Contraction of Mercury has resulted in numerous fault scarps, including the goliath, 1000 km-long Enterprise Rupes (top), and numerous smaller, 10 km scarps (bottom).
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It also became clear that older, larger fault scarps remain active today.
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These fault scarps appeared to be young—less than 50 million years old.
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Color-enhanced images of icy scarps, or cliffs, in late spring through to early summer.
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The resulting small fault scarps are like saplings on a tree thought to be extinct, he added.
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They're comparable in scale to the small scarps found on the moon, which is also shrinking and tectonically active.
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If those scarps had been bombarded a million years ago, scientists wouldn't be able to see them now, said Watters.
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He conveys the experience of kayaking through mountainous "scarps of sea"; his enthusiasm for snoozing in soggy sleeping bags is infectious.
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These images reveal numerous tiny fault scarps; offsets in the surface that form as Mercury's interior cools and the planet's crust shrinks.
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And since Mercury doesn't have a protective atmosphere like Earth's, these fault scarps must be young enough to have survived consistent meteoroid bombardment.
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A high-resolution elevation model derived from MESSENGER image reveals Mercury's Great Valley, in blue, cutting between two large fault scarps and intersecting a crater.
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The team found that eight of these quakes seemed to occur close to these fault scarps, according to the paper published Monday in Nature Geoscience.
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According to Watters and his team, this is the most likely explanation for the creation of the giant valley and the massive scarps that flank it.
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Large fault scarps, which appear like rocky cliffs, were first found on Mercury in the mid-1970s and confirmed that the planet had contracted in the past.
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Based on numerous tiny fault scarps scattered across the planet's surface, scientists determined that Mercury is undergoing crustal shrinking, a form of tectonic activity, as its core cools.
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Then, over that, I sculpted features like the very deep scarps, cliff sides, sulfur fields, volcanoes, craters, and things that might be perceived from a closer vantage point.
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Small fault scarps on the Moon are believed to be connected with moonquakes, which we've been picking up ever since Apollo astronauts installed a seismometer on the lunar surface.
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So in addition to finding the shallowest water ice deposits known on Mars, the researchers are also the first to observe active erosion of the Martian midlatitude ice scarps.
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Observing Mercury's small scarps has been an "interesting development," he said, because it shows that the planet hasn't cooled down yet—contrary to what its small size would suggest.
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But Mexican workers would not be the only ones at risk of losing their jobs if the Trump administration scarps NAFTA and puts up trader barriers that would invite retaliation.
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While the largest of Mercury's faults are comparable in size to the San Andreas, these newly found tiny fault scarps are only ten meters tall and a few kilometers wide.
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The valley is bounded by two enormous fault scarps—step-like structures where two sides of a fault have become vertically offset from one another—and it cuts up to 2 miles deep.
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But in 2010, high-resolution images taken by the Lunar Reconnaissance Orbiter (LRO) mission revealed Moon-wide fault scarps, or cliffs tens to hundreds of feet high produced by motion along fault lines.
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Watters hopes the LRO team will be able to re-analyze fault scarps imaged by the orbiter since 2009 to find evidence of movement—that would be a smoking gun signature, he said.
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Mercury has been hiding an exciting secret: the closest planet to our Sun is perpetually shrinking, according to new data from NASA, which shows the appearance of new, tiny cracks on Mercury's surface called "fault scarps".
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Watters also happens to be a mission scientist for the Lunar Reconnaissance Orbiter, which has spent the last few years snapping incredibly high-res images of the Moon's surface, through which we've identified numerous tiny fault scarps.
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A new theory put forth by NASA scientists proposes that a significant portion of these features, including numerous ridges, scarps, and valleys, were caused by a subterranean ocean that eventually froze and expanded, forcing itself to the surface.
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For tourists, it promised cheap, air-conditioned travel far from the Rift Valley scarps and rock-hewn churches of Ethiopia's Northern Circuit, in a region that nonetheless incorporated some of the most remarkable sights in the African Horn.
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This remotely operated vehicle (ROV) is currently livestreaming its adventures at the US-Mid-Atlantic margin, about 80 miles off the coast of Chesapeake Bay, where the North American continental shelf scarps into the deep waters of the Atlantic Ocean.
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"If we ever get to the point where we could put a seismometer on Mercury, there's a very good chance it could detect Mercury quakes associated with continued contraction," Watters said, adding that ongoing seismic activity may help tiny scarps evolve into larger features.
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The scarps tend to be straight in intercrater plains material, but become notably lobate in crater fill (for example, within Saikaku). This set of northeast-trending scarps and troughs, and another set of north-trending scarps and troughs within and north of crater Van Dijck, probably follow zones of structural weakness in the mercurian crust.
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The fault forms an outstanding prismatic-tectonic mountain block composed of pyroclastic flow and ash-fall deposits. This block is bounded by two well developed fault scarps of about height; one facing west-southwest and the other facing south-southwest. There is geomorphic evidence of scarp degradation and old landslides on the face of these scarps. Deep canyons cut about into scarps formed against a flat-topped high mountain.
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A fault scarp is a small step or offset on the ground surface where one side of a fault has moved vertically with respect to the other. Active faulting can cause fault scarps to appear either individually or as multiple subparallel scarps.
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The earthquake remains as one of the best examples ever for evidence of creating fault scarps along the west side of the Tobin Range. It produced four scarps, with a total length of , and re-ruptured Holocene scarps located at the bottom of the base of the mountain blocks. Among the scarps, the average vertical displacement among the affected areas was , and the maximum displacement of occurred near the old Pierce School site on Buskee Creek Canyon.Mt. Tobin, Nev 15 minute topographic quadrangle, 1961, USGS The rupture originated along an unnamed fault somewhere in the eastern side of Pleasant Valley, in north- central Nevada.
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Lobate scarps are the most common structural landforms in the Bach region. Almost all have convex slope profiles, rounded crests, and steep, sharply defined lobes. Three types are seen in the map region: (1) very small (<50 km long, ~100 m high), irregular scarps that commonly enclose topographically depressed areas; they are restricted to the intermediate and smooth plains units in the eastern part of the map region; (2) small (~100 km long, ~100 m high), arcuate or sinuous scarps, also confined primarily to the intermediate and smooth plains units in the eastern part of the map region; and (3) large (>100 km long, ~1 km high), broadly arcuate but locally irregular or sinuous scarps whose faces are somewhat steeper. Several of these scarps (lat 83° S., long 80°) deform craters and offset preexisting features vertically (FDS 166751).
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The northern portion of the image shows layered crust labeled "layered plain". ;Common features Several common features of Ionian mountains have been summarized. # Basal scarps: basal scarps always appear as an abrupt boundary of Ionian mountains that separate mountains from volcanic plains. Most Ionian mountains are observed to have this feature.
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Discovery Rupes cuts through Rameau crater, center Morphologically diverse scarps, ridges, troughs, and other structural lineaments are relatively common in the Discovery quadrangle. DzurisinDzurisin, D. (1978). "The tectonic and volcanic history of Mercury as inferred from studies of scarps, ridges, troughs and other lineaments." Journal of Geophysical Research 83(B10): 4883–4906.
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During the investigations of the Bloody Creek structure, a cluster of discontinuous arcuate scarps were found about north of it. These arcuate scarps are known as the North Group. The analysis of aerial photography found that it consists of several discontinuous arcuate scarps that are high and sharply outline depressions with relatively flat, inner floors. Sonar and lake sediment probing of a few of these structures, which are now submerged beneath Dalhousie Lake, revealed the presence of crater-like features, which underlie these floors and are inferred to be buried by lake sediment and peat.
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Altogether they produce a zigzag pattern. The pattern is shown by faults, volcanic fissures, valleys, dikes, volcanoes, grabens and fault scarps.
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Robinson M.R. and Lucey P.G. (1997) Science 275, 197-200. Such relations strongly support a volcanic origin for the mercurian smooth plains, even in the absence of diagnostic landforms. Lobate scarps are widely distributed over MercuryMelosh H.J. and McKinnon W.B. (1988) In Mercury, 374-400. and consist of sinuous to arcuate scarps that transect preexisting plains and craters.
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145 The fault system is reverse sinistral (left lateral) in the northern part of the country, conspicuous to about latitude 5° N, from there south to Ecuador, it is mainly reverse-dextral (right lateral). The system forms prominent fault lines and well-developed fault scarps as much as high on Pleistocene-aged sedimentary deposits, and eroded scarps on older Cretaceous to Paleozoic rocks. The system forms an outstanding break-in-slope above the easternmost parallel set of faults. The upper part of the easternmost major scarps forms the topographic divide of the Central Ranges of Colombia.
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The main cliff face of Hart Mountain towers above the valley floor. It runs the length of the valley, eventually being lost in a series of smaller fault scarps at the north end of the valley. These smaller scarps generally run from the east side of the valley to the northwest. The south end of the valley is more complex.
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Structural features are sparse or unresolved in this part of Mercury. The Kuiper quadrangle apparently has none of the scarps that occur elsewhere on the planet that have been interpreted as high-angle reverse faults. The most prominent structures are the rings associated with some large craters or basins, faults that transect crater floors, and lobate scarps and ridges in the plains materials. Most of the faults and scarps that transect crater floors clearly delineate crater-filling materials standing at different levels, and in at least two craters (19° S., 31°; 16° N., 30°), the traces of the faults on the crater walls indicate that the faults have normal displacements.
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One of the major differences between the mercurian and lunar surfaces is “the widespread distribution [on Mercury] of lobate scarps which appear to be thrust or reverse faults resulting from a period of crustal compression...” These scarps are unique structural landforms that were noted soon after the acquisition of Mariner 10 photographs. Murray and others (1974) described them as having a sinuous outline, a slightly lobate front, and a length of more than 500 km. A more detailed description is given by Strom and others. Dzurisin (1978) classified these scarps, differentiating between intercrater and intracrater scarps (a scheme adopted in mapping the Borealis region) in an attempt to understand the tectonic and volcanic history of Mercury. Melosh (1977) and Melosh and Dzurisin (1978) proposed a planetary grid composed of conjugate northeastand northwest- trending shear fractures formed by the stresses of tidal despinning early in mercurian history.
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A series of slump scarps along the western edge of the shelf are 18–2 Mya, but covered by younger sediments brought there by the Benguela upwelling.
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Scarps of this type are considered by Strom and others to be compressive thrust faults resulting from overall shortening of the mercurian crust early in its history.
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The scarps also separate a series of sandstone plateaus, the highest of which is the Adrar Plateau, reaching an elevation of 500 metres. Spring-fed oases lie at the foot of some of the scarps. Isolated peaks, often rich in minerals, rise above the plateaus; the smaller peaks are called Guelbs and the larger ones Kedias. The concentric Guelb er Richat is a prominent feature of the north- central region.
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At points where the Boring Lava sits over Troutdale Formation deposits, landslides are frequent, producing steep head scarps with heights of . These scarps tend to have grabens at their bases and Boring Lava blocks at their tops, and they show variable slide surfaces from hummocky to flat. A number of these exposure show dips up to 35 degrees, as well as minor faults. The landslides range in thickness from .
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The scarps also separate a series of sandstone plateaus, the highest of which is the Adrar Plateau, reaching an elevation of 500 metres. Spring-fed oases lie at the foot of some of the scarps. Isolated peaks, often rich in minerals, rise above the plateaus; the smaller peaks are called guelbs and the larger ones kedias. The concentric Guelb er Richat is a prominent feature of the north- central region.
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The main vegetation type on the island plateau is introduced grassland. Cliffs and scarps support grassland and herbfield. There are patches of mixed shrubland, including many introduced species.
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The target landing zone was a region near the south pole of Mars, called Ultimi Scopuli, because it featured a large number of scopuli (lobate or irregular scarps).
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Steep normal faults produced prominent seafloor scarps but resulted in only a minor extensional component. At this stage, in terms of horizontal motion, the Adare Basin is nearly locked.
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One unusual feature of Mercury's surface is the numerous compression folds, or rupes, that crisscross the plains. As Mercury's interior cooled, it contracted and its surface began to deform, creating wrinkle ridges and lobate scarps associated with thrust faults. The scarps can reach lengths of 1000 km and heights of 3 km. These compressional features can be seen on top of other features, such as craters and smooth plains, indicating they are more recent.
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The rupture caused clear surface faulting; a long northwest-trending zone of fresh scarps and ground ruptures was present on a slope of the Lost River Range. Extensive breakage occurred along a zone between West Spring and Cedar Creek; ground surface was literally "shattered" into tilted blocks, each several meters in width. These scarps were as broad as . The ground breakage was , and the throw on the faulting ranged from -0.5 to 2.7 m.
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The convents had their walls doubled in thickness, their windows blocked up, their surroundings guarded by scarps, counter-scarps, and palisades. Mounting 30 cannons, the largest fort, San Vincente was located at the southwest angle of the old city wall. San Cayetano with four cannons was southeast of San Vincente. South of San Cayetano was La Merced with two guns that prevented the Allies using the Roman bridge over the Rio Tormes.
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On the southern and eastern side the scarp is long and high, while the southern side is about long. A large wedge-shaped scar is recognizable on the northwestern flank, delimited by prominent scarps running through the western and northern flanks of the edifice. The existence of a lake in the summit area within the scarps at elevations of has been reported. On the northeastern flank a pumice deposit is clearly visible.
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Darío lies on the western rim of the much larger Aneirin crater. The highest of several scarps that cut across the floor of Darío corresponds with the rim of Aneirin.
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The 1915 Pleasant Valley earthquake produced dramatic fault scarps along the west margin of the range with up to of vertical displacement. Tobin Range was named after Clement L. Tobin.
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These three scarps lie on a large arc extending for more than 1000 km. Resolution Rupes is separated from Adventure Rupes by a high relief ridge informally called Rabelais Dorsum, which crosscuts the scarps. This means that Resolution Rupes and Adventure Rupes may be parts of one large structure similar in length to Discovery Rupes. The scarp is named after HMS Resolution, one of James Cook's ships on his second voyage to the Pacific, 1772–1775.
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These relations suggest that scarp formation occurred in c3 to c4 time. Very smooth plains material flanks some scarps and ridges and, if the material is ponded extrusives or mass-wasted products, may postdate the structures. Scarps and ridges are abundant in intercrater, intermediate, and smooth plains units, but they are not embayed by intermediate and intercrater plains materials. These relations suggest that the structures began to form after emplacement of these two oldest plains units.
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It is not always clear whether a strandline is actually a strand line or a surface expression of fault activity; some supposed lower strandlines at Mormon Point were later reinterpreted as fault scarps.
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They are most convincingly interpreted as thrust faults, indicating a period of global compression. The lobate scarps typically transect smooth plains materials (early Calorian age) on the floors of craters, but post-Caloris craters are superposed on them. These observations suggest that lobate-scarp formation was confined to a relatively narrow interval of time, beginning in the late pre-Tolstojan period and ending in the middle to late Calorian Period. In addition to scarps, wrinkle ridges occur in the smooth plains materials.
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However, unambiguous extensional features (very rare on the planet as a whole) are not seen in the Discovery quadrangle; only compressional scarps occur. Thus, core segregation occurred relatively early (before formation of a solid lithosphere) and was followed by cooling and contraction, the last phases of which probably contributed to the formation of arcuate scarps that predated the end of heavy bombardment. Rotational breaking by solar torques is another process likely to have occurred early in Mercurian history.Goldreich, P. & Soter, S. (1966).
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The process also involves capturing of digital aerial photographs. In order to interpret deep-seated landslides for example, under the cover of vegetation, scarps, tension cracks or tipped trees airborne lidar is used. Airborne lidar digital elevation models can see through the canopy of forest cover, perform detailed measurements of scarps, erosion and tilting of electric poles. Airborne lidar data is processed using a toolbox called Toolbox for Lidar Data Filtering and Forest Studies (TIFFS) for lidar data filtering and terrain study software.
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The many kilometers of visible fault breaks on the surface of the earth presented scientists with opportunities for field investigations that ultimately led to an improved understanding of the fault scarps that earthquakes often generate.
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Most of the sediments appear to originate locally, either from biological activity or as carbonates. Antiforms, gullies and scarps occur on the seamount, the latter are evidence of past submarine landslides or mass wasting phenomena.
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The Montenegro Fault is part of the Romeral Fault System, running through the western slope of the Central Ranges. The fault is located to the west of the city of Armenia. The fault crosscuts and deforms the Pleistocene volcanic and volcano-sedimentary deposits of the Quindío Fan (), which covers about . The Montenegro Fault forms outstanding fault scarps as much as in height, beheaded streams, hanging valleys, ponded alluvium, aligned and offset drainages, as well as soil and rock slides on the face of the scarps.
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Sachs Patera is a feature on Venus. Defined as a sag-caldera, Sachs is an elliptical depression 130 meters (81 feet) in depth, spanning in width along its longest axis. The morphology implies that a chamber of molten material drained and collapsed, forming a depression surrounded by concentric scarps spaced apart. The arc-shaped set of scarps, extending out to the north from the prominent ellipse, is evidence for a separate episode of withdrawal; the small lobe-shaped extension to the southwest may represent an additional event.
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The architectural feature has been richly detailed with sculpture, including the: lintel, window and portal frames, pilaster bases and capitals, cornices, and friezes. Furthermore, some of the blind windows, window niches, sacristy, and scarps are plastered.
