo de Valentina Clemente Bolívar y de su esposo Gabriel Camacho.

Hacia 1834 y ya con casi sesenta años de edad, María Antonia comenzó lo que a todos luces (sobre la base de los documentos de la época) fue una relación amorosa con un joven de unos veinte años de edad de nombre José Ignacio Padrón.

Bibliografía
Garrido, M (2006). Reseña de La criolla principal, María Antonia Bolívar, hermana del Libertador, de Inés Quintero. Historia Crítica. N.º 31. Universidad de los Andes, Colombia.

Enlaces externos

Caraqueñas
Familia Bolívar
Familia Palacios (Venezuela)

María Antonia Bolívar Palacios


Reşat Çiğiltepe (1879; İstanbul - 27 Ağustos 1922; Çiğiltepe, Sandıklı), Türk asker.

Büyük Taarruz sırasında Çiğiltepe'yi söz verdiği saatte alamaması üzerine intihar etmiş ünlü komutandır. Reşat Bey, I. Dünya Savaşı'nda üstün kahramanlıkları ile dikkat çekti. Türk Kurtuluş Savaşı sırasında yarbay rütbesi ile I. ve II. İnönü ve Sakarya muharebelerine katıldı. Son olarak 57. Tümen Komutanlığı görevine atandı. Büyük Taarruz'un ikinci gününde Çiğiltepe'yi geri alma emrini Başkomutan Mareşal Gazi Mustafa Kemal Paşa'ya söz verdiği sürede yerine getiremeyince intihar etti. Ölümünden sonra kırmızı şeritli İstiklâl Madalyası ile onurlandırıldı. Türkiye Cumhurbaşkanı Mustafa Kemal Atatürk tarafından ailesine "Çiğiltepe" soyadı verildi. Albay Reşat bey olarak da bilinmektedir.

Yaşamı
1879'da İstanbul'da doğdu. Babası Süleymaniye mutasarrıflığından emekli Ziya Paşa, annesi Şevkiye Hanım'dır. Babası, doğumunun ertesi senesi hayatını kaybetti.

1893 yılında girdiği Harp Okulunu 1896'da bitirerek ordunun farklı komuta kademelerinde görev yaptı. Balkan Savaşları'na katıldı, Yanya savunmasında yaralandı; bu görevdeki başarısından ötürü binbaşı rütbesine terfi etti. 1915 yılında seferberliğin ilanından sonra Çanakkale Cephesi'nde görevlendirildi.

I. Dünya Savaşı
I. Dünya Savaşı'nda Çanakkale Cephesi'nde olağanüstü kahramanlığı ile dikkatleri çektikten sonra 17. Alay Komutanlığı görevine getirildi. Bu görevdeyken Muş'un Rus işgalinden kurtarılmasında da önemli rol oynadı ve 16. Kolordu Komutanı Mustafa Kemal Paşa'nın takdirlerini kazandı. Ayrıca 5. ve 4. rütbeden Mecidi Nişanı, Gümüş Muharebe, Liyakat, Tahsiliye, Alman ve Avusturya Harp, Demir Haç Nişanı ile taltif edildi. 53. Tümen Komutanlığı'na getirilerek Suriye Cephesi'nde görevlendirildi.

1918'de İngilizlere esir düştü. Aralık 1919'da bir yıllık esaretten kurtulduktan sonra İstanbul İkinci Sıkıyönetim Askeri Mahkemesi üyeliğine verildiyse de dilekçe verip Türk Kurtuluş Savaşı'na katılmak üzere İnebolu üzerinden Ankara'ya geçti.

Kurtuluş Savaşı

Mustafa Kemal Paşa tarafından 11. Kafkas Tümeni (sonradan 21. Tümen) Komutanlığı'na atandı. Yarbay rütbesi ile I. ve II. İnönü ve Sakarya muharebelerine katıldı. 1 Mart 1922 yılında Miralay rütbesine terfi etti ve 57. Tümen Komutanlığı görevine atandı. Bizzat Başkomutan Mustafa Kemal Paşa tarafından, Büyük Taarruz'un ikinci gününde, muharebenin kaderini etkileyecek en kritik mevkilerden olan Sincanlı Ovası'ndan Dumlupınar'a kadar tüm yolların önündeki en stratejik engel olan Çiğiltepe'yi düşmandan temizlemesi emredildi. Ne var ki bu tepenin önemini çok iyi bilen Yunan Başkomutanı General Nikolaos Trikupis başarılı bir direniş gösterdi. 27 Ağustos 1922 sabahı Mustafa Kemal Paşa'ya telefonda kuşattıkları tepeyi yarım saat sonra alacaklarını bildirmesine rağmen bunu başaramayınca intihar ederek hayatına son verdi. Çiğiltepe, Reşat Bey'in intiharından birkaç saat sonra düşmandan temizlendi.

Ölümünden sonra
Reşat Bey'in cenazesi, bir gün sonra Sandıklı Hastanesine getirildi ve yıllarca bu ilçedeki anıtlı kabristanında yattı. Naaşı, 1988 yılında Ankara Devlet Mezarlığı'na nakledildi. Sandıklı halkı şehidin nakline karşı çıkmış ancak o günün şartlarında fazla direnememişti. Sandıklı'daki mezar boş olmasına rağmen hâlâ muhafaza edilmektedir.

Vefatının sonrasında TBMM kendisi adına ailesine kırmızı şeritli İstiklâl Madalyası takdim etti. Soyadı Kanunu çıktığında Türkiye Cumhuriyeti Cumhurbaşkanı Mustafa Kemal Atatürk tarafından ailesine "Çiğiltepe" soyadı verildi. Çiğiltepe'de onun ve hayatını kaybeden diğer askerlerin anısına yaptırılan şehitlik, 22 Haziran 1996 tarihinde hizmete açıldı. Girişte Reşat Bey'in bronz bir büstü bulunur.

Hayatı emekli Tümgeneral Cihangir Akşit tarafından "Çiğiltepe: Miralay Reşat Bey ve Vatan Savunmasında 27 Yıl" adıyla romanlaştırıldı.

Albay Reşat Çiğiltepe'nin adı, Ankara-Mamak'taki ortaokula verilmiş olsa da daha sonra 2020'de adı bu okuldan silinmiş ve yerine okula bağış yapan kişinin adı verilmiştir.

Ankara Büyükşehir Belediyesi Meclisinin 14 Aralık 2020 tarihinde toplantısındaki 1796 no.lu karar ile Kurtuluş Savaşı askerlerinden biri olan Reşat Çiğiltepe isminin Mamak ilçesi sınırları içerisinde bulunan ortaokuldan silindiği ve isminin yaşatılması için uygun görülecek cadde ve sokakta değerlendirilmesi istenildiğinden Mamak ilçesi, Ekin ve Başak mahalleleri; Altındağ ilçesi, Battalgazi ve Beşikkaya mahalleleri sınırları içerisinde bulunan isimsiz köprülü kavşağın adının "Reşat Çiğiltepe Alt Geçidi" olarak isimlendirilmesine oy birliği ile karar verilmiştir.

