"It represents sediments that were laid in ancient oceans, almost flat, and are essentially still that way today," he said—what he described as a "layercake" of rock that is regular and undeformed.
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This method is widely used for interfacial tension measurement between two liquids but care should be taken to make sure to keep the platinum ring undeformed.
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The North Orissa Craton comprises extensive banded iron formations, granite intrusives, and undeformed volcano-sedimentary assemblages belonging to the Archaean to-early Proterozoic times. They are followed by folded limestone-bearing rock formations of the Proterozoic age. The West Orissa Craton is underlain by occurrences of granites of the Archaean age and undeformed limestone-bearing platform sediments of the Proterozoic age. Small occurrences of Archaean banded iron formations and greenstones can also be found.
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Cleopatra is superimposed on the structures of Maxwell Montes and appears to be undeformed, indicating that Cleopatra is relatively young.Catalog Page for PIA00149 The crater is named after Egyptian queen Cleopatra VII.
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In igneous petrology, eutaxitic texture describes the layered or banded texture in some extrusive rock bodies. It is often caused by the compaction and flattening of glass shards and pumice fragments around undeformed crystals.
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Nitinol alloys exhibit two closely related and unique properties: the shape memory effect and superelasticity (also called pseudoelasticity). Shape memory is the ability of nitinol to undergo deformation at one temperature, stay in its deformed shape when the external force is removed, then recover its original, undeformed shape upon heating above its "transformation temperature". Superelasticity is the ability for the metal to undergo large deformations and immediately return to its undeformed shape upon removal of the external load. Nitinol can deform 10-30 times as much as ordinary metals and return to its original shape.
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The Southern foreland of the pyrenean orogen is the Ebro Basin or Ebro Foreland Basin. It can be divided into a Southern Folded Foreland section in the northeastern Catalan sector and a basically undeformed flat-lying main section taking up the rest. Like the Subpyrenean Zone in the north, the Southern Folded Foreland was also affected by the thrusting motions of the Sierras Marginales and their easterly representatives. The induced folding intensity decreases the farther one moves away from the thrust fronts until one reaches the undeformed Ebro Basin.
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Fig. 1 Imbricate fan in a thrust system with a basal décollement. The section below the décollement is undeformed basement rock. Above the décollement, deformation has occurred due to compression. A series of branching faults terminating at depth.
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The Torrens Hinge Zone is a transitional area between the relatively undeformed platform deposits of the Stuart Shelf and the deformed rocks of the central Adelaide Rift Complex. It runs along the western margin of the primary rift basin.
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The Stuart Shelf is a region of platform deposits on the western rift shoulder that overlies the Gawler Craton. It experienced deposition in the late Neoproterozoic after the Sturtian Glaciation during a period of marine transgression and remains relatively undeformed to this day.
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Its pyroclastic deposits are remnants of explosive volcanism. The oldest exposed rocks within the belt are fine to medium-grained basalts and andesites. Lava flow units range in thickness from to . Mafic agglomerate and breccia are relatively abundant, being either massive and undeformed, or sheared.
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It was determined that the deformation was minimal in the Eastern Belt by looking at dikes that had intruded the rocks which appeared to be mostly undeformed. These mostly undeformed dikes were dated using the K-Ar method and were determined to be between 169 and 209 Ma in age, which implies they were placed well before any deformation related to the Nevadan Orogeny would have occurred. As the age of these dikes are older than the deformation of the Nevadan Orogeny, it is evident that most of the deformation took place towards the western side of the Sierra Nevada, rather than in the eastern regions.
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Assumptions regarding the undeformed burrow and its geometric relationship cannot directly be determined, and only estimated. While it is common for Skolithos burrows to form normal to the deposition plane, this is not always true, in which case, the ideal, undeformed state can no longer be used as a reference orientation. Shallow depositional sediments are also susceptible to damage by erosion and tectonic stress forces, which can influence average measurements and geometric orientations. Since the rheological properties between the structure and the host rock are usually very similar, observations of the fossils are conducted with the assumption that they have deformed homogeneously, where the deformation forces are distributed evenly along the entire deformation zone.
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The bedrock is undeformed magmatic rock. The north part is an anorthositic massif. The south is granitoid orthopyroxene and an assemblage of granite and pegmatite. In the piedmont the rock is covered with a thin layer of glacial till less than thick, with areas of exposed rock on the hills and valley walls.
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A cross-section of this structure is provided, and the steeply dipping anticlines and synclines are characteristic of this type of structure. The interior of the granitic domes are mostly undeformed, however the margins and the greenstone belts are heavily deformed, and the metamorphic grade depends on the region's proximity to the dome-keel margins.
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Lavas of modern volcanoes, like Antuco, unconformbly overlies the formations and dykes associated to modern volcanoes intrude it. In some localities the formation is covered by moraines. The Cola de Zorro Formation is largely undeformed except from some minor tilting caused by block tectonics. The strata of Cola de Zorro Formation are sub-horizontal.