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The stresses responsible for the elongate ridges and scarps must have occurred after the end of the primordial bombardment and after emplacement of the intermediate plains unit. Where smooth plains material abuts ridges and scarps, the evidence is mostly ambiguous because we cannot tell if ridge formation involved smooth plains material or if the ridges are upwarped intermediate plains material with smooth plains material ponded against them. On the floors of some craters, such as Gluck, scarps apparently offset material mapped as smooth plains, but the exposures are so small that this interpretation could easily be challenged. Ridges appear to be both older and younger than medium-size craters (30–60 km in diameter) on the intermediate plains unit, but intersections of ridges with craters in this size range are too rare to constrain the time of ridge formation.
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The Honda Fault extends through the Middle Magdalena Valley, close to the Magdalena River and the cities of Ambalema, Honda, and La Dorada. It offsets beds of the Miocene Honda Group, Pliocene Mesa Formation, and Quaternary sediment in alluvial terraces. The fault trace is characterised by continuous prominent scarps, aligned drainages, fault saddles, linear ridges and valleys, sag ponds, degraded scarps, and localized uplifts. The southern half of the fault has a very low to low slip rate (less than per year), while the northern half is low to medium at per year.
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The Wambaw Swamp system is one such swamp. The highest ground in the Wambaw Swamp system is the Little Wambaw Swamp, which formed on the Princess Anne Terrace, bounded on the south by the Mount Pleasant Scarp and the north by the Awendaw Scarp. The Little Wambaw Swamp drains north through a gap in the Awendaw Scarp into the Wambaw Swamp proper, which is contained between the Awendaw and Cainhoy Scarps on the Pamlico Terrace. The Wambaw Swamp drains east along the Pamlico Terrace, parallel to the scarps and coast, into the Santee River.
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This area and its antipode in the Discovery quadrangle are the only two on Mercury where tensional forces can now be seen to have shaped the surface. The Tolstoj Basin is encompassed by parts of at least three ragged and discontinuous inward-facing scarps. Lineated ejecta is best developed in the vicinity of and beyond the outer scarp, whereas blocky materials occur between the inner and outer scarps. These relations are similar to those around Caloris, although Tolstoj is less than half its size and is much more severely degraded by later impact cratering.
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Some very smooth plains material, most of which postdates c4 craters, appears to postdate the scarps that it commonly embays. Superposition relations of scarps in other regions of Mercury indicate that tectonic activity may have continued into c5 time (Leake, 1982). However, the time of formation of c5 craters and very smooth plains material has, for the most part, been tectonically quiescent. During this period, with the exception of a scattering of extremely fresh craters and some minor mass wasting (Malin and Dzurisin, 1977), almost no geologic activity has occurred near the mercurian south pole.
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Parts of the Aeolis quadrangle contain fretted terrain which is characterized by cliffs, mesas, buttes, and straight-walled canyons. It contains scarps or cliffs that are 1 to 2 km in height.Sharp, R. 1973. Mars Fretted and chaotic terrains.
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Pediplanation is linked to scarp retreat in the following way: as scarps retreat over geological time pediments migrate and extend over large areas. The result is that the surface is eroded chiefly backward and that downward erosion is limited.
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They tend to be larger than shallow landslides and form along a plane of weakness such as a fault or bedding plane. They can be visually identified by concave scarps at the top and steep areas at the toe.
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Surface ruptures associated with normal faults are typically simple fault scarps. Where there are significant superficial deposits, sections with more oblique faulting may form sets of en- echelon scarp segments. Antithetic faults may also develop, giving rise to surface grabens.
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The area is mostly covered by a Pliocene blanket of pyroclastic rocks and calc-alkaline lavas, Quaternary lahar deposits and fluvio-glacial deposits. The Buesaco-Aranda Fault has a very well-defined fault trace, with strongly deformed landforms of Pleistocene- Holocene age, clear breaks in slope along eroded fault scarps, and fault scarps facing both to the southeast or the northwest, which is a characteristic of strike-slip faults. Systematic right lateral deflections of some stream gullies, river channels, and ridges are visible. Offset features in confined alluvial deposits and in recent alluvial fans have fresh scarp morphology.
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The Wambaw Swamp lies in a geological province known as the coastal terraces, with surface features derived from the Pleistocene inundations of the Atlantic Ocean. During this epoch, the Atlantic Ocean advanced and retreated over this area numerous times. The successive shorelines created alternating tidal flats and barrier islands, similar to those along the present coastline just to the southeast of the swamp; today these features, stranded on higher land once the ocean retreated, are marked by terraces and scarps, respectively. These scarps create barriers to drainage, capturing runoff and leading to the formation of swamps on their landward side.
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Neither faults nor scarps that are possibly associated with faults or monoclinal folding appear to be common in the Beethoven quadrangle, possibly because of the high sun elevation. The longest and most prominent of these structures occur in the plains and terra material, undivided, in the southeast quadrant of the map area. There, a series of prominent scarps extends northeast from near latitude 10° S., longitude 95° to latitude 4° S., longitude 86°, over a distance of about 400 km. The inner ring of crater Durer appears to be slightly offset on the north side by a small normal or strike- slip fault.
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Wine growing on the steep loess slopes facing Lake Neusiedl. All towns are situated at the foot of the scarps. Large-scale dairy farming. right left The East railway line and the A4 autobahn (opened in Autumn 1994) run through the Parndorf plain.
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It often weathers to prominent scarps without talus. For the most part, Middle Cretaceous rocks include thick sandstone, although some marine rocks are present to the north and Jordan. A combined sequence of of limestone and dolomite spans the Cretaceous into the Paleogene.
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Other boundaries lie on ridges in more recent deposits and scarps (escarpments). These include the Côte d'Or in the south-east (on an Alpine fault line) and, at a north end, the Hills of () Artois which overlie the margin of London-Brabant Massif.
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Vostok transects and foreshortens the crater Guido d'Arezzo, which suggests that arcuate scarps are compressional tectonic features (thrust or high-angle reverse faults). Melosh and DzurisinMelosh, H.J. & Dzurisin, D. (1978). "Mercurian global tectonics: A consequence of tidal despinning?" Icarus 35(2): 227–236.
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Mapa Geológico de Quindío, 2000 Well preserved fault trace controls stream draingages. The Córdoba- Navarco Fault forms fault saddles and eroded fault scarps. Neotectonic features are not very outstanding. Slopes in this part of the Central Ranges are rather steep, so erosion rate is high.
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Farther northeast, the fault is overlain by young alluvial deposits of the Middle Magdalena Valley. The fault is marked by well preserved fault scarps, long straight traces, displaced drainages, and it forms aligned river courses. The slip rate is calculated at per year.Paris et al.
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The Loburn fault, which runs along the south side of Hodgsons Road, is responsible for various terraced abandoned stream channels, wedge structures and scarps, notably Round Hill. The topography in Loburn is generally flat with gently rolling hills, altitude gradually decreases southwards from the foothills.
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The municipality's arms might be described thus: Per fess enhanced in chief party per pale Or five roundels, two, one and two, sable and gules two salmon addorsed argent, in base argent two scarps vert between which six oakleaves proper, one, three and two.
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The scarps include the highest point on the planet.Denevi, B. W., Ernst, C. M., Prockter, L. M., and Robinson, M. S., 2018. The Geologic History of Mercury. In Mercury: The View After MESSENGER edited by Sean C. Solomon, Larry R. Nittler, and Brian J. Anderson.
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There are no great earthquakes that are known to have occurred at the pass, where the main trace of the SAF is marked by numerous sag ponds and north-facing scarps. The Banning Fault lies about two miles to the south of these features.
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In this reach, it is bounded by the Aravalli mountain ranges on the North and the Vindhyan hill range on the south. The Vindhyan scarps, in the northwest, flank the left bank of the Chambal, and subsequently, is mainly drained by it. The Chambal rising within about 16 km of the Narmada river, appears as a consequent on the Mesozoic surface, superimposed on the scarps, and cuts straight through them, with subsequent tributaries on the softer shales. The River Chambal and its tributaries Kali Sindh and Parbati have formed a triangular alluvial basin, about above the narrow trough of the lower Chambal in Kota.
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Brent Knoll with a sign on the M5 motorway During the medieval era the local land was held by Glastonbury Abbey until the dissolution of the monasteries in 1536. Around the sides and top of the hill are several scarps which may be medieval strip lynchets.
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Borden Peninsula extends north for . It is - wide. The northern area, including the Hartz Mountains, are composed of flat, dissected rock rising to over above sea level. The Magda Plateau is to the south where river valleys occupy the land, dividing scarps and flat-topped hills.
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Plancha 227, 1998 The fault trace is characterised by offset spurs, degraded fault scarps, saddles, small pull-apart basins, aligned drainage, and deflected streams. The fault borders the Guaduas Synclinal to the east and south.Acosta & Ulloa, 2001, p.71 It forms the northwestern boundary of the Bogotá savanna.
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These dykes and a dacitic lava dome of similar composition were formed before the 1600 eruption. A number of faults with recognizable scarps occur within the amphitheatre and have offset the younger vents; some of these faults existed before the 1600 eruption while others were activated during the event.
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The Drakensberg mountains in South Africa are capped by a layer of Karoo basalts about thick, which overlay Clarens formation sandstones. They have long been considered a classic example of a landform created by scarp retreat following continental break-up, with the retreat controlled by an inland drainage divide. However, they have inland-facing scarps as well as seaward-facing scarps, so factors other than continental break-up have contributed to their formation. A 2006 paper argued that surface process models may be inadequate in explaining rates of scarp retreat, which can also be greatly affected by the types of rock encountered as the scarp retreats, and by other factors such as climate, tectonic processes and possibly plant cover.
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Ancient fractures that were reactivated by later impacts may have first provided the conduits for crater fill (smooth plains material) and later been propagated upward through the fill. That these ridges, scarps, and troughs are parts of a global grid of fractures cannot be stated conclusively because of their proximity to the terminator and the lack of photographic coverage beyond the 190° meridian. Some scarps probably were formed by normal faulting of the smooth plains material that covers some crater floors, as in the Kuiper quadrangle (Scott and others, 1980). We cannot, however, determine whether most lineaments are internal or are parts of a faulted and lineated facies associated with a nearby but unphotographed impact basin.
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The map region displays a wide variety of structural features, including lineaments associated with ridges, scarps, and polygonal crater walls. Joint- controlled mass movements are most likely responsible for the polygonal crater- wall segments; segments as long as 100 km suggest that these fractures extend deep into the lithosphere. The most conspicuous trends of these lineaments are east-west, N.50° W., and N. 40° E. More trends are north-south, N.20° E., and N.70° E. Large ridges and scarps are the most prominent structural features in the low-sun-angle Mariner 10 pictures of the Bach region. They are most numerous between long 0° and 90°, where they have no preferred orientation.
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The Abriaquí Fault parallels the Cañasgordas Fault to the south, cutting Cretaceous oceanic volcanic rocks as well as Tertiary and Cretaceous sedimentary rocks. The fault has a well defined fault trace with scarps, saddles, and deflected streams. The slip rate is estimated at per year deduced from displaced geomorphologic features.
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Along with three large volcano complexes, and two other small and steeper cone-shaped complexes, several valleys, scarps, and ridges were discovered as well as a new seafloor. Additionally, on the northeast of the plateau, what researchers believe are volcanic hills, were discovered from the bathymetry data from the survey.
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The Deltana Platform lies offshore, on the platform of the Orinoco delta about 90 km northeast of the island Tobejuba in the state Delta Amacuro, and approximately 233 km southeast of Güiria, Sucre State, Venezuela. Pinguer 3.5 KHz. Showing abrupt erosional slopes and scarps. Deiros,D. (2002). Side Scan Sonar100KHz.
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He was a member of the Cosmos Club and a fellow of the American Geographical Society. His papers include 'Scarps of southwestern Sierra Nevada, California': Bulletin of the Geological Society of America, December 1928; and 'Scientific Manpower and National Safety' in the Bulletin of the American Association of Petroleum Geologists 1956.
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It is native to an area of the Pilbara region of Western Australia centred around Newman where it is commonly found on scarps composed of weathered sediments growing in shallow soils. It only has a limited distribution in the Northern Territory but is quite common in central and southern Queensland.
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In the center of the elevated region is a depression; this is bounded by scarps and may be some kind of caldera. Just to the north is a feature called Little Dome, in diameter. Further north is an elongated dome, oriented north-south, called Middle Dome. It is long and wide.
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This species is endemic to New Zealand, found on coastal cliffs, sand dunes, banks and slopes and rocky lake shore scarps. It is at risk from browsing domestic and feral animals including pigs, cattle and sheep. Possums are also a threat. Its habitat can be impacted by road widening or erosion.
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This theory is now disproven and considered obsolete. In contrast to Earth, however, global cooling remains the dominant explanation for scarp (cliff) features on the planet Mercury. After resumption of Lunar exploration in the 1990s, it was discovered there are scarps across the Moon's surface which are caused by contraction due to cooling.
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The fault zone is characterized by fault scarps, saddles, linear ridges, displaced streams, shutter ridges, and aligned springs. Some topographic features show evidence of sinistral offset. Locally, two fault traces bound a depressed block (pull- apart basin). Based on stratigraphic evidence, dextral movement of about is reported, which probably occurred before Quaternary time.
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These scarps are long and as much as high. Most of the fault trace has a moderate alignment of topographic features, such as linear streams and offset spurs. Quaternary alluvial sediments of the Penderisco River are offset an unknown amount. The slip rate is estimated at per year deduced from displaced Quaternary sediments.
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It is shaped more like an irregular polyhedron with several slightly concave facets and relief as high as . Its surface is dark, neutral in color, and heavily cratered. Proteus's largest crater is Pharos, which is more than in diameter. There are also a number of scarps, grooves, and valleys related to large craters.
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Most of the group has been deeply eroded by numerous rivers creating the ragged plateaus and scarps of the Durban-Pietermaritzburg region.Tankard, A.J., Jackson, M.P.A., Erikson, K.A., Hobday, D.K., Hunter, D.R., Minter, W.E.L. (1982) Crustal Evolution of Southern Africa: 3.8 Billion Years of Earth History. pp. 333–363. Springer-Verlag. New York.
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The most conspicuous structural elements in the quadrangle are the radial and concentric ridges and cracks inside the Caloris Basin and the ridges developed in the Odin Formation and smooth plains unit immediately outside Caloris. O’Donnell and Thomas (personal communication, 1979) have suggested, on the basis of orientation of features outside Caloris, that these ridges and scarps largely follow preexisting radial and concentric fracture patterns in the mercurian lithosphere initiated by the Caloris impact, similar in character to those around Imbrium on the Moon (Mason and others, 1976). Caloris itself consists of a single mountain ring and a weak outer scarp. A few sinuous scarps also occur in this quadrangle, including the Heemskerck Rupes which cuts the older intercrater plains.
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The Magda Plateau is an uninhabited plain in Qikiqtaaluk, Nunavut, Canada. It is located in the southern area of Baffin Island's the Borden Peninsula. The plateau's river valleys traverse over scarps and flat-topped hills. Though part of the peninsula is within Sirmilik National Park, the plateau is outside of its boundaries, to the southwest.
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They are believed to form from the removal of subsurface material, maybe interstitial ice by sublimation (change from solid to a gas). More gentle slopes face in the direction of the equator, while steep scarps face the pole. This is probably due to differences in solar heating. The process is believed to be ongoing.
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In the Central region the Coastal Range is bounded by the N-S striking Remiendo Fault with ancient fault scarps in the eastern area of the region. In the Southern region the Coastal Range is bounded by the El Salado Fault, which trends North and is cut to the north by TalTal N130 striking faults.
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Museum entrance Silk glove display Detail of Medieval wall painting Sherborne Museum is an independent local museum centrally situated in Sherborne, a small market town in north-west Dorset. Formerly a Saxon burgh, Sherborne evolved through the cloth, gloving and silk industries and is embedded in varied countryside united by scarps of Jurassic limestone.
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The basal scarps are ten to a few hundred meters high. Sometimes, the scarp is resolved in high-resolution images as the margin of a debris apron. An example is Iopolis Planum. # Tilted block: thrust faults have been interpreted to bound tilted blocks on Io. Tilted blocks have a polygonal shape and curved crests.
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Other landforms on Proteus include linear features such as scarps, valleys, and grooves. The most prominent one runs parallel to the equator to the west of Pharos. These features likely formed as a result of the giant impacts, which formed Pharos and other large craters or as a result of tidal stresses from Neptune.
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Aside from these lapilli deposits, scoriaceous lava flows are exposed on the edifice as well. Farther down, lava flow fronts form scarps which become particularly noticeable at depths of , except on the northern flank. Even deeper, pillow lavas predominate. Below the summit area, the slopes fall down steeply to a depth of and then flatten out.
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Glacial-like flow features near the Mamers Valles. Scarps and hills appear twisted like taffy, probably the result of the slow movement of the subsurface ice. Note the patterned ground at top center. These small-scale textures may be the result of sublimation (evaporation) of subsurface ice combined with the taffy-like shifts in the ground surface.
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Surface scarps due to faulting are rarely observed in this area (due to topography, vegetation, and urbanization); a rare exception can be seen at Mee Kwa Mooks Park south of Alki Point. This is the site of the West Seattle Fault; the prominent rise there is due to uplift on the north side of the fault., p.1588; .