Kaynakça

1879 doğumlular
1922 yılında ölenler
Türk albaylar
Osmanlı savaş tutsakları
I. Dünya Savaşı'nda savaş tutsakları
Balkan Savaşları'nda Osmanlı askerleri
I. Dünya Savaşı'nda Osmanlı askerleri
Kurtuluş Savaşı'ndaki Türk askerler
Kırmızı şeritli İstiklâl Madalyası sahipleri
İntihar eden askerler
İstanbul doğumlu askerler
20. yüzyılda Osmanlılar
Devlet Mezarlığı'na defnedilenler
Afyonkarahisar'da ölenler
Mekteb-i Harbiye'de öğrenim görenler
Kurtuluş Savaşı'nda ölenler
Piyade subaylar

Reşat (Çiğiltepe)


Molly of Denali este un serial de televiziune animat americano-canadian creat și produs de Atomic Cartoons și WGBH Kids pentru PBS Kids și CBC Television. A avut premiera pe 15 iulie 2019.

Episoade

Radiodifuziune
 PBS Kids (2019-prezent)
 CBC Kids (2019-prezent)

Distribuție
 Sovereign Bill ca Molly Mabray
 Sequoia Janvier ca Tooey Ookami
 Vienna Leacock ca Trini Mumford
 Jules Koostachin ca Layla Mabray
 Ronnie Dean Harris ca Walter Mabray
 Lorne Cardinal ca Grandpa Nat
 Adeline Potts ca Auntie Midge
 Ellen Kennedy ca Singing Moose și Video Voice
 Luc Roderique ca Daniel și Announcer
 Michelle Thrush ca Shyahtsoo
 Shaun Youngchief ca Mr. Patak

Referințe

Seriale de televiziune americane
Seriale canadiene
Seriale de televiziune din 2019

Molly of Denali


Olaylar
 Koguryo-Tang Savaşları başladı (bitişi 668).

Doğumlar
 İmparatoriçe Jitō, Japonya'nın geleneksel veraset düzenine göre 41. hükümdarı (ö. 703)
 Mücâhid bin Cebr, ünlü hadis ve tefsir bilgini (ö. 723)

Ölümler
 21 Ekim - Yinçü Bilge Kağan, Orta Asya bozkırlarının kuzeyinde hüküm süren bir Sir-Tartuş kağanı
 tarihi bilinmeyen
 El-Hansa, Arap şair (d. 575)

645


De Otte var et dansk skuespillerensemble, som i 1905 brød ud af Dagmarteatret med planer om at etablere deres eget teater i Grønnegade i København (den nuværende bygning på adressen Gammel Mønt 4 er baseret på Johan Nielsens oprindelige arkitekttegninger til det forliste skuespilhus). De turnerede i Norge og Sverige i sæsonen 1905-06 med blandt andet opførelser af Kameliadamen og Alexander den Store. Truppen opløstes i juni 1906, efter at justitsminister P.A. Alberti i februar 1906 afviste deres ansøgning om en teaterbevilling.

Oprindelige medlemmer
 Jacob Jacobsen (kunstnerisk leder)
 William Norrie (økonomichef)
 Anna Larssen Bjørner (dengang Anna Larssen)
 Emmanuel Larsen
 Olivia Norrie (dengang Olivia Jacobsen)
 Johannes Poulsen
 Albrecht Schmidt
 Emma Wiehe
 Jacques Wiehe

Senere tilknyttede turnédeltagere
 Marie Dinesen
 Robert Dinesen
 Peter Fjelstrup
 Knud Lumbye
 Marie Niedermann
 Asta Nielsen
 Mimi Gade (dengang Mimi Mikkelsen)
 Robert Schmidt
 Valdemar Willumsen

Referencer

Eksterne henvisninger
 Peter Elfelts filmoptagelse af De Otte i Christiania (Oslo) 1905 på DR Bonanza

Teaterskuespillere fra Danmark
Grupper

De Otte (teatertrup)


Doğu Cephesi, Türk Kurtuluş Savaşı sırasında 1919-1921 yılları arasında Türk-Ermeni Savaşı (24 Eylül-2 Aralık 1920) dahil olmak üzere, Doğu Anadolu ve Güney Kafkasya'da gerçekleşen muharebelerden meydana gelen cephe.

Tarihçesi

I. Dünya Savaşı'nda, Kafkas Cephesi'nin açılması üzerine Ermeniler'le Ruslar işbirliğine yönelmişler ve Rusların kışkırtmalarıyla Osmanlılara saldırmaya başlamışlardır. 1917 yılında Rusya'da ihtilal gerçekleşince Ruslar, Doğu Anadolu Bölgesi'nde işgal ettikleri yerleri Türklere bırakarak geri çekildiler. Bu arada merkezi Erivan olan bir Ermeni devleti kuruldu (28 Mayıs 1918). Ruslar çekilirken daha Türk ordusu bölgeye ulaşmadan Ermeniler, Rusların yerini aldı ve Doğu Anadolu'nun kendilerine ait olduğunu ileri sürüp, Gümrü, Iğdır, Arpaçay ve Aras'a kadar ilerlediler. Azerbaycan petrollerine göz koyan Almanya, 1918'de Gürcistan'a asker çıkartırken Enver Paşa kumandasındaki 3. Ordu Kafkasya boyunca ilerledi ve Bakü Muharebesi (1918) sonrası Azerbaycan'ı Rus ve İngiliz boyunduruğundan kurtardı. Böylece Türkiye garantörlüğünde Azerbaycan bağımsızlığını kazandı.

I. Dünya Savaşı'nın sona ermesi ve bölgede bulunan Türk 3. Ordusu'nun 30 Ekim 1918 Mondros Mütarekesi gereğince Kafkasya'yı boşaltması sonucu Kafkaslar'da, Ermenistan başta olmak üzere Gürcistan, Azerbaycan ve Nahçıvan Cumhuriyetleri kuruldu.

Bu boşaltma sırasında muhtemel Ermeni saldırı ve tecavüzlerine karşı da Türk halkını korumak maksadıyla Ardahan, Batum bölgesinde Acara Şura Hükûmeti, Kars-Oltu-Sarıkamış-Kağızman bölgelerinde ise Güneybatı Kafkas Geçici Milli Hükûmeti kuruldu. Ancak bu iki hükûmet 3 ay sonra İngilizler tarafından dağıtıldı. Bu olaydan sonra bölgenin Ermeni saldırılarına karşı savunulması, karargâhı Erzurum'da bulunan 15. Kolordu tarafından sağlandı.

I. Dünya Savaşı sonrası itilaf ülkelerinin Bolşevik Rusya ve Türkiye'yi çevrelemek  amacıyla yürüttüğü askeri operasyonlar iki ülke arasında yakınlaşmaya neden oldu. Mustafa Kemal Paşa, Samsun'a çıktıktan sonra geçtiği Havza'da 22 gün kaldı ve burada Lenin, Stalin ve Troçki'nin en güvenilir adamlarından Rus albay Semyon Mihayloviç Budyonni ile görüştü. Rus albay, yardım yapmaya hazır olduklarını ancak saltanat ve hilafetin kaldırılıp komünizmin ilan edilmesini istedi. Mustafa Kemal Paşa ise tek amaçlarının savaşı kazanmak olduğunu, diğer şartların ancak zaferin kazanılmasından sonra düşünülebiceğini söyledi. Sivas Kongresi sonrasında da Halil Kut Paşa, Mustafa Kemal tarafından Moskova'ya gönderildi. Amaç Sovyetlerle ilişkileri geliştirmek, silah, cephane ve para yardımı sağlamaktı. 27 Aralık 1919'da Bolşevikler ve Kemalistler Samsun'da gizli bir antlaşma imzaladılar. Bu anlaşmaya göre, Rus tarafı, Sevr Antlaşması'nın sonuçlanmasına kadar, Türkiye'nin mevcut sınırlarının önceliğini kabul etmiş ve toprak bütünlüğünü koruma yükümlülüklerini üstlenmiştir. TBMM'nin kurulmasından üç gün sonra 26 Nisan'da Mustafa Kemal Paşa Rus lideri Lenin'e bir mektup gönderdi.

Bu öneri tamamen Rusya'nın çıkarına idi, çünkü Rusya ve Türkiye'ye düşman devletler, Kırım ve Güney Kafkasya'nın yanı sıra Rus deniz ticaretinin çoğunun gerçekleştirildiği İstanbul ve Karadeniz boğazlarına hakim durumdaydılar. Ayrıca 1917 Ekim Devrimi sonrası Rus İç Savaşı ve Beyaz Terör olayları ile yoğun bir iç çatışmaya giden Rusya'da bir yandan milyonlarca insan açlıktan ölüyordu, diğer taraftan 1920'de  Sovyet-Polonya Savaşı nedeniyle de epey zor durumdaydılar. Azerbaycan Cumhuriyeti'nin kaderi, Sovyetlerin, Polonya ile yeni savaşta özellikle değerini keskin bir şekilde gösteren Bakü petrolünün arzına kritik derecede bağımlıydı. Mektubun gönderilmesinden iki gün sonra Sovyet askerleri Azerbaycan'ı ele geçirdi ve 28 Nisan'da Azerbaycan Demokratik Cumhuriyeti yıkıldı ve Azerbaycan Sovyetleştirildi.

Sonra Sovyet Rusya ile görüşmelerde bulunmak üzere Bekir Sami Bey ve Yusuf Kemal Tengirşenk'in bulunduğu bir heyet 11 Mayıs 1920'de Ankara'dan ayrıldı ve 19 Temmuz'da 1920'de Moskova'ya varıp Lenin de dâhil önemli Sovyet yetkilileriyle görüştü. 24 Ağustos'ta taslak bir anlaşma hazırlandı. Bu, Moskova'daki ilk Rus-Türk konferansı idi.

Ermeniler bu yakınlaşmadan rahatsız oldular. Kafkasya'daki bir Sovyet hakimiyetinden endişeliydiler. Bir kısım birlikleri Sovyet hattında, bir kısım birlikleri ise Türkiye hattında bölünmüş durumdaydı. Bu sırada Kazım Karabekir Paşa ani bir harekât düzenledi ve bu savaşta Taşnak Ermenistanı yenildi. Daha sonra Sovyet birlikleri Ermenistan'a girdi ve Ruslar tarafından 28 Kasım 1920'de Ermenistan Sovyetleştirildi. 2 Aralık'ta iktidardan çekilen Taşnak hükûmeti, Gümrü Antlaşması'nı imzalamak zorunda kaldı.Sonra Türk ve Rus orduları ortak harekât ile Gürcistan'a ilerlemişlerdir.Müteâkiben Türkiye ve Sovyet Rusya arasında bir ittifaknâme imzalanması kararlaştırıldı. 9 Aralık 1920 tarihinde Çiçerin gönderdiği bir Sovyet notası ile Moskova'da Türkiye, Rusya, Azerbaycan ve Ermenistan'ın katılacağı bir konferansın yapılma isteği belirtildi. İktisat vekili Yusuf Kemal Tengirşenk ve Maarif vekili Dr. Rıza Nur riyasetindeki heyete daha önce Moskova büyükelçiliğine atanan Ali Fuat Cebesoy da Kars'ta katılmıştı.  29 Ocak 1921'de Bakü'ye gelen ve burada Neriman Nerimanov ile görüşen heyet buradan hareketle 6 Şubat 1921'de Moskova'ya ulaşmıştır. Heyet 26 Şubat'ta Lenin ile görüşmüş ve 27 Şubat'ta Türk-Rus konferansı başlamıştır. Rusya için hayati değerdeki Bakü petrollerinin sevkiyatını Ruslar Batum üzerinden yapmaktaydı. Türk heyeti 6 Mart'ta Stalin ile görüştükten sonra Ruslar Batum kendilerine devredilmek şartıyla 10 Mart 1921 günü Mîsâk-ı Millî'yi tanımış ve Kars ile Ardahan'ı Türkiye'ye bırakmışlardır.

Burada Georgi Çiçerin Nahcivan'ın Ermenistan'a verilmesini istemişse de Türk delegeler Yusuf Kemal ve Dr. Rıza Nur bunu reddetmişler ve Azerbaycan'a bağlanmasını sağlamışlardır.  "Nahçıvan, Azerbaycan'ın bu himayesini başka bir devlete devretmemesi koşuluyla, Azerbaycan'ın himayesi altında özerk bir bölge olarak tanınacaktır." Ek bilgi olarak, 1930 Ağrı isyanı sonrası İran ile 23 Ocak 1932 tarihinde sınır antlaşması imzalanmıştır. Yapılan toprak mübadelesi sonucu, isyancıların bulunduğu arazi olan "Boralan Gölü'ne kadar Karasu Çayı talvegini takip ettikten sonra Küçük Ağrı Dağı" Türkiye'ye bırakılmış, yani Dilucu bölgesi ve Küçük Ağrı Dağı alınarak Türkiye-Nahcivan karasınırı oluşmuştur. Karşılığında Ovacık, Kotur ve Salmas bölgesinin bir kısmı İran'a bırakılmıştır.

14 Mart 1921'de son şekli verilen Moskova Antlaşması Rus yetkililerin teklifi üzerine İstanbul'un işgali tarihi olan 16 Mart 1920'nin yıl dönümünde 16 Mart 1921'de imzalanmış ve Doğu cephesi kapanmıştır. Sovyet resmi verilerine göre 39 bin tüfek, 327 makineli tüfek, 54 silah, 63 milyon fişek, 147 bin mermi Anadolu'ya gönderilmiştir. Rusların gönderdiği mühimmatlar Sakarya ve Büyük Taarruz muharebelerinde kullanılmıştır. Ayrıca Lenin, en yetenekli Sovyet askeri liderlerinden Mihail Vasilyeviç Frunze'yi ve Kliment Efremoviç Voroşilov'u askeri danışman olarak 1921'de Ankara'ya göndermiştir.

1920 yılında kurulan Buhara Cumhuriyeti de, millî mücadeleye destek olmak için Rusya vasıtasıyla 100 milyon altın ruble gönderdiği halde, bunun ancak 17.5 milyonu anadoluya ulaşmış, Türkiye'ye gönderilmesi gereken diğer 82.5 milyon altın tutarındaki özbek altını Lenin hükûmeti tarafından gaspedilmiştir.