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The Colorado Plateau has a cuesta scarp topography, consisting of slightly deformed strata of alternating harder and softer rocks. The climate has been mostly dry throughout the Cenozoic. The conspicuous scarps on the plateau have massive sandstone caps over easily weathered rock such as shale. Freeze-thaw and groundwater sapping contribute to scarp retreat in this region.
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Crassula colligata is a herb in the family Crassulaceae that is native to Western Australia. The annual herb has an erect habit and typically grows to a height of . It is commonly found on cliffs, scarps, in gullies, behind dunes and near salt lakes along the south coast in the Great Southern, Wheatbelt and Goldfields-Esperance regions.
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Rembrandt is the second largest impact basin (crater) on Mercury after Caloris. Its outer boundary, which is called crater rim, is defined by a ring of inward facing scarps and massifs. The diameter of this ring is — half the diameter of Caloris. The basin is surrounded by blocky impact deposits made from material excavated at depth.
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From it the scarps of the footwall of the Sparta Fault are visible at the base of Tayegetus. Taygetus is transected by deep ravines through which tributaries flow into the Eurotas. At the foot of the massif is a zone of scree. To the east of that alluvial fans from Taygetus cover half the valley, making it asymmetrical.
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Sky City flies above a region of grassland dotted with crags. Alex Raymond and Don Moore, "Monsters of Mongo" (4/15/34 to 11/18/34) Between Mingo City and Sky City is the land of the Brown Dwarves. East of Sky City is Flame World, a dusty region of scarps and ravines of basaltic rock.
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Ronciglione (locally ) is a city and comune in the province of Viterbo, Lazio (central Italy), about from Viterbo. The city is located in the Cimini mountains, over two tuff scarps, on the SE slope of the former volcano crater now housing the Lake Vico. The city's economy is based largely on agriculture, with production of nuts, chestnuts and wine.
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Vulcan Planum is in the southern hemisphere of Charon. Its extents are not completely known, but it occupies at least . Vulcan Planum is separated from Oz Terra by a series of scarps that are several kilometers high. It has a mostly smooth surface with no large craters, and its elevation is about 1 km lower than Oz Terra's.
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Serenity Chasma is long, and about deep, and its typical width is . The northern wall continues for an additional as a scarp after exiting the chasma. The chasma is part of a global techtonic belt; a series of canyons, scarps, and troughs that traverse the face of Charon. This series of faults is the longest known in the solar system.
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Mandjet Chasma is a chasma on Pluto's moon, Charon. Mandjet Chasma is long, and about deep, its typical width is . The chasma is part of a global tectonic belt; a series of canyons, scarps, and troughs that traverse the face of Charon along the northern edge of Vulcan Planum. The feature was discovered using stereoscopic processing of New Horizons images.
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These are, in essence, lithified colluvium. Thick sequences of sedimentary (colluvial) breccias are generally formed next to fault scarps in grabens. In the field, it may at times be difficult to distinguish between a debris flow sedimentary breccia and a colluvial breccia, especially if one is working entirely from drilling information. Sedimentary breccias are an integral host rock for many sedimentary exhalative deposits.
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Adventure Rupes is separated from Resolution Rupes by a high relief ridge informally named Rabelais Dorsum, which crosscuts the scarps. This means that Resolution Rupes and Adventure Rupes may be parts of one large structure similar in length to Discovery Rupes. The scarp is named after HMS Adventure, one of James Cook's ships on his second voyage to the Pacific, 1772–1775.
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The fault forms strong linear features on satellite images and aerial photographs and controls the course of the Río Sucio, which has a prominent, linear V-shaped valley. Fault scarps are formed on Quaternary mud flows. The slip rate is estimated at per year deduced from offset of mud flows and the fault was probably active in the Late Pleistocene.Paris et al.
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Its dimensions are 105 km X 48 km. The patera appears to be situated on a large plateau, that declines elevation on each side. The steep scarps also suggest that the materials it's made out of must be tough to avoid collapse. This patera is often dubbed "golf course" because of its presence of green material on the floor, detected by NIMS.
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The surface is geologically heterogeneous and is intersected by a system of grooves and scarps, which are thought to be fractures. It has a high average density, meaning that it is made of metal- rich rock. The Rosetta probe passed within of Lutetia in July 2010. It was the largest asteroid visited by a spacecraft until Dawn arrived at Vesta in July 2011.
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Livistona nitida, the carnarvon fan palm, as seen from the Amphitheatre. Three broad vegetation types are present in Carnarvon Gorge; eucalypt and angophora dominated woodland to open woodland; mixed eucalypt, acacia, white cypress pine or turpentine woodlands and/or open forests on sandstone slopes, scarps, ridges and residuals; cleared and/or regrowth areas.Grant, Claire. 2005. "Carnarvon Gorge - Management Plan" pp 6-9.
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The Indian Hills Medical Center, the Foothill Medical Building, and the Pacoima Lutheran Professional building were heavily damaged. Nursing homes also were affected. The one-story Foothill Nursing Home sat very close to a section of the fault that broke the surface and was raised up three feet higher than the street. Scarps ran along the sidewalk and across the property.
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Sedimentary breccia consists of angular, poorly sorted, immature fragments of rocks in a finer grained groundmass which are produced by mass wasting. It is lithified colluvium or scree. Thick sequences of sedimentary (colluvial) breccia are generally formed next to fault scarps in grabens. Breccia may occur along a buried stream channel where it indicates accumulation along a juvenile or rapidly flowing stream.
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Fault scarps and the Gelai Volcano can also be seen. Numerous near-white salt-crust "rafts" pepper the shallowest parts of the lake (inset). The lake is fed principally by the Southern Ewaso Ng'iro River, which rises in central Kenya, and by mineral-rich hot springs. It is quite shallow, less than deep, and varies in width depending on its water level.
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It is up to wide and features scarps up to high. By comparison, the Grand Canyon is approximately deep in some places and long but only up to wide. Chasma Boreale cuts through polar deposits and ice, such as those present at Greenland. Planum Boreum interfaces with Vastitas Borealis west of Chasma Boreale at an irregular scarp named Rupes Tenuis.
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Hawks Crag Breccia, Hawks Crag, Buller River Unconformably overlying the basement rocks west of the Alpine Fault is a terrestrial sequence that represents Zealandia's progressive movement away from Gondwana. The Hawks Crag Breccia formed from erosion off fault scarps. It is also New Zealand's best source of Uranium. These are then overlain by coal measures formed in swamps from the continued extension.
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Oz Terra is the unofficial name given to a major geological region on Charon. The Pluto-facing hemisphere of Charon is divided onto two primary regions; Oz Terra in the north and Vulcan Planum in the south. These regions are separated by a series of scarps near Charon's equator. The region was discovered by New Horizons during its flyby of Pluto in July 2015.
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Sparti, located on the east side of the Eurotas rift valley. The fault scarps marking the strike of the Sparta Fault are visible on the eastern face of the mountain. The Taygetus, Taugetus, Taygetos or Taÿgetus () is a mountain range on the Peloponnese peninsula in Southern Greece. The highest mountain of the range is Mount Taygetus, also known as "Profitis Ilias", or "Prophet Elias".
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The water depths range from about 66 m in the southwest up to 308 m in the northeast, with an average slope of approximately 0.4% (0.25 grades) to the east-northeast. The relief of the seabed is generally irregular and includes frequent scarps related with faulting and erosion.Imbrie, J. y Van Andel, TH. (1964), “Vector analysis of heavy mineral data”. Geol. Soc. Am. Bull.
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These structures resemble large, flat-topped mesas with rugged surfaces. Other mountains appear to be tilted crustal blocks, with a shallow slope from the formerly flat surface and a steep slope consisting of formerly sub-surface materials uplifted by compressive stresses. Both types of mountains often have steep scarps along one or more margins. Only a handful of mountains on Io appear to have a volcanic origin.
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Bhogawati river is a large tributary of the Sina River which originates near Osmanabad city of Maharashtra, India. Bhogavati meets Sina near Mohol in Solapur district of Maharashtra. Sina River is tributary of Bhima River. Bhogawati rises in the south-facing scarps of the Balaghat range in the north- eastern parts of Barshi taluka and after a south-westerly course of about 65 km.
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Map of districts in Maharashtra The Sahyadri range, or main range of the Western Ghats, runs north and south along the western edge of the district, separating it from Ratnagiri District. The Mahadeo range starts about 10 m. north of Mahabaleshwar and stretches east and south-east across the whole of the district. The Mahadeo hills are bold, presenting bare scarps of black rock like fortresses.
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It is endemic to south western parts of Queensland on and around the Grey Range where it is often situated on lateritic scarps and ridge-tops growing in rocky soils as a part of savannah, heath or open woodland communities. The distribution is quite fragmented with outlying populations found in the Gregory South and Warrego districts and near the border with New South Wales.
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They are best developed along the inner edge of the basin where steep inward-facing scarps are common, grading outward into smaller massifs and blocks. The range marks the crest of most prominent ring structure around Caloris. The type area is the region near 18°, 184.5° (FDS 229). It is thought to be composed of uplifted prebasin bedrock covered by deep-seated late ejecta from Caloris.
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In 2008–09, trade between the two countries stood at approximately US$80 million. Namibia's main imports from India were drugs and pharmaceuticals, chemicals, agricultural machinery, automobile and automobile parts, glass and glassware, plastic and linoleum products. India primarily imported nonferrous metals, ores and metal scarps. Indian products are also exported to neighboring South Africa and re-imported to Namibia as South African imports.
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The Desengano State Park has an area of divided between the municipalities of Santa Maria Madalena, São Fidélis and Campos dos Goytacazes in the north of the state of Rio de Janeiro. Elevations range from . The rugged terrain includes ridges, pointed peaks, sugar loaf mountains and scarps with slopes of up to 75 degrees. Peaks include the Pico do Desengano , Pico São Mateus and Pedra Agulha .
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The longest, continuous individual trace mapped by the team is approximately in Anonang. In this barangay, surface rupture trends 40 degrees northeast. The surface rupture manifested as prominent fault scarps, which range from to of vertical displacements. Other geomorphic manifestations observed in Anonang include vertical displacement of Cawasan Creek in Sitio Calubian, producing a small waterfall at the point where the fault transects the creek.
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Namibia's main imports from India were drugs and pharmaceuticals, chemicals, agricultural machinery, automobile and automobile parts, glass and glassware, plastic and linoleum products. India primarily imported nonferrous metals, ores and metal scarps. Indian products are also exported to neighbouring South Africa and re-imported to Namibia as South African imports. Namibian diamonds are often exported to European diamond markets before being again imported to India.
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From one side, the church building exhibits Italian architectural movements, whilst from the other, it has a Netherlandish Mannerist architectural style. The church is orientated, has one nave with four spans. From the east, it is closed-off by a narrowing corpus-nave presbytery in the shape of a half-rounded apse with two scarps. From the west, the façade is crowned with two towers.
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Data obtained by the Mars Express satellite, made it possible in 2004 to confirm that the southern polar cap has an average of thick slab of CO2 ice with varying contents of frozen water, depending on its latitude: the bright polar cap itself, is a mixture of 85% CO2 ice and 15% water ice. The second part comprises steep slopes known as 'scarps', made almost entirely of water ice, that fall away from the polar cap to the surrounding plains. This transition area between the scarps and the permafrost is the 'cryptic region', where clusters of geysers are located. This model explores the possibility of active water-driven erosive structures, where soil and water derived from the shallow sub-surface layer is expelled up by CO2 gas through fissures eroding joints to create spider-like radiating tributaries capped with mud-like material and/or ice.
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In some parts along the rim, inward-facing scarps may be seen. The rim is not circular but appears to be petal-shaped. Outside the rim, a continuous ejecta blanket may be discerned. The morphology of impact features such as Neith results either from the response of a relatively weak target material to a high-energy impact or from long-term viscous relaxation of the surface subsequent to impact.
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This results in internal deformation of the moving mass consisting chiefly of overturned folds called sheath folds. Slumps have several characteristic features. The cut which forms as the landmass breaks away from the slope is called the scarp and is often cliff-like and concave. In rotational slumps, the main slump block often breaks into a series of secondary slumps and associated scarps to form stairstep pattern of displaced blocks.
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The Hazelhurst was created during the Late Miocene or Early Pliocene periods and not during the Pleistocene interstadial events according to geologists MacNeil, Yon, Hendry,Hendry, C. W. Jr., and Sproul, C., Geology and ground water resources of Leon County, Florida, FGS Bulletin No. 47. and Vernon. Their argument for late Miocene or early Pliocene origin is the absence of scarps on the Hazelhurst's upper edges. MacNeil et al.
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The fort is large and encloses an area of . The earthwork ramparts and ditches largely follow the contours of the hill. The ramparts cut across the neck of the plateau on the south side; on the north and northeast sides there are no earthwork defences since the steep scarps render them unnecessary. On the southwest side, marshland was incorporated into the defences, and gaps in the rampart occur in that area.
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The smooth plains, which Voyager 2 had observed, resolved into relatively crater-free regions filled with numerous small ridges and scarps. Numerous fractures were found within the older, cratered terrain, suggesting that the surface has been subjected to extensive deformation since the craters were formed. Some areas contain no craters, indicating major resurfacing events in the geologically recent past. There are fissures, plains, corrugated terrain and other crustal deformations.
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Two regions of smooth plains were observed by Voyager 2. They generally have low relief and have far fewer craters than in the cratered terrains, indicating a relatively young surface age. In one of the smooth plain regions, Sarandib Planitia, no impact craters were visible down to the limit of resolution. Another region of smooth plains to the southwest of Sarandib is criss-crossed by several troughs and scarps.
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It is covered by numerous impact craters reaching 210 km in diameter. Oberon possesses a system of chasmata (graben or scarps) formed during crustal extension as a result of the expansion of its interior during its early evolution. The Uranian system has been studied up close only once: the spacecraft Voyager 2 took several images of Oberon in January 1986, allowing 40% of the moon's surface to be mapped.
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This fault zone is the most notable feature within the basin that is a single strand with local (fault) splays. The fault zone is also marked by low hills, scarps, and ten anticlinal folds in a right-stepping en echelon pattern. It is located in the southwest portion of the basin and is a strike-slip margin. There are several oil fields that run parallel to this fault.
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The lake was about by wide and covered the present-day locations of Estancia, McIntosh, Progresso and Willard.The lake may have resembled Lake Tahoe in California, although Lake Tahoe is considerably deeper. Lake Estancia was the easternmost pluvial lake in Southwestern North America. Distinct shoreline landforms in the Estancia Valley occur at various elevations, including bars, beaches, gravel deposits, ridges, scarps, spits, swales, terraces and wave-cut cliffs.
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The Irlanda Fault extends through the axis of the Central Ranges, east of the city of Popayán. It cuts igneous and metamorphic rocks that are capped with Quaternary volcanic ash and lapilli. The Irlanda Fault consists of two en-echelon strands. The fault trace has medium geomorphic expression and, although somewhat obscure, there are offset spurs, degraded fault scarps, broad fault valleys, saddles, aligned drainage, and deflected streams.
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Ithaca Chasma is a giant trough system about 3 km deep and approximately confined to a great circle running through the poles of Tethys. It is approximately concentric with Odysseus impact crater—a pole of Ithaca Chasma lies only approximately 20° from it. The chasma has a rather complex structure consisting of two narrow branches towards the south. Its exterior walls are made of multiple sub-parallel scarps and terraces.
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A very large earthquake doublet occurred on December 16, 1954. The Dixie Valley/Fairview earthquakes occurred four minutes apart, each with a maximum Mercalli intensity of X (Extreme). The initial shock measured 7.3 and the second shock measured 6.9 . Damage to man-made structures was minimal because the region was sparsely populated at the time, but oblique-slip motion on a normal fault resulted in the appearance of large fault scarps.
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Plains cover 80% of the Venusian surface, and, unlike those seen on other silicate planets, are heavily faulted or fractured throughout. Structurally, these plains contain features such as wrinkle ridges, grabens (fossa and linea), fractures, scarps (rupes), troughs, hills (collis), and dikes in both local and region scales. Plains often contain visible flow patterns, indicating a source from volcanic lava flows. The more pronounced lave flow fields are named fluctūs.
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Babbar Patera, located in the top-left corner of a screenshot from NASA World Wind. Babbar Patera is a patera, or a complex crater with scalloped edges, on Jupiter's moon Io. It is about 86 kilometers in diameter and is located at . It is named after a Sumerian sun god, and its name was approved by the International Astronomical Union in 1979. Some scarps near Babbar Patera may represent faults.
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Surface exposure dating is a collection of geochronological techniques for estimating the length of time that a rock has been exposed at or near Earth's surface. Surface exposure dating is used to date glacial advances and retreats, erosion history, lava flows, meteorite impacts, rock slides, fault scarps, cave development, and other geological events. It is most useful for rocks which have been exposed for between 10 years and 30,000,000 years.
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The proposal was abandoned as it would have taken at least 9 years and cost twice as much. Thus, when the railway was electrified, a new diameter, tunnel was built to the west. It goes through Mahoenui Group soft sedimentary rocks, including landslides; the cause of hummocky ground and many small scarps. A drive at the north portal showed gently-dipping massive interbedded weak claystone, siltstone and sandstone.