Doğu Cephesi savaş düzeni

Bu cephede bulunan Türk 15. Kolordusu dört tümen ile süvari ve topçu alaylarından oluşmaktaydı. Muharip personel sayısı, 15.000 ile 20.000 kişi arasında idi. Ermeniler ise toplam 12 alaydan oluşan dört tümene sahiptiler. Ermeni kaynaklarına göre askerî  personel mevcutları 20.000 kadar idi. Milislerle beraber muharip personel sayısı 50.000'e kadar çıkıyordu.

Cephe hattı Osmanlı-Rus Savaşı (1877-78) sonrasındaki Osmanlı-Rus sınırını olan Ardeşen-Yusufeli-Oltu-Bayezit olarak belirlenmişti.

TBMM Hükûmeti ile Ermenistan Demokratik Cumhuriyeti arasındaki savaş

Türk Kurtuluş Savaşı başlamadan önce Doğu Anadolu Bölgesi'nin Ermenilerin eline geçmesine mani olmak için Doğu Anadolu Müdafaa-i Hukuk Cemiyeti adıyla bir örgüt kurulmuştu. Bu kuvvetler Ermenilerle Oltuda çatışma haline girmişlerdi.

TBMM Hükümeti artan Ermeni sorunlarına ve yayılmacılığına son vermek amacıyla 20 Eylül 1920'de bölgede bir askerî harekât yapılmasına karar verdi. 15. Kolordu Komutanı Musa Kâzım Karabekir'i tam yetkiyle Doğu Cephesi Komutanlığına atadı. Bu sırada Rus orduları Azerbaycan'a girmişlerdi. Ermeni orduları Türk ve Rus kuvvetleri karşısında iki ayrı cephede bölünmüş durumdaydılar.

28 Eylül 1920'de saldırıya geçen Kâzım Karabekir kuvvetleri, birkaç gün içerisinde Ardeşen-Yusufeli-Oltu-Bayezit hattını aşarak Drastamat Kanayan komutasında Ermeni kuvvetleriyle çatışmaya girdi. İlk cephe Oltu Muharebesi oldu. Daha sonra Simon Vratsiyan ve Artaşes Babalyan komutasında olan Ermeni güçleriyle Sarıkamış Muharebesi (1920) ve Kars Muharebesi yapıldı. 30 Ekim 1920'de Kars'tan çıkarılan ve Kars'ın doğusuna çekilen Ermeniler Bolşevik Rusya'dan ve ABD'den yardım istedi. Bolşevik Rusya bu Kafkasya'yı kendi nüfuz alanı olarak gördüğünden dolayı ve Türk Kurtuluş Savaşı'nı desteklediği için yardım etmeyi reddetti. ABD'den de olumlu yanıt alamayan Ermeniler, işgal ettikleri Erzurum, Kars ve çevresini Kâzım Karabekir kuvvetlerine bıraktı ve bugünkü Ermenistan'ın batısına çekildi. Ancak henüz barış antlaşması imzalanmamıştı. Kasım 1920'de Karakoyunlu'daki Yarmalar geçidini aldıktan sonra Iğdır'ı da Anadolu'ya dahil eden Kâzım Karabekir'in kuvvetleri Ermeni birliklerini daha ileri giderek Gümrü'ye kadar takip etti. Burada Gümrü Muharebesi yapıldı. 7 Kasım 1920'de Türk ordusunun Gümrü'ye girmesi üzerine yenilen Ermeniler barış istedi.

Gümrü Antlaşması

Barış isteğini kabul eden TBMM Hükümeti 2 Aralık 1920'de Ermenistan'la Gümrü Antlaşması'nı imzaladı. Antlaşmaya göre Batum, Sarıkamış, Kars, Ağrı, Erzurum, Artvin, Oltu ve çevresi TBMM Hükümeti bırakılırken savaş esnasında Kâzım Karabekir kuvvetlerinin eline geçen Gümrü kenti ise Ermenistan'a bırakıldı. Ayrıca, Mondros sonrasında Ermenistan'a bırakılan Tuzluca (Kulp) kazası da TBMM Hükûmeti kontrolüne kaldı. Gümrü Antlaşması'na göre:

 Sevr Antlaşması'nın geçersiz olduğu Ermenilerce de benimsendi.
 Ermeniler Doğu Anadolu Bölgesi'ndeki tüm isteklerinden vazgeçti. Büyük Ermenistan kurma girişimleri sona erdi.
 1878'de elden çıkan Kars ve çevresi Türkiye'nin topraklarına katıldı.
 Gümrü Antlaşması TBMM'nin uluslararası alanda ilk siyasi başarısıdır.
 Misak-ı Milli'nin doğu sınırları kısmen de olsa belirlendi.
 Halk üzerinde ordu ve meclisin güveni arttı.
4 Aralık 1920'de Kızıl Ordu Erivan'a girdi ve Azerbaycan'dan sonra Ermenistan da sovyetleştirildi.

TBMM Ordusu'nun Gürcistan Seferi

General Hüseyin Yalabık yönetmiştir.

Türk ve Rus kuvvetleri Gürcistan'a ilerlediler ve Gürcistan da sovyetleştirildi.

Kaynakça

Kâzım Karabekir (2016). İstiklal Harbimiz, Yapı Kredi Yayınları, İstanbul. ISBN 9789750813467

Doğu

Türk Kurtuluş Savaşı Doğu Cephesi


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Nicky Hayden, punim imenom Nicholas Patrick Hayden (Owensboro, okrug Daviess, Kentucky, SAD, 30. srpnja 1981.  - Cesena, pokrajina Forlì-Cesena, Emilia-Romagna, Italija, 22. svibnja 2017.), nadimka "The Kentucky Kid" je bio američki vozač motociklističkih utrka.