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However, some degradation of c3 basins occurred by isostatic adjustment. Most of the intermediate plains material formed at this time. Smooth plains material appears to be largely coeval with c4 craters and basins. The crust was under compression during c3 and c4 time, inasmuch as the compressional scarps and ridges post-date some c3 and c4 craters, and are cut by some c4 craters and by c5 craters.
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A very large earthquake doublet occurred on December 16, 1954. The Dixie Valley/Fairview earthquakes occurred four minutes apart, each with a maximum Mercalli intensity of X (Extreme). The initial shock measured 7.3 and the second shock measured 6.9 . Damage to man-made structures was minimal because the region was sparsely populated at the time, but oblique-slip motion on a normal fault resulted in the appearance of large fault scarps.
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The Laurentian Region, as recognized by Natural Resources Canada, is part of the plateau and dissected southern rim of the Canadian Shield in the province of Québec. It is a western extension of the Laurentian Mountains, and continues across the Ottawa Valley into Ontario as the Opeongo Hills. Viewed from the valleys of the Ottawa and St. Lawrence Rivers, the south-facing escarpments of the Shield give the appearance of mountains 500–800 meters high; looking across the plateau, the relief is more moderate and subdued. These scarps mark the dramatic southern edge of this Upland region, of which Mont Raoul Blanchard is the highest peak. Although the other limits are less well defined, this Laurentian Region in Quebec may be considered to extend 100–200 km northward from the scarps and to stretch from the Gatineau River in the west (mean elevation 400 m) some 550 km to the Saguenay River in the northeast.
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Close-up of Verona Rupes, a large fault scarp on Miranda possibly high, taken by Voyager 2 in January 1986 Close-up of the ring of concentric fault scarps around Elsinore Corona The three coronae imaged on Miranda by Voyager 2 The fault scarps around Elsinore (top right) and the chevrons of Inverness Corona (bottom left) Due to Uranus's near-sideways orientation, only Miranda's southern hemisphere was visible to Voyager 2 when it arrived. The observed surface has patchwork regions of broken terrain, indicating intense geological activity in Miranda's past, and is criss-crossed by huge canyons, believed to be the result of extensional tectonics; as liquid water froze beneath the surface, it expanded, causing the surface ice to split, creating graben. The canyons are hundreds of kilometers long and tens of kilometers wide. Miranda also has the largest-known cliff in the Solar System, Verona Rupes, which has a height of .
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This set of two parallel faults extend along the axis of the Western Ranges of the Colombian Andes, close to the valleys of the Anacosca and Penderisco Rivers, and the plateau of the Frontino Páramo. Located to the west of the city of Medellín, the faults mainly displace Tertiary sedimentary rocks. The west branch of the fault has mainly normal slip as observed from offset alluvial terraces. The fault forms spectacular fault scarps on terraces.
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It appears that when the Straight Creek Fault became stuck the north–south compressive force that it had accommodated by strike-slip motion was transferred to the crust of the Puget Lowland, which subsequently folded and faulted, and the various blocks jammed over one another. Other scarps associated with the Seattle fault have been identified by LIDAR-based mapping;. trenching has generally shown the faulting to be more complex than was first realized., p.1389.
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A beach on Zanzibar Zanzibar is home to large amounts of beaches and clear Indian Ocean water, as well as coral and limestone scarps which allow for significant amounts of diving and snorkeling. The diving and snorkeling are done in marine parks. The aquatic life seen includes; dolphins, moray eels, lion fish, octopus and lobster Tourists may also go dhow cruising around the small islands. Tourists can view the sunset and have refreshments on board.
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The southern extension of the valley is wider at most places. These three valley sections are separated by the closely approaching line of the scarps and the Satpura hills. Marble rocks alongside Narmada River Emerging from the Marble Rocks the river enters its first fertile basin, which extends about , with an average width of , in the south. In the north, the valley is limited to the Barna–Bareli plain terminating at Barkhara Hills opposite Hoshangabad.
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Bandiagara Escarpment in Mali. Scarp retreat is a geological process through which the location of an escarpment changes over time. Typically the cliff is undermined, rocks fall and form a talus slope, the talus is chemically or mechanically weathered and then removed through water or wind erosion, and the process of undermining resumes. Scarps may retreat for tens of kilometers in this way over relatively short geological time spans, even in arid locations.
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McCauley J.F. et al. (1981) Icarus 47, 184 Individual massifs are typically to long; the inner edge of the unit is marked by basin-facing scarps. Lineated terrain extends for about out from the foot of a weak discontinuous scarp on the outer edge of the Caloris mountains; this terrain is similar to the sculpture surrounding the Imbrium basin on the Moon. Hummocky material forms a broad annulus about from the Caloris mountains.
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A seiche, a wave effect created by wind, atmospheric pressure, or seismic activity on water, crested over Hebgen Dam, causing cracks and erosion. The earthquake created fault scarps up to high in the area near Hebgen Lake and the lake bottom itself dropped the same distance. of the area near Hebgen Lake subsided more than . Several geysers in the northwestern sections in Yellowstone National Park erupted and numerous hot springs became temporarily muddied.
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Thus, except for the lobate compressional scarps, it is difficult to separate internally produced structures from those of the complex impact history of Mercury. The azimuthal trends of all lineaments mapped within the quadrangle are, however, dominantly northwest (315°) and northeast (35°–40°). A minor, almost north-south trend is also observed. This situation is reminiscent of the so-called lunar grid on the Moon, which is generally ascribed to planetwide internal causes.
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These are compressional structures composed of linear asymmetric ridges that can be tens of kilometers wide and hundreds of kilometers long. Many aspects of these ridges appear to be consistent with terrestrial compressional features that involve surface folding overlying blind thrust faults at depth. Wrinkle ridges are believed to accommodate small amounts of shortening on the order of 100 m or less. Larger ridges and scarps have also been identified on Mars.
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Clip from Huntingtower YouTube.com Amongst his contemporaries at the East Kilbride Rep Theatre was the actor John Hannah. Leaving acting behind, he studied geography and geology at Strathclyde University, graduating in 1986 with a first class honours Bachelor of Science degree. He obtained his doctorate, entitled "The evolution of neotectonic normal fault scarps in the Aegean Region" in 1990 at the University of Bristol on research into earthquakes in Greece and Turkey.
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An unusual area between lat 69° and 80° S. and long 30° and 60° consists of young, relatively smooth plains marked by many flat-topped ridges unlike any seen in other areas of Mercury. Scarps similar to Discovery Rupes (in the Discovery quadrangle adjacent to the north) are relatively common throughout the Bach region. The most common terrain units in the region are the plains units, which display a wide range of small-crater densities.
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Topography of Mauritania Mauritania is in the western region of the continent of Africa, and is generally flat, its 1,030,700 square kilometres forming vast, arid plains broken by occasional ridges and clifflike outcroppings. It borders the North Atlantic Ocean, between Senegal and Western Sahara, Mali and Algeria. It is considered part of both the Sahel and the Maghreb. A series of scarps face southwest, longitudinally bisecting these plains in the center of the country.
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The Paraiso Fault is concave to the east and shows an outstanding linear trace for more than . The fault is divided in two portions: the southern portion, about long, is located to the south of the Amaime River; the northern part extends about north of the river. Geographic expression suggests that the northern portion is more active than the southern one. The fault is characterised by a series of discontinuous short sinuous scarps of about long.
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As mentioned above, small patches of pure water ice with an albedo as high as 80% are found on the surface of Callisto, surrounded by much darker material. High-resolution Galileo images showed the bright patches to be predominately located on elevated surface features: crater rims, scarps, ridges and knobs. They are likely to be thin water frost deposits. Dark material usually lies in the lowlands surrounding and mantling bright features and appears to be smooth.
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8 The Sabana Formation, named after the Bogotá savanna were deposited in the Pleistocene paleolake Lake Humboldt, of which the many wetlands and the Bogotá River are the present-day remainders.Montoya & Reyes, 2005, p.72 The fault mainly cuts Cretaceous and Tertiary sedimentary rocks and, to some extent, early Quaternary deposits. The fault produces strong slope changes between different geologic units on both sides of the fault plane and displays degraded fault scarps,Paris et al.
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They were formed by endogenous forces (including uplift) and exogenous forces (including weathering and erosion).China Danxia The first studies on what are now referred to as Danxia landforms were conducted at Mount Danxia near Shaoguan, China. In the 1920s and 1930s Chinese geologists made an effort to learn more about these interesting geomorphic structures. Danxia landforms are made up of uplifted continental crust that has been faulted and eroded, exposing large scarps of layered rock, red in color.
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The trench was formed as soluble limestone, dolomite and gypsum dissolved forming potholes, funnels and caves that eventually collapsed. Today the trench features many scarps and offsets and generates long rain clouds caused by the air rising above it. There is a vernal lake in the south-west of the trench and a stream rising from a drilled well that disappears back into the ground within the trench. The trench is inhabited by mouflon, corsac, snakes, hares and vultures.
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The original scalloped margin dome: The Tick A scalloped margin dome is a type of volcanic dome, found on Venus, that has experienced collapse and mass wasting such as landslides on its perimeter. The margins of these domes have headscarps or 'scallops' separated by ridges that are a consequence of adjoining scallops. Sometimes debris or slumping can be found at the bottom of these scarps or scattered many tens of kilometers away. Many examples show no debris at all.
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Material obtained in drill cores includes chalk, chert, hyaloclastite, limestone, ooze and sandstone; basalt and chert outcrop in some places. In certain areas boulders and cobbles cover the seafloor; ferromanganese crusts cover exposed rocks. The seamount shows evidence of repeated mass failures; including hummocky terrain, scarps and slump blocks, which are on average thick. Landsliding is probably triggered by earthquakes; after the failure the landslides either stay coherent and do not travel far but some advance quickly and far.
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The Red Cones are cinder cones at the south end of the Mono–Inyo volcanic system. South of the Inyo volcanic chain are other features related to the dike system responsible for creating the craters, volcanoes and lava flows. These include a north–south trend of fault scarps up to high and pull-apart cracks or fissures in the earth. These fissures are not technically faults because little or no vertical or horizontal movement has occurred along them.
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Rembrandt basin is cross-cut by a large lobate scarp running from the southwest to the north, named Enterprise Rupes. It is about long and belongs to the global system of scarps, which covers the entire surface of Mercury. These features are thought to have resulted from the global contraction of the planet as its interior cooled. The scarp is the youngest tectonic feature observed in this region, because it cuts all other units including smooth plains.
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Extensive fill dirt was placed on the slope from the late 1950s to the early 1960s. This increased pressure on the soil below, turning what had been a dormant or slow slide into an accelerated one. Regrading of the hillside occurred afterward, after which significant slope instability began. Fault scarps (ranging in size from a few inches to several feet) exist at the top of the slope (where the slope meets the West Side Plateau) and along Franklin Avenue.
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Since about 2004, subsidence and the emergence of medium fault scarps have occurred along Riverbed Street to the water, indicating the failure of the toe of the slope (likely due to failure of 1950s-era bulkheads) and increased water in the soil. There is evidence that a failure plane exists about behind the surface of the hillside. A cross- section diagram of the Cuyahoga River and Irishtown Bend. The dashed green line shows where a stable slope would exist.
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Its surface consists of craters of a wide variety of sizes and morphologies, as well as plains units, fault scarps, and ridges. It includes three double-ring basins that range from 140 to 200 km in diameter: Bach (after which the region is named), Cervantes, and Bernini. Another large crater, Pushkin, is 240 km in diameter and occurs at the map boundary at latitude 65° S., longitude 25° . Both Bach and Bernini display extensive fields of secondary craters.
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The quarrying has destroyed the fort's defences on the north side of the hill, but they are elsewhere evidenced by two concentric scarps separated by a wide shelf. On the northeast side, a ridge line meets the fort, and was cut by a shallow ditch, which meets with a later boundary that runs around the base of the hill on the east side, and encloses a number of terraces on the lower slopes of the hill.
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Kargel and Pozio (1996) suggested that they might be fold belts, similar to North America's Appalachian Mountains. Recent images by the Cassini spacecraft show of Harran Sulci at much higher resolution than in the Voyager 2 images. The feature has a convex cross-section with numerous ridges running down the length of the feature. Like Samarkand Sulci, tall scarps facing the feature separate the surrounding cratered terrain to the north, and Diyar Planitia to the south, from Harran Sulci.
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Mapping of the features has suggested a total shrinkage of Mercury's radius in the range of ~1 to 7 km. Small-scale thrust fault scarps have been found, tens of meters in height and with lengths in the range of a few km, that appear to be less than 50 million years old, indicating that compression of the interior and consequent surface geological activity continue to the present. The Lunar Reconnaissance Orbiter discovered that similar small thrust faults exist on the Moon.
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The Ubehebe Craters are atop a fault that forms the edge of the Tin Mountain range; adjacent to the craters the fault has formed scarps. This fault is also known as the Tin Mountain fault, which cuts through Ubehebe Crater and branches out in a diffuse set of faults. This fault intersects the nearby Northern Death Valley fault close to the Ubehebe Craters; the latter fault may have ruptured at the same time or soon after an eruption in the volcanic field.
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In the west there is a widely dispersed group of oases in unconnected shallow depressions, the Kufra group, consisting of Tazerbo, Rebianae and Kufra. Aside from the scarps, the general flatness is only interrupted by a series of plateaus and massifs near the centre of the Libyan Desert, around the convergence of the Egyptian-Sudanese-Libyan borders. Slightly further to the south are the massifs of Arkenu, Uweinat, and Kissu. These granite mountains are ancient, having formed long before the sandstones surrounding them.
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The Georges River is popular for recreational activities such as water skiing and swimming. The banks of the river along the lower reaches are marked by large inlets and indentations overlooked by steep sandstone ridges and scarps, many being home to expensive residential properties. The Georges River features some artificial lakes in the suburb of Chipping Norton, near Liverpool. These lakes, known as the Chipping Norton Lakes, are the result of sand mining and quarrying operations in the twentieth century.
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The maximum elevation of Appledore is about 80 feet above sea level. The majority of the island has a metamorphic makeup, with gneiss being the most prevalent. The formation of the island is thought to be characterized by 5 major geological events, namely formation of the Rye Complex of Maine and New Hampshire, intrusion of diorites, Acadian orogeny, diabase dikes, and glaciation. Evidence of these events can be seen in glacial scarps, evidence of abrasion, presence of dikes, glacial plucking, and more.
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The gulf bottom surrounding the Corossol structure is characterized by a relict cuesta landscape consisting of partially eroded, gently inclined sedimentary rock layers that decreases southwards into a flat topography. The cuestas consist of steep northward-facing scarps and gentle southward-dipping slopes. Along its north side, the crater is truncated by a steep scarp of one of these cuestas and a wide and deep basin. Distinct long and wide streamlined glacial lineations cut across the southern half of the Corossol structure.
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A topographic image of the Sputnik Planitia basin, showing the rising scarps bordering the glacial plains. The banding is an artefact of the camera. On its northwest, Sputnik Planitia is bordered by a chaotic set of blocky mountains, the al-Idrisi Montes, which may have formed via the collapse of adjacent water ice highlands onto the planitia. On its southwest, the planitia is bordered by the Hillary Montes, rising above the surface, and, further south, the Norgay Montes, rising above the surface.
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The scenery and level of traffic changes upon leaving the Fallon area. The road narrows from four lanes to two and crosses remote terrain characterized by Basin and Range topography. The summits start out low and gradually increase in elevation. The features in the first basins include Labou Flat, a dry lake used by the US Navy for low-level flight operations, and Dixie Valley, with several visible fault scarps that resulted from the magnitude 7.1 Dixie Valley/Fairview earthquake in 1954.
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The surface of Lutetia is covered by numerous impact craters and intersected by fractures, scarps and grooves thought to be surface manifestations of internal fractures. On the imaged hemisphere of the asteroid there are a total of 350 craters with diameters ranging from 600 m to 55 km. The most heavily cratered surfaces (in Achaia region) have a crater retention age of about 3.6 ± 0.1 billion years. The surface of Lutetia has been divided into seven regions based on their geology.
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Map of Mauritania Location of Mauritania Topography of Mauritania Mauritania, a country in the western region of the continent of Africa, is generally flat, its 1,030,700 square kilometres forming vast, arid plains broken by occasional ridges and clifflike outcroppings. It borders the North Atlantic Ocean, between Senegal and Western Sahara, Mali and Algeria. It is considered part of both the Sahel and the Maghreb. A series of scarps face southwest, longitudinally bisecting these plains in the center of the country.
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Both types of mountains often have steep scarps along one or more margins. Only a handful of mountains on Io appear to have a volcanic origin. These mountains resemble small shield volcanoes, with steep slopes (6–7°) near a small, central caldera and shallow slopes along their margins. These volcanic mountains are often smaller than the average mountain on Io, averaging only 1 to 2 km (0.6 to 1.2 mi) in height and 40 to 60 km (25 to 37 mi) wide.
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In low sun-angle photography additional scarps and splays can be observed. The erosion/sedimentation patterns and the path of drainages such as Canyon Creek may have been influenced by movement along the fault, and topographic ridges are offset. Finally ductile folding, vegetation and landform variations have also been recognized on the Meers fault. In some rock formations faulting has mainly led to warping, instead of brittle displacements and in several sites evidence of faulting appears to be concealed by floodplain sedimentation.