 Životopis i karijera
Nicky Hayden je rođen 1981. godine u Owensboru u američkoj saveznoj državi Kentucky. Njegov otac Earl i majka Rose su se bavili motociklizmom, te su se tako Nicky i njegovih četvero braće i sestara počeli baviti motociklizmom u ranoj dobi. Nicky je prvu utrku imao sa samo četiri godine - na minibikeu u "dirt track" utrci, te se tako narednih godina, skupa sa svojom braćom natjecao u "dirt track" utrkama u organizacijama WKCRA i CMRA, a od 1989. i u AMA Amateur National Dirt Track. Nicky i braća su vozila za obiteljski trkači tim - "Earl's Racing". Uz "dirt track" utrke (na zemljanim stazama), od 1990. godine je Nicky počeo i voziti minibike utrke na asfaltnim stazama ("flat track"). Prvo iskustvo s trkaćim motociklom (klase 125cc) je imao 1992. godine. Do 1996. godine se Nicky uglavnom natjecao u AMA Amateur National Dirt Track te u organizaciji WERA.  1997. godine je napunio 16 godina, te je po pravilima mogao postati profesionalna vozač i natjecati se u cestovnom motociklu. On i brat Tommy su potpisali profesionalni ugovor s timom "Muzzy Racing". Nicky je zakupio motocikl proizvođača Kawasaki te je nastupio u nekoliko utrka AMA 600 Supersport i AMA 750 Supersport prvenstva. Također je te godine osvojio nagradu AMA Dirt Track Horizon Award.
1998. godine je prešao u momčad "Hypercycle Suzuki" (na Suzuki motociklima), te je vozio kompletno prvenstva AMA 600 Supersport i AMA 750 Supersport (u oba je završio četvrtoplasirani), te u AMA Formula Xtreme - u sve tri kategorije je osvojio pobjedu u toj sezoni. 1998. godine je također prvi put nastupio na utrci za svjetsko prvenstvo - u Supersport svjetskoj seriji na utrci na stazi Laguna Seca, ali nije završio utrku.
1999. godine je prešao u tim "Erion Honda", regularno nastupavši u prvenstvima AMA 600 Supersport (postao prvak) i AMA Formula Xtreme (osvojio drugo mjesto), te je kao zamjenaski vozač debitirao u AMA Superbike prvenstvu. Također se natjecao u AMA Grand National Championship u flat track utrkama (vozio Harley-Davidson). 2000. godine je prešao u momčad "American Honda" te je u AMA Superbike prvenstvu osvojio drugo mjesto, a 2001. treće mjesto.
2002. godine je Nicky Hayden osvojio AMA Superbike prvenstvo, kao najmlađi prvak dotada, te je početkom sezone osvojio i poznatu utrku "Daytona 200". Te je sezone također nastupio prvi put na utrci Superbike svjetskog prvenstva.
2003. godine Hayden je prešao u MotoGP svjetsko prvenstvo u momčad "Repsol Honda Team" (motocikl Honda RC211V) kao momčadski kolega svjetskom prvaku Valentinu Rossiju, osvojivši na kraju sezone peto mjesto, a najbolji rezultat su bila dva treća mjesta. U sezoni 2004. je osvojio osmo mjesto uz dva postolja, a timski kolega je bio Brazilac Alex Barros. Prvu pobjedu u MotoGP svjetskom prvenstvu je osvojio 2005. godine - "VN SAD-a" na stazi Laguna Seca. U ovoj sezoni je ukupno bio trećeplasirani u prvenstvu, uz ukupno šest postolja. Timski kolega u sezoni 2005. je bio Talijan Max Biaggi. U sezoni 2006. Nicky Hayden je dobio četvrtog timskog kolegu u "Repsol Hondi" u četiri sezone - Danija Pedrosu iz Španjolske. U sezoni u kojoj je sedam vozača osvojilo pobjede u MotoGP klasi, a pet vozača je bilo u stalnoj borbi za naslov - Nicky Hayden je osvojio naslov s 5 bodova prednosti ispred Valentina Rossija (ukupno 252). Osvojio je dvije utrke, te je na 10 utrka ukupno bio na postolju. 2007. godine su u MotoGP klasi umjesto dotadašnjih motocikala od 990cc uvedeni motocikli od 800cc, što nije odgovaralao Haydenovom vozačkom stilu. U te dvije sezone je osvojio 8. i 6. mjesto u prvenstvu, uz osvojenih pet postolja te više nikad nije ostvario pobjedu u MotoGP prvenstvu. 2009. godine prelazi u "Ducati Marlboro Team" - tvorničku momčad Ducatija (kasnije kao i "Ducati Team", odnosno "Ducati Corse"), za koji vozi do kraja sezone 2013., odvozivši 86 utrka na kojima se tri puta plasirao na pobjedničko postolje. Najboli plasman na kraju sezone u Ducatiju je imao 2010. godine - 7. mjesto. Timske kolege u "Ducati Teamu" su mu bili Australac Casey Stoner (2009. i 2010.), Valentino Rossi (2011. i 2012.) te Andrea Dovizioso (2013.)
2014. godine je prešao u "Aspar team", koji je koristio Hondine motocikle u tzv. "Open" podklasi - Honda RCV1000R (2014.) i Honda RC213V-RS (2015.).  2016. godine je Nicky Hayden prešao u Superbike svjetsko prvenstvo za Honda World Superbike Team (motocikl Honda CBR1000RR). Na kraju prvenstva je bio petoplasirani s 248 pobjeda, osvojivši jednu pobjedu (u Maleziji), te je četiri puta bio na pobjedničkom postolju. Također je 2016. na dvije utrke MotoGP svjetskog prvenstva nastupio kao zamjenski ("wild card") vozač na motociklu Honda RC213V'').
Pripremajući se za nastavak sezone, 17. svibnja 2017. dok je vozio bicikl blizu grada Rimini u Italiji, na njega je naletio osobni automobil. S teškim ozljedama glave i prsnog koša je prevezen u bolnicu u Cesenu, gdje je operiran i stavljen u induciranu komu.
Od posljedica teških ozljeda je preminuo 22. svibnja 2017. u 35. godini života.

Nickyeva braća Tommy (r. 1978.) i Roger Lee (r. 1983.) su također uspješni motociklisti, te su se pretežno natjecali u prvenstvima organizacije AMA.

Uspjesi u prvenstvima
 Svjetsko prvenstvo - MotoGP
 prvak: 2006.
 trećeplasirani: 2005.

 AMA - Superbike
 prvak: 2002.
 doprvak: 2000.
 trećeplasirani: 2001.

 AMA - 600 Supersport
 prvak: 1999.

 AMA - Formula Xtreme
 doprvak: 1999.

Osvojene utrke
 Osvojene utrke u natjecanjima sa statusom svjetskog prvenstva

 Ostale pobjede

Pregled karijere

Po sezonama - cestovni moticiklizam

Unutarnje poveznice

Vanjske poveznice
  nickyhayden.com
  motorsportmagazine.com, Nicky Hayden
  motogp.com, Nicky Hayden
  worldsbk.com, Nicky Hayden

Izvori

  nickyhayden.com, Biography - Nicky Hayden's life and career, pristupljeno 26. veljače 2021.
  nickyhayden.com, Accomplishments - Nicky Hayden's awards and numbers, pristupljeno 26. veljače 2021.
  nickyhayden.com, Timeline - Nicky Hayden through the years, pristupljeno 26. veljače 2021.
  nickyhayden.com, Facts, pristupljeno 26. veljače 2021.
  motorcyclemuseum.org, Nicky Hayden, pristupljeno 26. veljače 2021.
  pilotegpmoto.com, HAYDEN Nicky, preuzeto 2. ožujka 2021.
  motorsport-archive.com, Nicky Hayden, pristupljeno 5. ožujka 2021.
  the-sports.org, Nicky Hayden, pristupljeno 5. ožujka 2021.
  motorrad-autogrammkarten.de, Nicky Hayden, wayback arhiva
  crash.net, Nicky Hayden, pristupljeno 1. ožujka 2021.
  motorrad-autogrammkarten.de, AMA Pro Road Racing , pristupljeno 26. veljače 2021.
  racingmemo.free.fr, Les Champions Américains, pristupljeno 26. veljače 2021.

Američki športski motociklisti

Nicky Hayden


William Edward Fichtner (d. 27 Kasım 1956; Long Island, New York) Alman asıllı Amerikalı aktör.

Filmografi

Kaynakça

Dış Bağlantılar

1956 doğumlular
Nassau County, New York doğumlular
Amerikalı erkek dizi oyuncuları
Amerikalı erkek sinema oyuncuları
Ekran Oyuncuları Derneği Ödülü sahipleri
Yaşayan insanlar
21. yüzyılda Amerikalı erkek oyuncular

William Fichtner


ජනමත විමසුමක් (හෝ ජනමත විචාරණයක් හෝ ජනමත විචාරයක්) යනු යම් යෝජනාවක් සඳහා මැතිවරණ කොට්ඨාසයක සිටින සියලු ම චන්ද දායකයින් හට ඡන්දය ප්‍රකාශ කළ හැකි ඍජු ඡන්දයකි. මෙයක ප්‍රතිඵලයක් ලෙස නව නීතියක් සම්මත කර ගැනීම සිදු විය හැකි ය.

පරණතම භාවිතය
ජනමත විමසුමක් එම තේරුමින් ම භාවිතයට ගැනීම පළමුවෙන් ම සිදු කෙරුණේ 16වැනි සියවසේ ග්‍රෞබ්‍යූන්ඩන් (Graubünden) නම් ස්විස් කැන්ටනයේ ය.

තාර්කිකත්වය
දේශපාලන-දාර්ශනික දෘෂ්ටි කෝණයකින් බැලූ විට, ජනමත විචාරණ යනු ඍජු ප්‍රජාතන්ත්‍රවාදයේ උසුරුවකි. නමුත් නූතන ලොවෙහි ජනමත විමසුම් නියෝජනාත්මක ප්‍රජාතන්ත්‍රවාදයෙහි ලා ද වටහාගත යුතු ය. එනිසා,  මෙම විමසුම් ඉතා ම වරණීය ලෙස දැනට පත් ව ඇති නිලධරයන් හට නීත්‍යානුකූල අවසරයක් හෝ රිසියක් නැති ඡන්ද පද්ධති වෙනස් කිරීම වැනි ගැටලු වලට විසඳුම් සොයා ගැනීමට භාවිතා කරයි.

රටවල් අනුව ජනමත විමසුම
18වැනි සියවස අවසානයේ සිට ලොව පුරා සිය ගණන් ජාතික ජනමත විචාරණ සංවිධානය කොට තිබුණි; ස්විට්සර්ලන්තය 1848 හි දී නූතන රාජ්‍යයක් වීමෙන් අනතුරු ව ජාතික ඡන්ද 600 කට ආසන්න ප්‍රමාණයක් පවත්වා ඇත. ඉතාලිය ජාතික ජනමත විමසුම් 72ක් සමඟ දෙවන ස්ථානයේ සිටියි: ජනප්‍රිය ජනමත විමසුම් 67ක්, ව්‍යවස්ථාමය ජනමත විමසුම් 3ක්, සංස්ථායික ජනමත විමසුම් එකක් හා එක උපදේශාත්මක ජනමත විමසුමක් වශයෙනි.

බහුවරණ ජනමත විමසුම්

ව්වේචන

මූලාශ්‍ර

 The Federal Authorities of the Swiss Confederation, statistics (German). http://www.bfs.admin.ch/bfs/portal/de/index/themen/17/03/blank/key/stimmbeteiligung.html

යොමු

ඉදිරියට කියවන්න

 Morel, L. (2011). 'Referenda'. In: B. Badie,  D.  Berg-Schlosser,  &  L.  Morlino(eds), International  Encyclopedia  of  Political Science.Thousand Oaks: SAGE: 2226-2230.

 Setälä, M. (1999). Referendums and democratic government. London and New York: Palgrave Macmillan.

ජනමත විමසුම


شعارة أو شعارة اللجاة

تقع قرية شعارة شمال شرق مدينة درعا وتبعد عنها بحوالي 70 كم و جنوب شرق العاصمة دمشق بحوالي 30 كم. وتتبع لمنطقة المسمية التي تبعد عنها إلى الجنوب الغربي ب 5 كم على زاوية اللجاة الشمالية الغربية.
يصلها جسر جباب يربطها بالأستراد (الطريق السريع) ويمكن من الوصول إليها للقادمون من دمشق أو درعا وأيضا هناك طريق السويداء - دمشق يصلها بمحافظة السويداء و مدينتها.

معالم القرية الأثرية
يضم موقع شعارة مدينة أثرية هامة، محفوظة بشكل جيد إلى الجنوب والجنوب الغربي وشرق هذه المدينة أربعة معابد تبعد عن المدينة الأثرية بين 2 كم حتى 700 متر. وقد تم إعطاء اسم المعبد الأول والثاني والثالث والرابع للمعابد المذكورة والمحددة وفق مخطط المدينة.

اسمها القديم غير معروف حتى اليوم وتحتوي على الكثير من الآثار والمخلفات الأثرية البالغة الأهمية منها الجامع القديم والحمامات والبرج العالي وبقايا لمنحوتات أثرية. تعمل فيها بعثة فرنسية منذ عدة سنوات.

الفخار المكتشف فيها يعود للعصور التاريخية المختلفة وأغلبه الكلاسيكي والإسلامي. وفيها كهوف ومغارات منحوتة في الصخر استخدمت كمقابر ومدافن لعائلات المدينة.

تشكل مدينة شعارة لوحة فنية من البازلت لكثرة أبنيتها وتوزعها بشكل منتظم وهي خالية من البيوت البيتونية الحديثة التي تم بناءها بعيدًا في الجهة الغربية لكي تبقى المنطقة محافظة عى طابعها الأثري القديم.

المصادر
 موقع درعا

مراجع وهوامش

قرى محافظة درعا

شعارة


Çetin Güngör (* 7. Juni 1990 in Istanbul) ist ein türkischer Fußballspieler, der für Altay Izmir spielt.

Karriere

Galatasaray
Çetin Güngör begann mit dem Vereinsfußball in der Jugend seines Heimatvereins Beşyüzevler Spor. Dort wurde er von den Scouts von Galatasaray Istanbul entdeckt, und so wechselte er 2005 in die Jugendabteilung von Galatasaray. 2009 erhielt er von seinem Verein einen Profi-Vertrag, spielte aber vorerst überwiegend für die zweite Mannschaft. Im Laufe der Saison bekam er die Möglichkeit auch bei der Profi-Mannschaft mitzutrainieren. In einigen Profi-Spielen wurde er sogar als Reservespieler in den Mannschaftskader übernommen. So kam er bis zum Saisonende auf einen UEFA-Europa-League-Einsatz und zwei Pokal-Einsätze für das Profi-Team.

Şanlıurfaspor
In der neuen Saison 2010/11 wurde er bereits zu Saisonbeginn an den Drittligisten Şanlıurfaspor ausgeliehen. Dort wurde er auf Anhieb Stammspieler und machte bis zum Saisonende 22 Spiele.

Gaziantepspor
Zum Ende der Saison lief sein Vertrag mit Galatasaray aus, daraufhin wechselte Güngör ablösefrei zum Erstligisten Gaziantepspor. Hier kam er lediglich zu neun Einsätzen für das Profi-Team und spielt eher für die Reservemannschaft.

Çaykur Rizespor
Zum Ende der Saison lief sein Vertrag mit Gaziantepspor aus, daraufhin wechselte Güngör ablösefrei zum neuen Zweitligisten Adana Demirspor.

Dieser Wechsel zu Adana Demirspor kam später doch nicht zustande und so wechselte Güngör zum Zweitligisten Çaykur Rizespor. In der Saison 2012/13 wurde er mit dem Verein Vizemeister und stieg somit in die Süper Lig auf.

Adanaspor
Zur neuen Saison wechselte er innerhalb der 1. Lig zu Adanaspor. Kurz vor Saisonbeginn wurde der Vertrag aufgelöst.