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On the other hand, north–south extensional movements, yet unexplained, are pulling the plate apart, creating normal extensional faults and generating a parallel sequence of horsts and grabens, or rift valleys, running in a north–south direction. Mount Taygetus is a limestone horst bordering the Eurotas Rift Valley. Below its eastern face is the Sparta fault, a normal fault striking perpendicular to the direction of extension. Footwall scarps are visible on the eastern side of Taygetus at the base of its spurs.
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The East Vättern Scarp Landscape () Biosphere Reserve (established 2012) is a UNESCO Biosphere Reserve in Sweden. The reserve is a distinct example of the landscape in the central part of southern Sweden. The East Vättern Scarp Landscape contains many parallel fault scarps, most notably a steep western- facing precipice above the eastern border of Lake Vättern. This rugged landscape, cut by many small waterways, is dominated by agriculture and forestry lands, with villages and settlements consisting of small farms and individual homes.
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Summer in Maceió. The state's name originates with the lakes along its coast near the city of Maceió. The coast is bordered by fringing reefs and many fine beaches. Behind the beaches, sometimes only hundreds of meters and defined by steep scarps, lies a stretch of green coastal hills having enough rainfall for considerable agriculture and scarce remnants of the Mata Atlântica (Atlantic Rain Forest) that now is largely limited to steep hill tops or steep valley sides and bottoms.
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The Shropshire Hills are listed as Natural Area No. 42 and also as National Character Area 65 by Natural England, the UK Government's advisor on the natural environment. The NCA covers an area of and measure around from west to east and north to south. The dominant pattern of the hills is a series of southwest to northeast ridges, scarps and valleys. They are characterized by steep, rounded 'whaleback' hills, often crowned with open moorland, with woodland dressing the steeper slopes.
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Glacial valleys of Coropuna are up to deep and long. There are several collapse scarps on the mountain, especially around its central sector. A sector collapse took place on the southwestern flank and formed a landslide deposit as well as a horseshoe-shaped valley that was later filled by glaciers. Also on the southern side, mud-water flow deposits have been found in the Capiza River valley and appear to relate to Coropuna; at least eight such debris flows have been identified.
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This unit has a complex history of deposition; it was reworked in place and probably includes brecciated plutonic rocks and possibly ancient volcanic flows. Deposition of the intercrater plains material was waning as the next oldest basins (Dostoevskij, Tolstoj) were formed. Partly overlapping their formation was the deposition of the intermediate plains material, probably emplaced partly as distal basin ejecta and partly as volcanic flows. Regional deformation of these plains units by compressive tectonics, forming scarps, was contemporaneous with their deposition.
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The approximately enclosure was defended by rock scarps and steep slopes to the south and west with triple stone ramparts forming an arc on the other sides. Research by Historic England in 2016 using lidar proposed that the structure was instead "some form of non-defensive hilltop enclosure, possibly dating to the Late Bronze Age." Includes link to full report as .pdf Many plants are found on the crag, including horseshoe vetch near its northern limit, spindle tree and many ferns.
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Like all of Uranus' moons, Ariel probably formed from an accretion disc that surrounded the planet shortly after its formation, and, like other large moons, it is likely differentiated, with an inner core of rock surrounded by a mantle of ice. Ariel has a complex surface consisting of extensive cratered terrain cross-cut by a system of scarps, canyons, and ridges. The surface shows signs of more recent geological activity than other Uranian moons, most likely due to tidal heating.
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Cerro El Cóndor is a stratovolcano in Argentina. Cerro El Cóndor is a remote peak in the Argentine Puna de Atacama. As such it was probably the last major 6000m+ peak in the Andes to be climbed, with the summit reaching a height of . The volcano has the form of a massif (which covers a surface of ) constructed by two separate volcanoes; the older edifice forms parts of the northern and eastern flanks which are cut by scarps interpreted as caldera remnants.
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The Tucura Fault is located in the northern part of the Central Ranges of the Colombian Andes, west of the Romeral Fault System. It extends from the Paderisco River in the south to the Sinú Valley in the north, where it crosses the Serranía de Abibe. The fault crosscuts middle and upper Tertiary folded marine sedimentary rocks and Quaternary alluvial deposits. The fault controls drainage, forms linear ridges, topographic lineaments, and fault scarps about high on Quaternary terraces south of the town of Dabeiba, Antioquia.
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The massif itself may have originated in a similar manner to many other ocean core complexes. Lost City is a location dominated by steep cliffs to the south, chimneys, and mounds of carbonate material deposited from chimneys that collapse as they age. Breccia, gabbros, and peridotites are dominating rock types as one maneuvers away from the field, which are prone to mass wasting as the bathymetry steepens. Mass- wasting events of the past are evident by bountiful scarps on the slope of the massif.
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For example, the clays were relatively easily eroded and formed gentler gradients, whilst the harder sandstones or limestones were less susceptible to weathering and formed the steeper scarps. The resulting geological structures brought the various geological strata to the earth's surface where they could be easily observed and assessed. The most important strata are named after the geological periods of the Mesozoic era. These are, in order of their occurrence from west to east: Bunter sandstone, Muschelkalk, Keuper, Black Jura, Brown Jura and White Jura.
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Bunter sandstone occurs predominantly in the Northern Black Forest and has ensured the continued existence of large forested areas, because of the low productivity of its soils. Muschelkalk underlies the fertile Gäu landscapes of the Baar as far as Lower Franconia. The Keuper, with its relatively poor soils again, lends its name to the scarplands of the Keuper-Lias Uplands. The most prominent Jurassic scarps - notably the Swabian and Franconian Jura – are formed by the White Jura and, in the southwest, also the Brown Jura.
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At the high resolution achieved in some Galileo images the central part of Valhalla looks like a knobby terrain, where bright knobs are surrounded by dark smooth plains; there is noticeable deficit of small impact craters. The inner ridge and trough zone surrounds the central palimpsest. The ridges that immediately surround the central zone have steep flanks facing outward. These scarps, when studied at a high resolution, turned out to be discontinuous consisting of a series of small bright knobs surrounded by the smooth dark material.
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It is composed of relics of carbonatite intrusion, now appearing as carbonatite ring and subsided central part. The carbonatite ring is characterized by vertical scarps on inner side, with surface which often shows irregular knots, nodes, or veins of more resistant (silicate) material. Laterite covers are formed on both sides of carbonatite ring with accumulation of residual ferruginous-manganese minerals. Carbonatitic rocks are characterized by considerable variation, or great variety of textures, while the mineral composition is quite uniform and chiefly independent of texture.
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Strom and others interpreted most of these features to be surface expressions of thrust faults, and we can find no evidence within the Victoria quadrangle not already considered in their discussion. Because of their globally systematic orientations, these ridges and scarps have been associated with stresses developed by tidal despinning of Mercury. However, most trend approximately north-south and thus do not fit the pattern expected in the midlatitude belt, unless stresses from overall contraction were superposed on the stresses due to despinning.Melosh, 1977, figs.
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The lesser amount of intermediate plains material indicates decreasing plains formation, some localized within older basins. Scarps such as Vostok Rupes (in the Discovery quadrangle adjacent to the north) are apparently the expression of thrust faults; they suggest that planetary contraction may have stressed the lithosphere at about the time that c3 craters and smooth plains material were formed. Following core formation, lithospheric cooling and consequent contraction may have closed the conduits, restricting formation of plains material (Solomon, 1977). By c4 time, such formation was greatly reduced.
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Ita Mai Tai has a flat summit with a surface area of , and a slope break at about depth. Unconsolidated sediments cover the summit platform. There is evidence that the flat summit was a lagoon surrounded by a coral reef, and the volcanic basement forms an uplift in the central section of the flat summit. Volcanic cones form swells on the western part of the summit plateau of Ita Mai Tai, and structures such as domes, ridges, scarps, steps and terraces are dispersed all over the seamount.
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The arrival of explosive shells in the 19th century led to yet another stage in the evolution of fortification. Star forts did not fare well against the effects of high explosive and the intricate arrangements of bastions, flanking batteries and the carefully constructed lines of fire for the defending cannon could be rapidly disrupted by explosive shells. The ditch and counter scarp of Fort Delimara. Built in 1878, Delimara was built as a typical polygonal fort ditches and counter scarps made to be very deep, vertically sided, and cut directly into the rocks.
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USGS ShakeMap for the event The mainshock and the primary aftershock occurred on the previously mapped Roseau Fault, a , northeast-dipping normal fault that forms the western portion of the northwest-trending Les Saintes channel graben within the overriding North American Plate. Late 1990s bathymetric studies showed that it had vertical fault scarps approaching . The type of slip was primarily extensional, but included a small amount of left-lateral slip, and may have contributed to hydrological/volcanic effects that were observed on the island of Dominica, where a flooded fumarole drained twice.
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The second part, where the ice cap forms steep slopes at the boundary with the surrounding plain, is almost exclusively water ice. Finally, the ice cap is surrounded by permafrost fields that extend for tens of kilometres north away from the scarps. The centre of the permanent ice cap is not located at 90°S but rather approximately 150 kilometres north of the geographical south pole. The presence of two massive impact basins in the western hemisphere - Hellas Planitia and Argyre Planitia - creates an immobile area of low pressure over the permanent ice cap.
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The highlands of Kerala experience several types of landslides, of which debris flows are the most common. They are called 'Urul Pottall' in the local vernacular. The characteristic pattern of this phenomenon is the swift and sudden downslope movement of highly water saturated overburden containing a varied assemblage of debris material ranging in size from soil particles to boulders, destroying and carrying with it every thing that is lying in its path. The west facing Western Ghats scarps that runs the entire extent of the mountain system is the most prone physiographic unit for landslides.
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Galileo image of cratered plains, illustrating the pervasive local smoothing of Callisto's surface The ancient surface of Callisto is one of the most heavily cratered in the Solar System. In fact, the crater density is close to saturation: any new crater will tend to erase an older one. The large-scale geology is relatively simple; there are no large mountains on Callisto, volcanoes or other endogenic tectonic features. The impact craters and multi- ring structures—together with associated fractures, scarps and deposits—are the only large features to be found on the surface.
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Danube Planum as seen by Voyager 1 in March 1979 Danube Planum is a rifted mesa on the surface of Jupiter's moon Io. It is located on Io's trailing hemisphere at . Danube Planum is 244.22 kilometers across and 5.5 km tall. The mountain is bisected by a 15-to-25-kilometer-wide, northeast-southwest- trending canyon, splitting the mountain into two main east and west mountains, with several additional blocks at the southern end of the fracture. The outer margin of the plateau is marked by 2.6-to-3.4-km-tall scarps.
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They appear not to have progressed beyond trials.Adams, John: Mines of the Lake District Fells: Dalesman (1995) Looking north-west from the summit to the Coledale Fells. The mysterious Hackney Holes are now interpreted as the source of the largest 'rock slope failure' in the Lake District (1.3 sq. km.), where most of the Buttermere-Gatesgarthdale trough wall has deformed and bulged downslope, leaving open trenches (the Holes) or, across the Little Dale col, a chevron pattern of short steep scarps; midslope, there are bold antiscarps (uphill-facing scarplets), a classic indicator.
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The majority of the surface was covered in smooth, layered plains, with scarps marking the boundary between different layers. Even in the highest resolution images, no impact craters were observed, suggesting that Io's surface was being regularly renewed by the present-day volcanic activity. The encounter over one of Io's poles allowed Voyager 1 to directly sample the edge of the Io flux tube, finding an intense electric current of 5 amperes. The color data from Voyager's cameras showed that Ionian surface was dominated by sulfur and sulfur dioxide () frosts.
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Components of a scarp where the caprock slopes back from the rim, as is common Aerial view of retreating scarp in Namibia. A scarp is a line of cliffs that has usually been formed by faulting or erosion. If it is protected by a strong caprock, or if it contains vertical fractures, it may retain its steep profile as it retreats. Scarps in dry climates typically have a near-vertical upper face, that may account for 10% - 75% of the total height, with a talus-covered sloping rampart forming the lower section.
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Note also the presence of toilet facilities, which at the time of Vauban were still a privilege. Built on a six-hectare site, the Fort du Questel dominates the valley of Allégoet, a tributary of the Penfeld. This site is now part of a set of refurbished natural spaces that lead to the banks of the Penfeld by a track passing in front of the Cavale Blanche hospital. Onsite, the fortress offers walks through its sheltered green moat and its underground galleries, staircases, scarps and counterscarps, esplanade and fresh greenery nearby.
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Vegetation is slowly invading the fort. The tops of a few scarps remain visible, emerging from the ground, as well as a dame, a column of stone that prevented attackers from walking along the top of the enclosure. It isn't possible to visit the fort, but a few nonprofits have taken up residence in the only surviving building, the barracks, such as AS Caluire - Tir à l'arme de poing or AS Pétanque Caluire. The exterior of the fort has been transformed into green space; there is a skatepark nearby.
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Surveys near the epicentre revealed a surface rupture of about and numerous fault scarps, with general vertical displacements of ; a maximum displacement of occurred at the small village of Shionohira. Localised right-lateral slip of was observed at the subsiding west side of the rupture. The segments of the Idosawa Fault associated with this surface feature were classified as the "Shionohira Fault" in 2011. The nearby Yunodake Fault, a normal dip-slip fault northeast of the Shionohira Fault that had been dormant for 120,000–130,000 years, also ruptured during the quake.
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Geologists hypothesize that Puu Waawaa originally formed during a pumice eruption a little over 100,000 years ago, and has continued to build itself since then, with at least three distinct trachyte flows recognized. The eruptions, although partially covered by flows from Hualālai and Mauna Loa, have built a distinctive structure known as the Puu Anahulu ridge. The westward-facing flank of Hualālai forms a large underwater slump known as the North Kona slump. An area of about , the slump consists of an intricate formation of beaches and scarps below the waterline.
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A field fretty is composed of bendlets and bendlets-sinister or "scarps", interleaved over one another to give the impression of a trellis. Although almost invariably the bendlets and scarpes are of the same tincture, there is an example in which they are of two different metals. It is rare for the number of pieces of the fretty to be specified, though this is sometimes done in French blazon. The bendlets and bendlets sinister are very rarely anything other than straight, as in the arms of David Robert Wooten, in which they are raguly.
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The images revealed splotches, small areas whose reflectance is markedly different than that of the surrounding terrain, presumably from disruption of the surface by recent impacts. By September 2015, LROC had imaged nearly three-fourths of the lunar surface at high resolution, revealing more than 3,000 lobate scarps. Their global distribution and orientation suggests that the faults are created as the Moon shrinks, with influence by gravitational tidal forces from Earth. In March 2016, the LROC team reported the use of 14,092 NAC temporal pairs to discover over 47,000 new splotches on the Moon.
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Acacia pataczekii is native to the Australian island state of Tasmania with a limited range in pockets predominantly within the north east at altitudes between approx. 500–1400 m asl, however natural populations do occur in the Southern Midlands Region and also does well under cultivation at sea level. It naturally exists as a shrub layer, understory tree or as scattered individuals in moist gullies and flats, mountain summits, slopes and plateau scarps in low woodland to tall open, dry, wet and mixed Eucalyptus forests, most of which dominated by Eucalyptus delegatensis.
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Planimetrically arcuate escarpments in the Discovery quadrangle cut intercrater plains and crater materials as young as c4. These scarps are typically 100 to 400 km long and 0.5 to 1.0 km high, and they have convex- upward slopes in cross section that steepen from brink to base. More trend closer to north–south than to east–west. Discovery (lat 55° S., long 38° W.), Vostok (lat 38° S., long 20° W.), Adventure (lat 64° S., long 63° W.), and Resolution (lat 63° S., long 52° W.) Rupes are the most prominent examples in the quadrangle.
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The very smooth plains unit has virtually no visible small craters and displays smoother planar surfaces than those of the smooth plains unit. It occurs in the lowest areas within smooth plains material (including areas within buried crater depressions) and commonly within older craters. The areas of greatest concentration of smooth and very smooth plains materials also contain the most ridges, which suggests that ridges and the younger plains units are genetically related. Very smooth plains material for instance, commonly lies at the base of ridges or scarps.
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The regional geography developed during the Middle and Late Miocene, when basins and ranges were formed by thrusting and subsidence; the basins were filled with evaporites above older molasse-like material, while the ranges are mainly formed by Paleozoic rocks. Precambrian and Late Cretaceous rocks crop out in the Eastern Cordillera on the eastern margin of the Puna. The tectonic activity decreased about 9 million years ago, with the exception of a brief reactivation less than 4 million years ago. The present-day southern Puna is tectonically quiescent, although fault scarps indicate recent ground movements.
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It is separated from the flanking basins by fault scarps made of thick, high-density crust. It is made of thinned continental crust marked by the volcanism that occurred near the KT- boundary c. 66 Ma. The western coastal margin of the Indian subcontinent was affected by two large igneous provinces at 85 Ma and 65 Ma. This left a complex of ridges that run parallel to the west coast of which the Laccadive Ridge is the larger. A complex of considerably smaller ridges constitutes a northern extension to the CLR.
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A major feature within the caldera is Halemaʻumaʻu, a large pit crater and one of Kīlauea's most historically active eruption centers. The crater is approximately in diameter and deep, but its form has varied widely through its eruptive history; the floor of Halemaʻumaʻu is now mostly covered by flows from its 1974 eruption. Kīlauea has two rift zones radiating from its summit, one leading out to the east, the other long and trending towards the southwest. A series of fault scarps connecting the two rift zones form the Koa'e Fault Zone.
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Transport is also caused by glaciers as they flow, and on terrestrial surfaces under the influence of wind. Sediment transport due only to gravity can occur on sloping surfaces in general, including hillslopes, scarps, cliffs, and the continental shelf—continental slope boundary. Sediment transport is important in the fields of sedimentary geology, geomorphology, civil engineering and environmental engineering (see applications, below). Knowledge of sediment transport is most often used to determine whether erosion or deposition will occur, the magnitude of this erosion or deposition, and the time and distance over which it will occur.
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Penmoelallt is composed of a layer cake of rocks laid down during the Carboniferous period and subsequently tilted to the south into the South Wales Coalfield basin. Lowermost, and exposed along its northern and eastern scarps, are Carboniferous Limestones. Above these are the coarse sandstones of the Twrch sandstone (formerly the 'Basal Grit') of the Marros Group (former 'Millstone Grit Series') whilst the southernmost slopes are formed in the lowermost beds of the Lower South Wales Coal Measures. A couple of northwest to southeast aligned faults runs across the hill.
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It has been speculated that the hill may have been the site of a Bronze or Iron Age hill fort. Field investigations searching for a fort were made in 1966, but no evidence was found. The scarps which had been seen from the road and were thought to provide evidence of a man-made structure were found to be natural geological formations. There was also no sign of the cairn or pile of stones which had been described in the 18th century, but in 1975, Ralph Whitlock wrote of hilltop earthworks that were occupied in Iron Age times.
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The primary capability of TLS is the generation of high resolution 3D maps and images of surfaces and objects over scales of meters to kilometers with centimeter to sub-centimeter precision. Repeat TLS measurements allow the imaging and measurement of changes through time and in unprecedented detail, making TLS even more valuable for transformative science investigations. TLS is a powerful geodetic imaging tool ideal for supporting a wide spectrum of user applications in many different environments. Geoscience applications to date include detailed mapping of fault scarps, geologic outcrops, fault-surface roughness, frost polygons, lava lakes, dikes, fissures, glaciers, columnar joints and hillside drainages.
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The Banger joins from the left. The river then runs north–west in a narrow loop towards Jabalpur. Close to this city, after a fall of some (), called the Dhuandhara, the fall of mist, it flows for (), in a deep narrow channel through the magnesium limestone and basalt rocks called the Marble Rocks; from a width of about , above, it is compressed in this channel of (), only. Beyond this point up to its meeting the Arabian Sea, the Narmada enters three narrow valleys between the Vindhya scarps in the north and the Satpura range in the South.
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Mount Tchaikovsky () is a snow-covered mountain, rising to about 600 m, with scarps on the south and east sides, located in the north part of Derocher Peninsula, situated in the southwest portion of Alexander Island, Antarctica. A number of mountains in this vicinity first appear on maps by the Ronne Antarctic Research Expedition in 1947–48. This mountain, apparently one of these, was mapped from RARE air photos by Searle of the Falkland Islands Dependencies Survey in 1960. The feature was named by United Kingdom Antarctic Place-Names Committee after Peter Ilyitch Tchaikovsky (1840–93), Russian composer.
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The Arafura Swamp is a large and irregular floodplain surrounded by a low plateau in height, with prominent scarps to the east and west. The eastern scarp contains the Arafura Jungles site. It is laced with drainage channels and billabongs and forms a major flood-control and sedimentation basin for the Goyder-Glyde river system, with the main inflow coming from the Goyder and Gulbuwangay Rivers in the south, and with discharge northwards through the Glyde River into the Arafura Sea. It has a monsoonal tropical savanna climate with a mean annual rainfall of over , falling mostly from December to April.
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This is in contrast to other definitions of albedo such as the geometric albedo, which can be above 1. In general, though, the Bond albedo may be greater or smaller than the geometric albedo, depending on surface and atmospheric properties of the body in question. Surface features include the large southern polar cap, older cratered planes cross-cut by graben and scarps, as well as youthful features probably formed by endogenic processes like cryovolcanism. Voyager 2 observations revealed a number of active geysers within the polar cap heated by the Sun, which eject plumes to the height of up to 8 km.
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Her research determined which characteristics of riverscapes are valued by certain demographics of the population through a ratings system that determined factors of beauty. Morisawa furthered her research on watersheds and geomorphology, publishing the article Quantitative Geomorphology of Some Watersheds in the Appalachian Plateau. Her research included looking at the geologic structure of the watershed basins in the Appalachian Plateau, and how other interactions affect the streamflow and geomorphology of the basins. The stratigraphy or specifically sequence stratigraphy of basins include anticlines that have been eroded over time and the outer edges of the basin defined with steep scarps.
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The circumbasin scarps around Caloris, Tolstoj, and Mozart are the most prominent structural features in the quadrangle. The main Caloris Montes scarp is thought to approximate the edge of the basin of excavation of Caloris and is probably a structural and stratigraphic counterpart of the Montes Rook scarp around the Orientale Basin on the Moon. A subdued outer scarp is present around most of the visible part of Caloris, better seen in the Shakespeare quadrangle to the north. This scarp is generally coincident with the transition between the massifs of the Caloris Montes Formation and the lineated facies of the Van Eyck Formation.
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The sharpness of the single rim-scarp of Mozart reflects the youth (younger than the smooth plains) of this large impact. The position of Mozart at the west terminator of the Mariner 10 image data precludes visibility of its floor and thus hides any evidence of a possible central uplift or inner structural ring. Lobate scarps or ridges, which are best seen within the smooth plains material and vary locally within the intercrater plains material, are generally steep on one side and gently dipping on the other. Some, like the lunar mare ridges, appear to mark the outlines of subjacent craters.
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The depression is bounded by a zone of circumferential curvilinear structures interpreted to be graben and fault scarps. These structures are spaced 0.5–4 kilometers (0.3–2.5 miles) apart, are 0.6–4.0 kilometers (0.4–2.5 miles) in width and up to in length. Extending up to approximately in length from the southeast of the patera is a system of linear structures thought to represent a flanking rift zone along which the lateral injection and eruption of magma may have occurred. A shield edifice in diameter with a prominent central pit lies along the trend of one of these features.
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Bundelkhand lies between the Indo-Gangetic Plain to the north and the Vindhya Range to the south. It is a gently sloping upland, distinguished by barren hilly terrain with sparse vegetation, although it was historically forested. The plains of Bundelkhand are intersected by three mountain ranges, the Vindhya, Fauna and Bander chains, the highest elevation not exceeding 600 meters above sea-level. Beyond these ranges the country is further diversified by isolated hills rising abruptly from a common level, and presenting from their steep and nearly inaccessible scarps eligible sites for forts and strongholds of local kings.
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The Central Mountain Range extends from Su'ao in the northeast to Eluanbi at the southern tip of the island, forming a ridge of high mountains and serving as the island's principal watershed. The mountains are predominantly composed of hard rock formations resistant to weathering and erosion, although heavy rainfall has deeply scarred the sides with gorges and sharp valleys. The relative relief of the terrain is usually extensive, and the forest-clad mountains with their extreme ruggedness are almost impenetrable. The east side of the Central Mountain Range is the steepest mountain slope in Taiwan, with fault scarps ranging in height from .
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Topographic map of the Lennon-Picasso Basin The Lennon-Picasso Basin is an ancient (Pre-Tolstojan) impact basin on Mercury, discovered from topographic mapping of the surface by the MESSENGER spacecraft. It is approximately 1450 km in diameter and spans the region between Picasso crater on the north rim to Lennon crater on the south rim, and the crater Holst is near the center. The basin is heavily eroded by subsequent impacts and is not obvious on the surface. A topographic low is present near the center, and scarps representing a remnant of the eastern basin rim are intact.
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"Global tectonics of a despun planet." Icarus 31(2): 221–243. has shown analytically that the expected pattern of fracturing includes linear strike-slip faults oriented roughly N. 60° W. and N. 60° E., and a younger set of thrust faults with east–west throw and rough north–south trends. Melosh and Dzurisin have pointed out the similarity between this predicted tectonic pattern and that observed on Mercury, and they have proposed that the global system of lineaments and arcuate scarps, which is well developed in the Discovery quadrangle, formed in response to early, simultaneous planetary contraction and tidal despinning.
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Formation of intermediate and smooth plains materials may have been abetted by the c3 and c4 crater- and basin-forming events that opened up temporary magma conduits. One of the latest large impacts was the Caloris event, which occurred on the other side of the planet from the Discovery quadrangle and which may have initiated formation of the hilly and lineated material within it. Subsequent to formation of the smooth plains material, the Discovery quadrangle underwent minor tectonic adjustments that formed scarps on plains within craters. The very smooth plains unit was formed in some young craters.
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The ridges associated with the intermediate plains unit are best interpreted as tectonic in origin because they extend into adjacent exposures of intercrater plains material and, more significantly, because they transect ejecta, rims, and floors of craters. The ridges range in length from about 50 km to many hundreds of kilometers, are sinuous to lobate in plan, and generally trend about north-south. Most are asymmetric, with one slope steeper than the other, and at places they can be more logically referred to as rounded scarps. Commonly, an individual ridge changes along trend from symmetric ridge to asymmetric ridge to rounded scarp.
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The cratered plains material is relatively flat with broad ridges and lobate scarps that in places resemble those of some of the lunar maria. It is difficult to obtain reliable crater counts on this unit because many secondary craters cannot be distinguished from primary craters. Cratered plains materials embay craters in classes c1 to c3; they may represent lava flows extruded after an initial phase ofimpact flux. The albedo of the cratered plains is intermediate compared to that of other mercurian units, but higher than that of the lunar maria, and may reflect lower iron and titanium content.
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The tephra and ash from the Black Lapilli tuff by the caldera formed agglutinates around its rim. Newberry Volcano is cut by several fault scarps, small step offsets on the ground surface where one side of a fault has moved vertically with respect to the other. At the center of the isthmus that separates Newberry Volcano's two crater lakes is the central volcanic cone, named Central Pumice cone, which reaches above East Lake. With a broad, flat top, it formed during an explosive eruption about 7,000 years ago, and sits in the center of the caldera.
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Fogo consists of a single volcano, so the island is nearly round and about in diameter. The large summit caldera (about 10 kilometers in the north-south direction and 7 kilometers in the east-west direction) is not located in the center of the island, but rather towards its northeastern corner. The caldera is bounded by steep near-vertical fault scarps on the north, west, and south sides but is breached to the east where lava can flow to the coast. North-northeast-trending eruptive fissures opened along the western flank of Pico, which formed inside the caldera between about 1500 and 1760.
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This caused strong extensional stresses in the moon's crust reaching estimates of 30 MPa, which may have led to cracking. Some present-day scarps and canyons may be a result of this process, which lasted for about 200 million years. The initial accretional heating together with continued decay of radioactive elements and likely tidal heating may have led to melting of the ice if an antifreeze like ammonia (in the form of ammonia hydrate) or some salt was present. The melting may have led to the separation of ice from rocks and formation of a rocky core surrounded by an icy mantle.
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12m) at the SE. There are some large stones in situ in the interior of the site and traces of a boulder revetment at the base of the bank. Possibly a modified prehistoric kerbed cairn. (Price 1934, 46) The above description is derived from the published 'Archaeological Inventory of County Wicklow' (Dublin: Stationery Office, 1997). In certain instances the entries have been revised and updated in the light of recent research." below Cloghleagh Church,Record of Monuments and Places WI005-007: "Description: Situated on the SW extremity of a small natural promontory with short steep scarps on the N, S and W sides.
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Pen y Bryn in 1811, sepia drawing by Sir Richard Colt-Hoare The modern Garth Celyn is defined by the Royal Commission on the Ancient and Historical Monuments of Wales (RCAHMW) as a series of features, including the house Pen y Bryn itself, a large 'barn', and earthen terraces and scarps, collectively interpreted as an enclosure 90–100 metres across. The name "Garth Celyn" may be translated as "Holly Enclosure" or "Holly Hill" in Welsh. "Celyn" is also an element of local field names and of Hafod Celyn up the valley.A Brief Report on Pen y Bryn and Aber, Gwynedd.
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Devonian age rocks are broadly synonymous with the Old Red Sandstone (commonly referred to as ‘the ORS’) though the lowermost ORS is late Silurian in age. The Anglo-Welsh Basin which stretches from the border with England westwards through the Brecon Beacons National Park into Pembrokeshire includes the larger part of this sequence. It is the sandstones and mudstones of the Lower Devonian Brownstones and Senni Formations, sometimes capped by the hard wearing sandstones of the Plateau Beds which form such striking peaks as Pen y Fan and Sugar Loaf and the dramatic scarps of the Black Mountains and Black Mountain. There are restricted occurrences of Devonian rocks on Anglesey too.
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The southern end of the bridge was protected by a bridge-head that was overlooked by Fort Napoleon. Fort Napoleon was a strong fort, capable of holding 450 men and situated atop a hill above a steep embankment. It was not a difficult climb for any attacking troops, however, and entry into the fort was eased slightly by two large scarps, rather like steps, which led onto the fort's ramparts. The rear of the fort sloped down to the bridge-head and was protected by a palisaded ditch and loop-holed tower that would act as the last place of refuge should Hill's men gain entry into the fort.
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South polar vantage of Enceladus's anti-Saturn hemisphere, using a false color scheme in which fractured areas show up as blue terminator – north is up Voyager 2 was the first spacecraft to observe Enceladus's surface in detail, in August 1981. Examination of the resulting highest-resolution imagery revealed at least five different types of terrain, including several regions of cratered terrain, regions of smooth (young) terrain, and lanes of ridged terrain often bordering the smooth areas. In addition, extensive linear cracks and scarps were observed. Given the relative lack of craters on the smooth plains, these regions are probably less than a few hundred million years old.
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Color map and elevation map The Odysseus crater is now quite flat for its size of approximately 450 km or more precisely, its floor conforms to Tethys' spherical shape. This is most likely due to the viscous relaxation of the Tethyan icy crust over geologic time. The floor lies approximately 3 km below the mean radius, while its exterior rim is about 5 km above the mean radius—the relief of 6–9 km is not very high for such a large crater. Inside the crater the rim is composed of arcuate scarps and extends for about 100 km until the floor is reached.
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The La Plata or Chusma Fault extends across the eastern slope of the Central Ranges of the Colombian Andes, southeast of the city of Neiva in southwestern Colombia. The fault displaces Triassic, Jurassic and Cretaceous sedimentary rocks, as well as Tertiary volcanic rocks. Coalescent Quaternary alluvial fan deposits are offset by the La Plata Fault. The trace is characterised by old retreated and declined scarps, en-echelon semiparallel associated faults that cut alluvial deposits of the Páez River and local lahar deposits, a well developed topographic fault-line expression, and a probable pull-apart basin filled with Quaternary alluvial fans and alluvium near the town of La Plata.
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These two great areas of scarpland are linked in the south by the scarps of the Tafeljura on the High Rhine, as well as those in the region of Basle, the Ajoie and in the rest of the Belfort Gap. In the area of the Faltenjura, around the southern perimeter of the Upper Rhine Rift in the Sundgau (Pfirter Jura), the two scarplands (unfolded layers) are separated from one another by a short distance. The rock layers involved were formed in the Triassic und Jurassic periods of the Mesozoic era. The sedimentary beds were gently tilted and exposed to the surface and erosion and weathering occurred differentially based on their composition.
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The area was subject to repeated glaciation during the Quaternary period. Glacial till covers large parts of the landscape whilst recessional moraines occur within the major valleys of the Geopark and late-glacial moraines form striking features beneath the main north and north- east facing scarps of the mountains. Both moraines and glacial lakes are visible at the foot of the spectacular north face of the Black Mountain (range), especially Llyn y Fan Fach and Llyn y Fan Fawr below the summits of Picws Du and Fan Foel. Numerous landslips have occurred in the post-glacial period in both bedrock and superficial deposits, though these are no longer active.
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Echo Bank rises from the continental slope to a depth of about below sea level, making it the shallowest seamount in the region. It has a maximally wide flat top like a guyot at a depth of that is surmounted by volcanic cones which reach depths of and also by small depressions; the cones cluster in the central summit platform. Around the summit lie terraces and scarps, with the terraces particularly pronounced on the eastern side and perhaps reflecting a slight tilt of the seamount. The slopes of the seamount are steep and cut by curved slide scars and gullies which both reach lengths of .
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They thought that these fractures were later modified, and predicted that east-trending normal faults caused by tensional stresses would be found in the polar regions. In a later report, Pechmann and Melosh (1979, p. 243) stated that “the NE and NW trends become nearly N-S in the polar regions.” The northwest-trending component of the postulated global grid of fractures is markedly absent in the Borealis region. Northeast-trending scarps and troughs are conspicuous, however, across intercrater plains material and in crater fill (smooth plains material) between the 155° and 185° meridians, and from crater Van Dijck northward to crater Purcell and beyond.
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The size and density of these ghost craters suggest that, prior to emplacement of smooth plains material, the original heavily cratered surface of Borealis Planitia—which may have been the cratered floor of a very large multiring impact basin—and the cratered floor of the Goethe Basin were similar in composition and age to the intercrater plains material of the highlands to the west. Many scarps in Borealis Planitia are subconcentric to the rim of the Goethe Basin and have steeper slopes that face away from it, suggesting that they represent the fronts of lava flows that resurfaced extensive areas of heavily cratered terrain (intercrater or older plains material).