Altay Izmir
Zur Saison 2013/14 heuerte er beim Drittligisten Altay Izmir an.

Nationalmannschaft
Çetin Güngör durchlief über die Jahre türkische U-18, U-19 und die U-20 Juniorennationalmannschaften. 2009 nahm er mit der türkischen U-19 an der U-19-Fußball-Europameisterschaft 2009 teil. Hier schied man bereits in der Gruppenphase aus dem Turnier aus.

Erfolge
 Mit Gaziantepspor
 Spor Toto Pokal (1): 2012

 Mit Çaykur Rizespor
 Vizemeister der TFF 1. Lig 2012/13 und Aufstieg in die Süper Lig

Weblinks

Einzelnachweise

Fußballspieler (Adanaspor)
Fußballspieler (Altay Izmir)
Fußballspieler (Çaykur Rizespor)
Fußballspieler (Eyüpspor)
Fußballspieler (Galatasaray Istanbul)
Fußballspieler (Gaziantepspor)
Fußballspieler (Gaziosmanpaşaspor)
Fußballspieler (Şanlıurfaspor)
Türke
Geboren 1990
Mann

Çetin Güngör (Fußballspieler)


Frank V. Phillips (* 7. April 1912 in San Bernardino, Kalifornien; † 10. April 1994 in Prescott, Arizona) war ein US-amerikanischer Kameramann.

Leben und Wirken
Der gebürtige Kalifornier war im Jahre 1931 als Laufbursche zu Metro-Goldwyn-Mayer gestoßen. Wenig später entschied er sich für eine Karriere als Football-Spieler und ging an die University of Notre Dame in South Bend, Indiana. Nach dem frühen Tod (Flugzeugabsturz) des dort als Trainer arbeitenden Footballstars Knute Rockne kehrte Phillips nach Hollywood zurück.

Er begann dort anfänglich als Filmeinleger und wirkte als rechte Hand des Regisseurs Irving Reis. Sein Handwerk als Kameramann erlernte Phillips als Assistent der erfahrenen Kameraleute Harry Stradling Sr. und George J. Folsey. Deren Kollege Robert Surtees verpflichtete Frank Phillips 1950 und gab ihm bei dem Abenteuerfilm König Salomons Diamanten erstmals die Gelegenheit, als einfacher Kameramann zu arbeiten. In dieser Funktion war Phillips anschließend auch an Filmklassikern wie Du sollst mein Glücksstern sein und Giganten beteiligt. Für die Twentieth Century Fox wurde Frank Phillips 1954 erstmals als Chefkameramann eingesetzt: man ließ ihn bei einer Second-Unit-Einheit die in Monte Carlo entstandenen Sequenzen des Rennfahrerfilms Der Favorit alleinverantwortlich ins Bild setzen.

1956 wechselte Frank Phillips zum Fernsehen, für das er in der Folgezeit Hunderte einzelner Folgen populärer Serien wie Navy Log, Hotel de Paree, Have Gun – Will Travel, Maverick, Colt .45, Perry Mason und Adventure in Paradise fotografieren sollte. Als Phillips 1963 vorübergehend das Fernsehen verließ, war er gerade mit der überaus beliebten Westernserie Rauchende Colts beschäftigt. Mit der Krimiserie Hawaii Fünf-Null beendete er seine Tätigkeit für das Serienfernsehen endgültig.

Phillips eigentlicher Karrieredurchbruch begann erst in der zweiten Hälfte der 60er Jahre, als er der Hauskameramann für eine Reihe von familiengerechten Unterhaltungsfilmen der Walt Disney Company wurde. Ein beträchtlicher Teil dieser Produktionen waren in den 70er Jahren beachtliche Kinoerfolge. Für seine Arbeit an dem aufwendigen Science-Fiction-Streifen Das schwarze Loch wurde Frank Phillips 1980 für den Oscar nominiert. Im Alter von 70 Jahren zog sich Phillips ins Privatleben zurück.

Filmografie
Filme als Chefkameramann

 1961: Rider on a Dead Horse
 1965: Wild Wild Winter
 1967: The One and Only Genuine Family Band
 1969: Superhirn in Tennisschuhen (The Computer Wore Tennis Shoes)
 1969: McGee, der Tiger (Darker Than Amber)
 1970: Rauhes Land (The Wild Country)
 1970: Cowboy John – Der letzte Held im Wilden Westen (Scandalous John)
 1971: Die tollkühne Hexe in ihrem fliegenden Bett (Bedknobs and Broomsticks)
 1972: Es kracht, es zischt, zu seh'n ist nischt (Now You See Him, Now You Don't)
 1972: Erbschaft in Weiß (Snowball Express)
 1972: Big Boy – Der aus dem Dschungel kam (The World's Greatest Athlete)
 1973: Herbie groß in Fahrt (Herbie Rides Again)
 1974: Insel am Ende der Welt (The Island at the Top of the World)
 1975: Die Flucht zum Hexenberg (Escape to Witch Mountain)
 1975: Die Semmelknödelbande (The Apple Dumpling Gang)
 1976: Das große Ferienabenteuer (No Deposit No Return)
 1976: Gus (Gus)
 1976: Der Goldschatz von Matecumbe (The Treasure of Matecumbe)
 1977: Zotti, das Urviech (The Shaggy D.A.)
 1977: Elliot, das Schmunzelmonster (Pete's Dragon)
 1978: Der Sieg der Sternenkinder (Return from Witch Mountain)
 1978: Heiße Schüsse, kalte Füße (Hots Shots, Cold Feet)
 1978: Goin' Coconuts
 1979: Die Rückkehr der Semmelknödelbande (The Apple Dumpling Gang Rides Again)
 1979: Das schwarze Loch (The Black Hole)
 1979: Midnight Madness – ein ausgeflippter Haufen (Midnight Madness)
 1979: Herbie dreht durch (Herbie Goes Bananas)
 1980: Wir sind alle Gottes Kinder (All God's Children) (TV)
 1980: Affen, Gangster und Millionen (Going Ape!)
 1981: The Return of the Beverly Hillbillies (TV)
 1982: Ambush Mörder (The Ambush Murders) (TV)

Literatur
 Kay Weniger: Das große Personenlexikon des Films. Die Schauspieler, Regisseure, Kameraleute, Produzenten, Komponisten, Drehbuchautoren, Filmarchitekten, Ausstatter, Kostümbildner, Cutter, Tontechniker, Maskenbildner und Special Effects Designer des 20. Jahrhunderts. Band 6: N – R. Mary Nolan – Meg Ryan. Schwarzkopf & Schwarzkopf, Berlin 2001, ISBN 3-89602-340-3, S. 223.