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The Van Eyck Formation is characterized by an extensive radial ridge-and-valley system with minor concentric scarps and lineaments. These features are considered for the most part as gouges and depositional plumes from secondary cratering within the Van Eyck; the remarkably straight ridges and steep walls, however, suggest formation by fracturing. Only a small part of the ridge and fracture system that characterizes the floor of Caloris is within the quadrangle. The ridges in the floor of Caloris, which are like those within the smooth plains, do not appear to be as complex as lunar mare ridges and are cut by numerous open grabenlike gashes.
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Some of these thermal features still discharge, with their presence evident as gas bubbles rising from the vents in the lake bed. Despite the loss of so many of its thermal features under the artificial lake, Orakei Korako remains the largest geyser field in New Zealand, with up to 35 active geysers. The most famous of these is the Diamond Geyser, whose unpredictable eruptions can last from a few minutes to many hours, ejecting boiling water as high as nine metres. The three terraces above the lakeside Emerald Terrace are great fault scarps formed by an earthquake in 131 AD, around the time when Lake Taupo (a supervolcano) was last erupting.
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The origin of the tsunami was thought to have been due to an underwater landslide triggered by an earthquake on the Dead Sea Transform itself. More recent analysis suggested that an offshore continuation of the Roum Fault mapped onshore was responsible. However, seabed surveys have discounted this possibility and the discovery of geologically recent fault scarps at seabed indicate that movement on the newly identified Mount Lebanon Thrust was the cause of the earthquake and the resulting tsunami. Quaternary uplift recorded by a series of marine-cut terraces between Tripoli and Beirut are consistent with continuing upward movement of the hanging wall of the proposed thrust.
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North and south of the FTFZ the axis of the MAR is near-perpendicular to the spreading direction and the spreading rate is 2.6 mm/yr. The axial valley south of the FTFZ is composed of short axial volcanic ridges separated by 8–18 km-long en echelon deeps, while north of the FTFZ the axial ridges are much longer and more linear. North and south of the FTFZ the ocean floor is relatively smooth with long abyssal hills, probably detachment faults, aligned near-parallel to the ridge axis. In contrast, close to the FTFZ the terrain is more rugged and adorned with short, oblique fault scarps.
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The morphology and structural relations of the scarps suggest that most result from thrust or reverse faults. However, an extrusive origin has been suggested by Dzurisin (1978) for a scarp more than 200 km long that extends from about lat 70° S. to the map border between long 45° and 52°; he based this interpretation on albedo differences between the two sides of the scarp and on partial burial of craters transected by it. Age relations among structural features are not readily apparent. In the Bach region, the youngest craters cut by a scarp are of c4 age; the oldest crater to superpose a scarp is a c3.
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Theoretical studies by Melosh (1977), based on observations recorded by Dzurisin (1978), suggested that tidal spin-down combined with core or lithospheric contraction could explain many of the tectonic features of Mercury. The scarps occurring in the polar regions do appear to be the result of thrust faulting, which substantiates the suggestion that contraction occurred concurrently with spin-down. Linear structures (other than some ridges) are thus interpreted to form as a result of these two active processes. Fracture and lineament patterns around the Caloris basin suggested to Pechmann and Melosh (1979) that Mercury's despinning period began before global contraction started and ended during the contraction's early phases.
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Subcrustal zones of tension may have allowed molten materials to reach the surface through fractures beneath craters, even during the period of global contraction (Solomon, 1977). Ridges of domical cross section cut some c4 craters and, at places, flank areas of young, very smooth plains material. Thus, possible volcanic extrusions associated with tectonic activity may have continued into the period of formation of c4 craters and the oldest very smooth plains material. The period of tectonic adjustment of the mercurian lithosphere lasted at least through the time of formation of smooth plains material; c4 craters that formed during this period are cut by scarps and are superposed on them.
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Thus the smooth plains unit may have a relatively wide age range. Like the cratered plains, it exhibits lobate scarps and few mare-like ridges, but these are generally smaller than those of the cratered plains and more nearly resemble those of the lunar maria. Although crater counts are more reliable because there are fewer secondaries than in the cratered plains, resolution is a serious constraint to developing crater counts on the relatively small tracts of smooth plains. Preliminary counts made on a few of the more extensive occurrences of smooth plains show a cumulative crater frequency of about 7.5 × 102/106 km2 for craters larger than approximately 2.5 km.
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During this period of deposition occurred the impacts of the last of the major basins (Beethoven, Michelangelo, Valmiki, and Bach). Minor tectonic activity continued as scarps andl lunar mare-type wrinkle ridges developed within the smooth plains materials. The cratering rate declined rapidly as the c3, c4 and c5 craters were produced. Regolith production continues to the present day on all units. If the geologic history of the Moon is a guide, most of the events discussed were essentially complete within the first 1.5 to 2.0 billion years of Mercury’s history (Murray and others, 1975). A summary of global mercurian geology may be found in Guest and O’Donnell (1977) and Strom.
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The seamount is located in the Greenland Sea-Norwegian Sea, west of due north from Jan Mayen Island and in between Norway and Greenland. Vesteris Seamount is an isolated volcanic seamount that reaches a depth of below sea level and with two summits that rise from a plateau at depth; it is likely that the summit once emerged from the sea. The summit area of the seamount is flat, probably due to wave erosion during the Weichselian glaciation, and sediment cover is scarce. Lava flows extend from the summit area to depths of almost , and sheet flows, scarps, pillow lavas, lava tubes and lava debris have been observed on the seamount.
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Alexa Bank rises to depths of , has an eastward elongated flat top and is long and wide, widening towards the west; such dimensions resemble these of Savaii and Upolu in Samoa. The flat top has some features of an atoll including a raised rim, and it may indeed once have been an atoll. The rim is surrounded by a narrow terrace and in turn encloses a much wider terrace, that surrounds the flat top at an average depth of . The northern and southern flanks are formed by steep scarps, with the eastern slope featuring a terrace at depth and the western slope extending as a long volcanic ridge.
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Axial Seamount is the most active volcanic site in the North Pacific. Study of magnetic delineations along the seamount have modeled the ridge's history up to 30 million years ago, and shown that growth has progressed mostly in the north, with some southward progression dating back 3.5 million years. The base of Axial Seamount is a long, low-lying plateau, and the eastern part of the seamount is defined by a series of linear scarps. Axial Seamount has two major volcanic rifts extending approximately north and south of its main summit, as well as several much smaller, ill-defined ones aligned in a roughly similar pattern.
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Mariner 10, the first probe to visit Mercury The first spacecraft to visit Mercury was NASA's (1974–1975). The spacecraft used the gravity of Venus to adjust its orbital velocity so that it could approach Mercury, making it both the first spacecraft to use this gravitational "slingshot" effect and the first NASA mission to visit multiple planets. provided the first close-up images of Mercury's surface, which immediately showed its heavily cratered nature, and revealed many other types of geological features, such as the giant scarps that were later ascribed to the effect of the planet shrinking slightly as its iron core cools. Unfortunately, the same face of the planet was lit at each of close approaches.
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The rocks are of the Devonian, in common with their companion peaks of the Brecon Beacons to the east. The area was glaciated during the ice ages and a number of fresh moraines are to be found beneath the spectacular north and east facing sandstone scarps in the north-east of the range, especially below Fan Hir. There are smaller moraines lying immediately below the cliffs of Waun Lefrith and Picws Du. Llyn y Fan Fawr, below Fan Brycheiniog in the Black Mountain The lakes below the escarpment of Llyn y Fan Fawr and Llyn y Fan Fach are also remnants of glacial action, having been created by other moraines blocking drainage by forming deep hollows below the cliffs.
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Europa-like surface with the Labtayt Sulci fractures at center and the Ebony and Cufa dorsa at lower left, imaged by Cassini on February 17, 2005 Voyager 2 found several types of tectonic features on Enceladus, including troughs, scarps, and belts of grooves and ridges. Results from Cassini suggest that tectonics is the dominant mode of deformation on Enceladus, including rifts, one of the more dramatic types of tectonic features that were noted. These canyons can be up to 200 km long, 5–10 km wide, and 1 km deep. Such features are geologically young, because they cut across other tectonic features and have sharp topographic relief with prominent outcrops along the cliff faces.
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A 2013 study proposed that a number of craters within Arabia Terra, including Eden Patera, Euphrates Patera, Siloe Patera, and possibly Semeykin crater, Ismenia Patera, Oxus Patera and Oxus Cavus, represent calderas formed by massive explosive volcanic eruptions (supervolcanoes) of Late Noachian to Early Hesperian age. Termed "plains-style caldera complexes", these very low relief volcanic features appear to be older than the large Hesperian-age shield volcanoes of Tharsis or Elysium. Eden Patera, for example, is an irregular, 55 by 85 km depression up to 1.8 km deep, surrounded by ridged basaltic plains. It contains three linked interior depressions, demarcated by arcuate scarps, that have terraces suggestive of lava lake drainage and faults suggestive of collapse.
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Ham Hill summit and war memorial seen from Stoke-sub-Hamdon To the south of Somerset there is an upland with a series of rolling valleys and scarps, from Penselwood in the east to the Blackdown Hills, another designated Area of Outstanding Natural Beauty, in the west. This is a geologically complex area of clays, limestone and marl. The honey-coloured limestone at Ham Hill (also known as Hamdon Hill) is particularly important to geologists because of the assemblages of fossils which it contains, the sedimentary features which it displays and the way it relates to other rocks of equivalent age in the close vicinity. It has been quarried since Roman times at least.
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Cerro Autana as other table-top mountains in the region is the remains of a large sandstone plateau that once covered the granite basement complex between the north border of the Amazon Basin and the Orinoco, between the Atlantic coast and the Rio Negro. The table-mountain topography is formed as water percolates along joints and bedding planes, the siliceous cement dissolves, quartzite disaggregates and large blocks collapse which accumulate in the foot of the scarps. The percolating water forms large and intricate cave systems, which frequently emerge in the scarp zone as high waterfalls.Briceño, Henry O. and Schubert, Carlos (1990), 'Geomorphology of the Gran Sabana, Guayana Shield, southeastern Venezuela', Geomorphology, 3 (2), 125-41.
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Because of the time period in which it struck, very little is known about the nature of the earthquake. However, its epicentre was almost certainly located somewhere in what is now Shanxi (山西) province, near the present-day towns of Hongdong (洪洞) and Zhaocheng (赵城). The earthquake likely occurred on the Taigu fault zone in Shanxi, and several scarps and uplifts of local faults were seen as evidence of this; the Taigu fault zone has not experienced any measurable activity since the 1303 earthquake. The magnitude was calculated by modern seismologists to be 8.0 on the moment magnitude scale, though it is impossible to say for sure due to lack of accurate geological data.
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Anticipating that Frederick would rely on his cavalry, the Russians effectively negated any successful cavalry charge by using fallen trees to break up the ground on the approaches. Saltykov had little concern about the extreme northwestern face of the ridge, which was steep and fronted by the marshy Elsbruch, but a few of the Austrian contingents faced northwest as a precaution. He expected Frederick to attack him from the west, from Frankfurt, and from the Frankfurt outer city. The Russians constructed redans and flèche to protect all the potentially weak points of their fortifications; they built glacis to cover the most shallow of the hills, and scarps and counterscarps to protect seemingly weak points.
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The Gorneşti culture, characterized by the occurrence of the so-called high-necked milk pots with two small protuberances pulled at the margin and drilled vertically, is a continuation of the [Româneşti] (featuring receptacles with bird bill protuberances and decorated with step or nettle incisions), in turn descended from the Tisa culture in the developed Neolithic period. The settlements of the neo-Eneolithic cultures were located on the low or high river terraces, on hilltops or hillspurs and consisted in several dwellings whose positions sometimes observed particular rules. Recent research has tended to focus on the defense systems (ditches and scarps) of these sites. The culture strata are thick and superposed forming at times regular tells.
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The 1934 M6.3 Excelsior Mountains earthquake and the 1986 Chalfant Valley event were several smaller earthquakes that have occurred within the gap, and both generated limited surface faulting and some surface cracking in the Volcanic Tableland, which was created .7 million years ago from a major volcanic eruption that also formed the Long Valley Caldera northwest of Bishop. An estimated 500 cubic kilometers of material (tephra) produced in the event covers the northern Owens Valley as a rocky landform. The surface of the layered plateau is known as Bishop Tuff and features fumarole mounds and hundreds of north-south oriented fault scarps, many of which are visible on topographic maps, via aerial photography, and satellite imagery.
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Noar Hill, one of the East Hampshire Hangers The East Hampshire Hangers are located in the English county of Hampshire and form a line of hills with steep scarps that marks the eastern edge of the Hampshire Downs and its boundary with the Western Weald, an area of rolling countryside east of Petersfield and Liss. The Hangers run from the area of Farnham to Petersfield, before swinging eastwards to take in the north-facing scarp of the South Downs. The main settlements of the area are the villages of Selborne, Hawkley and East Worldham. The name is derived from the "hangers": long, narrow remnants of ancient woodland clinging to the steep scarp slopes.
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The floor of Sveinsdóttir was later covered by the smooth plains material and deformed by wrinkle-ridges before the scarp appeared. More than long and one of the largest fault scarps on the planet, Beagle Rupes marks the surface expression of a large thrust fault believed to have formed as Mercury cooled and the entire planet shrank. Beagle Rupes crosscuts Sveinsdóttir crater and has uplifted the easternmost portion (right side portion) of the crater floor by almost a kilometer, indicating that most of the fault activity at Beagle Rupes occurred after the impact that created Sveinsdóttir. Crosscutting relationships such as this are used to understand the sequence in time of the different processes that have affected Mercury’s evolution.
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The seabed in general is composed mainly of very soft clays. The geologic features in this area include normal faults with northwest-southeast orientation, a system of exposed and buried reefs that cross the area from the northwest toward the southeast, gas pockets trapped in faults and shallow strata at different levels of depth, paleo-channels, abrupt erosional slopes and scarps associated with submarine debris flows and faulting. Several side scan sonar targets are interpreted as scattered small debris.Deiros, D. Sackett, D. Malavé, G , Study of the shallow geological conditions, seabed and its potential impact for the development of the exploitation of natural gas in the Venezuelan Plataforma Deltana Geophysical Congress, Caracas (2002).
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Donhead Hollow from Win Green The Blackmoor Vale and Vale of Wardour area is a natural region in the counties of Dorset, Somerset and Wiltshire in southern England. The region is listed as National Character Area 133 by Natural England, the UK Government's advisor on the natural environment. Its irregularly shaped area covers and runs from Batcombe in the southwest to Frome and Warminster in the northeast, and from Wincanton in the west to Compton Chamberlayne in the east. To the west are the Yeovil Scarplands, to the north are the Mendip Hills and Avon Vales, to the south and east are the scarps of the Dorset Downs and the West Wiltshire Downs.
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The topographical layout of the village is consistent with that of many of the small towns and villages of the region: a fertile valley surrounded by high volcanic scarps descending from the surrounding mesas. Sacramental records for the pueblo church at Abiquiu, Province of New Mexico, often referred to a settlement Nuestra Señora de Guadalupe de la Cueva. This hamlet probably served as the initial source of settlers that later formed the future village of La Cañada de La Madera approximately two miles due north of this site. At some point in time in the early 1900s the name of the village of La Cueva was changed to Cañada de La Madera.
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The Wealden Anticline. The Chalk outcrops across large parts of southern and eastern England and forms a significant number of the major physiographical features. Whilst it has been postulated that a chalk cover was laid down across just about all of England and Wales during Cretaceous times, subsequent uplift and erosion has resulted in it remaining only southeast of a line drawn roughly between The Wash and Lyme Bay in Dorset and eastwards from the scarps of the Lincolnshire and Yorkshire Wolds. Gentle folding of the Mesozoic rocks of this region during the Alpine orogeny has produced the London Basin and the Weald–Artois Anticline, the Hampshire Basin and the less gentle Purbeck-Wight monocline.
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The Swan coastal plain is characterised by a series of sand dune systems, the Quindalup dunes, the Spearwood dunes, and the Bassendean dunes, which run from west to east (in increasing age) from the coastline to the major faults which form the eastern boundary of the plain. The plain is bounded to the east by the Darling Scarp, to the north by a subsidiary fault running north-west from Bullsbrook, and to the south by the Collie-Naturaliste Scarp. The Pinjarra plain lies between the Bassendean dunes and the eastern scarps. Early work on all three dune systems considered them to have been formed at differing times by the deposition of sands carried by wind (aeolian and/or by river processes (fluviatile).
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By comparison, topographic maps of the Moon, Mars, and Venus have been conducted at resolution and the most remote land areas on Earth have been mapped at resolution. Data from the bathymetric survey revealed numerous subsea volcanoes and evidence of large submarine landslides with slide scarps—cliff faces at the top of the origin of the landslide—up to high and wide and debris fans more than long. Data from the bathymetric survey and underwater search may be used for oil, gas, and mineral exploration. Two features within the search area—Broken Ridge and the Kerguelen Plateau—potentially contain oil and gas deposits, while a field of manganese nodules—which also contain iron ore, nickel, copper, and cobalt—on the seafloor could also be exploited.