Weblinks

Kameramann
US-Amerikaner
Geboren 1912
Gestorben 1994
Mann

Frank V. Phillips


وهو سياسي أمريكي ينتمي إلى الحزب الديمقراطي ولد توماس لي جج في 12 تشرين الأول - أكتوبر من سنة 1934 في ولاية مونتانا الأمريكية كان توماس لي جج نائبا لحاكم ولاية مونتانا ما بين الأعوام 1969 إلى عام 1973 فاز جج في انتخابات حاكم ولاية مونتانا الأمريكية سنة 1972 وأصبح جج حاكما للولاية ما بين الأعوام 1973 إلى عام 1981 توفي توماس لي جج في 8 ايلول - سبتمبر من سنة 2006 في ولاية أريزونا الجدير بالذكر بان توماس لي جج كان كاثوليكيا ودفن في مقبرة القيامة في هيلانة

مراجع

أشخاص من تشاندلر
أعضاء مجلس نواب ولاية مونتانا
أفراد عسكريون من مونتانا
حكام ولايات أمريكية من الحزب الديمقراطي
حكام ولاية مونتانا
خريجو جامعة نوتر دام
رومان كاثوليك أمريكيون
سياسيون أمريكيون في القرن 20
سياسيون من هيلينا (مونتانا)
مواليد 1934
مواليد في هيلينا (مونتانا)
وفيات 2006
وفيات في تشاندلر
وفيات بسبب التليف الرئوي
وفيات بسبب الفشل التنفسي
نواب حكام مونتانا

أعضاء مجلس شيوخ ولاية مونتانا
ديمقراطيون من ولاية مونتانا
كاثوليك من أريزونا
كاثوليك من مونتانا
أعضاء الحزب الديمقراطي في مجلس نواب ولاية مونتانا

توماس لي جج


Die Liste der denkmalgeschützten Objekte in Horná Kráľová enthält das eine nach slowakischen Denkmalschutzvorschriften geschützte Objekt in der Gemeinde Horná Kráľová im Okres Šaľa.

Denkmäler

Legende

Einzelnachweise

Weblinks

!
Horna Kralova


O mină de teren este un dispozitiv exploziv ascuns sub sau pe sol și conceput pentru a distruge sau a dezactiva ținte inamice, variind de la combatanți până la vehicule și tancuri, care trec peste sau pe lângă ea. Un astfel de dispozitiv este de obicei detonat în mod automat prin presiune când o țintă pășește pe ea sau conduce pe deasupra ei, deși alte mecanisme de detonare sunt, de asemenea, folosite uneori. O mină de teren poate provoca daune prin efectul direct al exploziei, prin fragmentele care sunt aruncate de explozie, sau prin ambele moduri.

Denumirea provine de la practica veche de minerit militar, prin care tuneluri erau săpate sub fortificațiile inamice sau sub formații de trupe de către geniști. Aceste tuneluri ucigașe ("mine") au fost la început prăbușite pentru a distruge obiective situate deasupra lor, dar ele au fost mai târziu umplute cu explozibili și detonate în scopul de a provoca pagube mai mari.

În zilele noastre, în limbajul comun, minele de teren se referă în general la dispozitive fabricate special ca arme anti-personale sau anti-vehicule. Deși multe tipuri de dispozitive explozive improvizate ("Dei"), pot fi clasificate ca mine de teren, practic, termenul de mină este de obicei rezervat pentru dispozitive fabricate și concepute pentru a fi utilizate de către servicii militare recunoscute, în timp ce IED este folosit pentru dispozitive improvizate și asamblate de grupuri paramilitare, insurgente sau teroriste.

Utilizarea minelor de teren este controversată din cauza potențialului lor de a fi arme folosite fără discernământ. Ele pot rămâne periculoase după mulți ani de la încheierea conflictului, afectând economia și civilii din multe națiuni în curs de dezvoltare. Convenția din 1997 privind Interzicerea Utilizării, Stocării, producerii și Transferului de Mine antipersonal și Distrugerea acestora, cunoscută și ca Tratatul de la Ottawa a fost încheiat din cauza unor presiuni din partea grupurilor organizate prin Campania Internațională pentru interzicerea minelor terestre, o mișcare globală. Până în prezent, 162 de state au aderat la tratat.

Utilizarea
Minele de teren au fost concepute pentru două utilizări principale:
 Pentru a crea bariere tactice de apărare, dirijând forțele atacante către zonele de incendiu predestinate sau încetinind înaintarea forțelor invadatoare pentru a permite sosirea întăririlor.
 Pentru a acționa ca arme pasive din zonă de negare (pentru a opri inamicul de la utilizarea unui teren valoros, a unor resurse sau facilități când apărare activă din zonă nu este de dorit sau posibilă).
Minele de teren sunt utilizate în prezent în cantități mari, mai ales pentru acest prim scop, astfel, utilizarea lor pe scară largă în zone demilitarizate (DMZs) probabil tensionate, cum ar fi Cipru, Afganistan și Coreea. Începând din anul 2013, numai guvernele care încă puneau mine de teren au fost Myanmar în cadrul unui conflict intern, și Siria, în războiul civil.

Minele de teren continuă să ucidă sau rănesc cel puțin 4.300 de oameni în fiecare an, chiar zeci de ani după finalul conflictelor pentru care acestea au fost plasate.

Istorie

Dezvoltarea premodernă
Jiao Yu în prefața lui la Huolongjing Quanzhi, scrisă în 1412 AD, a susținut că al 3-lea Cancelar Zhuge Liang a Regatului Shu, nu a folosit numai "arme de foc", ci și mine de teren în Bătălia de la Hulugu Valea împotriva forțelor Sima Yi și fiul lui Sima Zhao din Regatul Wei. Această afirmație este dubioasă, deoarece praful de pușcă pentru război nu s-a dezvoltat în China până la apariția aruncătorului de flăcări (Pen Huo Qi) în secolul al 10-lea, în timp ce mina de teren nu a fost observată în China până în secolul al 13-lea.

Note

Mine de teren

Mină de teren


Pilar de Borbón (fulde navn: María del Pilar Alfonsa Juana Victoria Luisa Ignacia y Todos los Santos (et omnes sancti) de Borbón y Borbón-Dos Sicilias, født 30. juli 1936 i Cannes, død 8. januar 2020) var en spansk infanta (prinsesse) og storesøster til den tidligere konge Juan Carlos af Spanien.

Opvækst
Pilar var ældste datter af Juan af Barcelona, der var den første i rækken til at føre den spanske kongefamilie videre. Hans far, Alfons 13., havde som følge af politiske uroligheder måttet frasige sig tronen og gå i eksil i 1931, og i 1933 frasagde Juans ældre brødre begge tronen, hvormed Juan blev arving. Han boede i de kommende år i Cannes og Rom og blev i 1935 gift med María de las Mercedes de Borbón y Orléans. Pilar blev født året efter som parrets første barn.

Pilar og hendes yngre søskende voksede op forskellige steder i Europa, hvor forældrene boede – primært i Estoril i Portugal.

Ægteskab
I 1967 blev hun gift med Luis Gómez-Acebo y Duque de Estrada (1934-1991), en spansk adelsmand. For at gifte sig med en person, der ikke var kongelig, måtte Pilar frasige sig retten til den spanske trone. Parret fik fem børn.

Filantropi
Pilar var præsident for Fédération Équestre Internationale, det internationale ridesportsforbund, i perioden 1994-2005 og var efterfølgende fortsat en aktiv støtte til ridesporten. Hun var også medlem af Den Internationale Olympiske Komité for Spanien i perioden 1996-2006, hvorpå hun blev æresmedlem af komiteen. Hun har desuden været præsident for Europa Nostra i perioden 2007-2009.

Pilar talte fem sprog flydende: Spansk, fransk, italiensk, engelsk og portugisisk.

Referencer

Kongelige fra Spanien

Pilar de Borbón