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This structure gives rise to a series of landscape features along its length, not least the steep northwest-facing scarps of the hills and ranges mentioned above. Indeed, the feature can be seen as a significant lineament in aerial and satellite views of Wales.British Geological Survey 1:50,000 map sheets 196 'Builth Wells', 212 'Llandovery', 213 'Brecon' and 230 'Ammanford' & accompanying sheet explanationsOrdnance Survey Explorer map OL12 'Brecon Beacons National Park: western area' The Steep Belt effectively marks the southeastern edge of the intensely folded region of the Caledonian Orogenic Belt in central Wales. A series of major folds and faults affect the Ordovician and Silurian rocks to its northwest whilst folding and faulting of the Devonian rocks to its southeast is much more subdued.
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A conspicuous high and – long fault scarp just north of the Wichita Mountains is noticeable on Google Earth; it has formed on the Holocene part of the fault and continues southeastwards in the form of more subtle scarps although it may not exactly coincide with the path of the fault. Because the scarp is not present along the entire length of the fault, it is subdivided in a southeastern section in Comanche County and a northwestern section in Kiowa County, with only the southeastern section featuring a scarp. The scarp marks the Holocene section of the fault. The Meers fault is the only Mid-Continent fault scarp and has been called the "finest" such scarp east of the Rocky Mountains.
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Five periods were postulated by Murray and others (1975) to constitute the history of Mercury’s surface: (1) accretion and differentiation; (2) terminal bombardment; (3) formation of the Caloris Basin; (4) flooding of that basin and other areas; and (5) light cratering on the smooth plains. Only the periods following accretion are directly interpretable within the Borealis region. Intercrater plains material, which may be a reworked and mixed aggregate of impact and volcanic deposits, was emplaced over a long period that extended past the creation of the Goethe Basin and many smaller basins and craters. The scarps and troughs that trend across intercrater plains material may indicate an early compressional episode that followed even earlier expansion and differentiation of the crust.
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Titania's surface is cut by a system of enormous canyons and scarps, the result of the expansion of its interior during the later stages of its evolution. Like all major moons of Uranus, Titania probably formed from an accretion disk which surrounded the planet just after its formation. Infrared spectroscopy conducted from 2001 to 2005 revealed the presence of water ice as well as frozen carbon dioxide on the surface of Titania, which in turn suggested that the moon may have a tenuous carbon dioxide atmosphere with a surface pressure of about 10 nanopascals (10−13 bar). Measurements during Titania's occultation of a star put an upper limit on the surface pressure of any possible atmosphere at 1–2 mPa (10–20 nbar).
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The vale lies along the eroded core of an anticline, a westward extension of the Mendip Axis, with a relatively thin covering of Mesozoic sediments folded upwards over an up-faulted horst of Palaeozoic rocks.Melville, R.V. & Freshney E.C. (4th Ed 1982), The Hampshire Basin and adjoining areas, British Regional Geology series, Institute of Geological Sciences, London: HMSO, p115 The floor of the vale is composed of Albian (Lower Cretaceous) beds of the Upper Greensand, exposed by removal of the overlying chalk. It is surrounded to the north and south by chalk scarps which close to the east near Burbage. There is also a small inlier of Greensand to the east at Shalbourne;Chilterns: Sheet 51N 02W Solid Geology, 1:250,000 Geological map series, British Geological Survey, Keyworth, 1991 this area drains northwards to the Kennet.
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On the other hand, the three smaller valleys between the large ones - Honopue, Honokea, and Honokane Iki - as well as the many smaller gulches which are not yet valleys, are deprived of groundwater by the orientation of the rift zone and its dikes. Without the large amount of water that is received by the bigger valleys, these valleys grow far more slowly. Due to its topography as essentially a flat crater floor surrounded by cones and fault scarps, the main caldera is affected relatively little by erosion from water. Most of Kohala's summit groundwater ends up in either Waipi'o or Honokane Nui; the enormous amount of water routed through these valleys results in a large amount of water erosion, which causes the valley walls to frequently collapse, accelerating valley development.
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Numerous sites running along the New River were examined including the twin reinforced concrete bridges in Brawley. Slumping of the foundations there resulted in severe damage, and occurred as a result of the 15 October main shock, though the Brawley earthquake's epicenter was nearby. At the Imperial County Dump, several instances of ground failure were observed in sedimentary deposits near the top of and parallel to the river bank, and other cracks were found in that area that were determined to be the result of differential settling. Farther north at the entrance to the Del Rio Country Club, scarplets were located west of Route 111, but undisturbed Pleistocene sedimentary layers likely indicated that the scarps were the result of local slumping in the roadcut and not the result of surface faulting.
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The Craven Fault System is the name applied by geologists to the group of crustal faults in the PenninesAitkenhead, N. et al 2002 British Regional geology: the Pennines and adjacent areas (4th Edn) British Geological Survey, Nottingham that form the southern edge of the Askrigg Block and which partly bounds the Craven Basin. Sections of the system's component faults which include the North, Middle and South Craven faults and the Feizor FaultBritish Geological Survey 1:50,000 scale geological map (England and Wales) sheet 60 Settle are evident at the surface in the form of degraded faults scarps where Carboniferous Limestone abuts millstone grit. The fault system is approximately coincident with the southwestern edge of the Yorkshire Dales National Park and the northeastern edge of the Bowland Fells. retreated ca.
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On the other hand, the wrinklelike sinuous ridge along the northeast border of the Goethe Basin, together with the outward-facing concentric scarps along its periphery, may represent the fronts of lava flows that are associated with the development of a structural moat between the basin fill and the wall. The latter interpretation supports the view that impact craters and basins on Mercury, as on the Moon (Schultz, 1977) and Mars, “have played a dominant role in controlling the surface expression of igneous activity” (Schultz and Glicken, 1979, p. 8033). Slow, long-lasting isostatic adjustment of the basin floor may have continued well after the emplacement of the basin fill, a structural situation similar to that of crater Posidonius on the Moon (Schaber and others, 1977, Schultz, 1977).
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The most prominent features within the plain itself are a pair of craters, similar in size to one another, known as Brontë (Mercurian crater) and Degas (crater). Brontë is the older of the two craters, and the impact that formed Degas has overlapped the edges of that older crater and spread a spray of rays across the southern regions of Sobkou Planitia and beyond. According to Peter Grego's book Venus and Mercury and how to observe them Sobkou Planitia is free of scarps, ridges, fractures and valleys. Its southeastern edge is bordered by the scarp Heemskerck Rupes (26N, 125W) which is about 300 km long which along part of the line of a very broad, bright swathe which is 1,000 km long and terminating just to the east of Chong Ch'ol (45N, 116W).
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The floor of the Fort Rock Basin is relatively flat at around 1,315 m (4,315 ft) throughout much of the basin, so the depths of the lake at each level were fairly consistent. The highest shoreline at 1,384 m (4,540 ft) is best seen at Fandango Canyon, but traces of beach sediments and wave-washed scarps have also been identified at Cougar Mountain and the southern end of the Connley Hills. The lake had an average depth of 70 meters (230 feet), with a maximum depth of 76 meters (250 feet) at the eastern edge of the basin. The Connley Hills and Buchgrass Butte formed two major islands. The next shoreline at 1,364–67 m (4,475–85 ft) is seen at only a few places in the Fort Rock Basin, such as Fandango Canyon and Cougar Mountain.
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The soil nailing technique applied to temporarily and/or permanently stabilise natural slopes and artificial scarps is based on a fundamental principle in construction engineering: mobilizing the intrinsic mechanical characteristics of the ground, such as cohesion and the angle of internal friction, so that the ground actively collaborates with the stabilisation work. Nailing, on a par with anchors, induces normal stress, thereby increasing friction and stability within the hillside. One nailing method is rapid response diffuse nailing: CLOUJET, where the nails are embedded in the ground by means of an expanded bulb obtained by means of injecting mortar at high pressure into the anchorage area. Drainage is important to the CLOUJET method since the hydraulic regime, considered in the form of pore-pressure applied normally to the fractured surfaces, directly influences the characteristics of the system.
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Lifted type block mountains have two steep sides exposing both sides scarps, leading to the horst and graben terrain seen in various parts of Europe including the Upper Rhine valley, a graben between two horsts - the Vosges mountains (in France) and the Black Forest (in Germany), and also the Rila - Rhodope Massif in Bulgaria, Southeast Europe, including the well defined horsts of Belasitsa (linear horst), Rila mountain (vaulted domed shaped horst) and Pirin mountain - a horst forming a massive anticline situated between the complex graben valleys of Struma and that of Mesta. Tilted type block mountains have one gently sloping side and one steep side with an exposed scarp, and are common in the Basin and Range region of the western United States. Example of graben is the basin of the Narmada River in India, between the Vindhya and Satpura horsts.
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Kieffer, H. H. (2003), Sixth International Conference on Mars, no. 3158. this 1 meter deep carbon dioxide (CO2) ice transition area—between the scarps of the thick polar ice layer and the permafrost—is where clusters of the apparent geyser systems are located. The seasonal frosting and defrosting of carbon dioxide ice results in the appearance of a number of features, such dark dune spots with spider-like rilles or channels below the ice, where spider-like radial channels are carved between the ground and the carbon dioxide ice, giving it an appearance of spider webs, then, pressure accumulating in their interior ejects gas and dark basaltic sand or dust, which is deposited on the ice surface and thus, forming dark dune spots. This process is rapid, observed happening in the space of a few days, weeks or months, a growth rate rather unusual in geology – especially for Mars.
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The archipelago of the Azores includes a rich and vast geodiversity, and an important geological heritage, comprising various locales of interest to the scientific and learning communities, in addition to its socio-economic importance to tourism. Due to it being an archipelago, the Azores Geopark is disperse: guaranteeing a representative geodiversity that characterizes the Azorean territory; manifesting in a history based on geological and active volcanism; with conservation strategies that are common; and based on a decentralized management structure with supports in all islands. Characteristic of the Azorean geological history is a range of diverse features that includes (but is not limited to) volcanoes, calderas, lakes, lava fields, fumaroles, hot springs and thermal waters, volcanic caves, fajãs, fault scarps and marine fossil deposits. Beyond this heritage, there are other values of reference in the archipelago, such as its rich biodiversity, architecture, culture and ethnography.
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The mounds and heightenings found along this bank serve as evidence of purposeful re-working, cultivation and enhancement. Just like the counterscarp, the trapezoidal central platform narrows from the south and widens from east to west. Only the western side of the central platform lacks a steeply defined edge to the moat ditch circuit; the ill-defined western edge could be caused by stock animals having using this side to access the water. Many marginal earthwork features are present on the central platform: scarps and banks which sub-divide the interior into quadrants, a raised rectangular terrace, a low rectangular mound with rounded corners (probably a building platform), along with more general evidence of buildings and sporadic evidence of hollowed track, the latter possibly pertaining to the moated enclosure's more recent function as an orchard, with the tracks representing the subsequent wear-and-tear the site would have received.
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The South German Scarplands run (from north(-northeast) to south(-southwest)) more or less between the southern Rhön, the Spessart, the Odenwald and the Black Forest in the west, the Franconian Jura in the east, the Swabian Jura to the southeast and the northeastern foothills of the Jura to the south. The wooded west and northwest-facing scarps drop sharply towards the Rhine Rift Valley and the Rhine-Main Plain, whilst the dip slopes fall comparatively gradually towards the (north-)east into the depressions beyond which lie the Thuringian Forest, Thuringian Highland, Franconian Forest, Fichtelgebirge, Upper Palatine Forest and Bavarian Forest. Similarly the Swabian and Franconian Jura descend quite gently towards the south(east) to the Danube valley, whilst the Swabian Jura, for example, drop very steeply to the north(-northwest) from the so-called Albtrauf - the top of the main scarp.Dickinson (1964), p 567.
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A prominent Fault system (Burnett Fault) runs approximately east-west just to the north of the village (an extension of the Newton fault,Geological Survey of Great Britain, 1:50,000 Geological Map sheet 265; Bristol), and the two rises on Burnett Hill (B3116) represent the eroded scarps of two branches of this fault. In contrast, the steady incline of the B3116 from Burnett south to the junction with the A39 represents the geological dip of the top of the Blue Lias. The steep slope marking the edge of the Chew Valley, immediately west of Burnett village, is an erosional scarp through the softer red and green shales of the Triassic Mercia Mudstone. The fields in the bottom of the valley, north of the Burnett Fault, are underlain by the Supra- Pennant Measures of the Carboniferous period, represented by the Pensford Syncline coal basin, which formed part of the Somerset coalfield.
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The processes leading to landslides were accelerated by anthropogenic disturbances such as deforestation since the early 18th century, terracing and obstruction of ephemeral streams and cultivation of crops lacking capability to add root cohesion in steep slopes. The events have become more destructive given the increasing vulnerability of population and property. Majority of mass movements have occurred in hill slopes >20° along the Western Ghats scarps, the only exception being the coastal cliffs. Studies conducted in the state indicates that prolonged and intense rainfall or more particularly a combination of the two and the resultant persistence and variations of pore pressure are the most important trigger of landslides.Kuriakose SL, Jetten VG, van Westen CJ, Sankar G & van Beek LPH, 2008, Pore Water Pressure as a Trigger of Shallow Landslides in the Western Ghats of Kerala, India: Some Preliminary Observations from an Experimental Catchment, Physical Geography 29(4) 374–386 , Retrieved on 12 January 2009.
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Fort Souville, located to the south of Fort Douaumont, played a most important role in Verdun's defences and was never taken by the Germans. As part of the Thiaumont-Fleury-Souville ridge it dominated the combat zone and for the Germans, possession of the Fort would have literally put Verdun in their sights. It was Captain Gustave de la Taille who built this fort and gave it the name of the Loiret village, Souville, in which his ancestor, Bertrand de la Taille, groom to the Lord of Souville, had been laid to rest in 1319. Fort Souville was 388 metres above sea level, the same altitude as Fort Douaumont, and built between 1875 and 1879 from limestone covered with 3-5m of earth. The ditches that surrounded it featured built-in scarps and counterscarps, flanked by caponniers armed with revolver cannons and 12 tonne breechblock cannons and in 1889, the whole thing was wrapped in barbed wire 30m thick.
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Rampart at Croft Ambrey The monument includes a small multivallate hillfort with an annexe containing a Romano- Celtic temple and a medieval warren of up to five pillow mounds on the summit of a prominent steeply sloping spur overlooking Yatton Marsh and the valley of a tributary to Allcock's Brook. The hillfort survives as a roughly triangular enclosure defined to the north by two scarps with a buried ditch: to the west by three rampart banks and a larger internal ditch and to the south by three rampart banks with two medial ditches and a wide internal ditch which may have been used to store water. There were two complex entrances which through time had 20 successive gateposts and were further enhanced with guardrooms, corridors and bridges of which the south western was the principal entrance and the north eastern was complex and inturned. The enclosure originally covered approximately 2.2ha, but this increased through time to 3.6ha and eventually a southern rectangular annexe was added.
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The Priest and Clerk sandstone rocks east of Cartington Hill, with the Simonside Hills in the distance The Northumberland Sandstone Hills are a major natural region that lies entirely within the English county of Northumberland. Their sandstone hills form distinctive skylines with generally level tops, northwest facing scarps and craggy outcrops offering exceptional views to the Cheviots further west. The Northumberland Sandstone Hills lie not far from the coast of Northumberland and the region is listed as National Character Area 2 by Natural England, the UK Government's advisor on the natural environment. The region covers an area of , beginning at Kyloe in the north and running in a strip roughly 10 to 15 kilometres wide and parallel to the coastal plain as far as Alnwick, where it changes direction to head southwest via Thrunton Wood, Rothbury Forest and Harwood Forest to the area of Throckington and the River Rede, passing over the highest peaks in the area, including Tosson Hill () in the Simonside Hills.
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On the central portion of the south flank of Kīlauea the thousand-foot high cliffs of the Hilina Pali and similar scarps were recognized as early as 1930 as headscarps resulting from slumping of the coast.. The Hilina Pali is the headscarp of the Hilina Slump, a type of landslide where a large and relatively intact block slips along a concave surface, dropping vertically at the head, with the toe often extending upward as well as outward, following . The Hilina Slump extends seaward from both ends of the Hilina Pali out to a depth of 5000 meters.As outlined by , figure 1, and the oblique map view of figure 19, available here. Whether this slump is shallow, or reaches down to the décollement that underlies the entire Kīlauea south flank, is still under debate.. With the discovery in the late 1980s that the entire south flank of Kīlauea is involved with submarine landslides the term "Hilina slump" has been applied by some scientists to the broader area.
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The Garlock Fault moves at a rate of between 2 and 11 mm a year, with an average slip of around 7 millimeters. While most of the fault is locked, certain segments have been shown to move by aseismic creep, which is motion without resulting earthquakes. The Garlock is not considered to be a particularly active fault, seldom producing any shaking detectable by humans, although it has been known to generate sympathetic seismic events when triggered by other earthquakes and in one instance by the removal of ground water. These events, as well as continuing microearthquake activity and the state of the scarps from previous ruptures, do indicate that the Garlock will produce another major quake at some point in the future. A study published in October 2019 in the journal Science indicated that a part of the Garlock fault slipped after being triggered by the series of earthquakes in the Ridgecrest area which occurred in July 2019.
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