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Undeformed platy minerals such as micas and amphiboles align in a preferred orientation, and minerals such as quartz or calcite deform into a grain shape preferred orientation. Continuous cleavage is scale dependent, so a rock with a continuous cleavage on a microscopic level could show signs of spaced cleavage when observed on a macroscopic level.
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Three fragments of cotton blankets accompanied the mummy. The body showed evidence of perforations caused by cadaveric fauna. Remains of Coleoptera (Ancognatha and Phyllophaga) were identified and remains of the left lung have been described in the thoracic cavity. The cranium was undeformed and showed remains of straight black hair with signs it had been cut.
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The highest point in the watershed is in the north at . The bedrock of the southern half of the watershed is relatively undeformed migmatite, a magmatic rock. The northern half has metamorphic rocks of magmatic and sedimentary origin, such as gneisses and paragneisses. The plateau and hills generally have thin soil with large areas of rocky outcroppings.
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Orogenic wedge including Foreland basin Foreland basins are flexural depressions created by large fold thrust sheets that form toward the undeformed continental crust. They form as an isostatic response to an orogenic load. Basin growth is controlled by load migration and corresponding sedimentation rates. The broader a basin is, the greater the subsidence is in magnitude.
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Molasse-type sediments were deposited on the Superior Province margin in the third cycle during this period. # Undeformed and likely post-tectonic small intrusions of monzonite occurred in the Labrador Trough around 1.81 Ga. # The hinterland near Kuujjuaq is characterized by pegmatite intrusion and hydrothermal activity followed by a cooling period from 1.77 to 1.74 Ga.
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Within the Tengiz Basin, deposits are never more than two kilometers thick and grow thicker to the south. The Chu Basin is filled with undeformed Middle Devonian through Permian red molasse and carbonate deposits. Calc- alkaline magmatism was extensive in the southeast Kazakh Uplands and the Tien Shan Mountains. Geologists have recognized these rocks through magnetic anomalies, drillholes and occasional outcrops.
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Sedimentary rocks cover around 15% of Hong Kong land surface. They are formed by deposition of sediments such as sand, mud, skeletons of marine species and pebbles, etc. As more and more sediments were deposited in layers, older layers are compressed by weight of younger layers above, eventually hardened and become sedimentary rocks. Undeformed sedimentary rocks always form horizontal layers.
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The most common rock type is monzogranite with biotite and an igneous texture that is equigranular but varies from coarse grained to porphyritic. The emplacement of plutons occurred in the Middle to Late Devonian period. Contact aureoles for the batholith are, contrary to other batholiths, largely undeformed. The relation of the magmatic episode represented by the Cerro Aspero Batholith to the Famatinian orogeny is not fully understood.
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Upon application of a constant stress, the material deforms at a decreasing rate, asymptotically approaching the steady-state strain. When the stress is released, the material gradually relaxes to its undeformed state. At constant stress (creep), the model is quite realistic as it predicts strain to tend to σ/E as time continues to infinity. Similar to the Maxwell model, the Kelvin–Voigt model also has limitations.
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Much of the Gulf of Mexico subsurface is dominated by relatively horizontal and undeformed salt that has advanced basinward ahead of continental shelf tectonic activity. The southern front of this salt is rimmed by thrust faults as a result of this movement, forming the Sigsbee Escarpment, a 1250-meter change in bathymetry. The salt in this region has stopped advancing recently during the Quaternary.
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Bending of an edge-clamped circular plate under the action of a transverse pressure. The left half of the plate shows the deformed shape, while the right half shows the undeformed shape. This calculation was performed using Ansys. Bending of plates, or plate bending, refers to the deflection of a plate perpendicular to the plane of the plate under the action of external forces and moments.
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The Spawning Lake Stock is an Archean age granitoid stock in Northeastern Ontario, Canada, located in Briggs Township and Chambers Township of Temagami. It intrudes through the Tetapaga Syncline, a major geologic fold in the Temagami Greenstone Belt. However, it remains undeformed by strain associated with the formation of the fold. The stock is intruded by dikes composed of biotite lamprophyre on its outer margins.
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Allometric measurements on the bony labyrinth of BAC-208, a fragmentary cranium that preserves a complete, undeformed petrosal bone suggest that Oreopithecus moved with agility comparable to extant great apes. Its anterior and lateral semicircular canal sizes fall within the range for great apes. Its relatively large posterior arc implies that Oreopithecus was more proficient at stabilizing angular head motion along the sagittal plane.
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The rectococcygeal muscles are two bands of smooth muscle tissue arising from the 2nd and 3rd coccygeal vertebrae, and passing downward and forward to blend with the rectal longitudinal smooth muscle fibers on the posterior wall of the anal canal.Wu Y, Dabhoiwala NF, Hagoort J, et al. 3D Topography of the Young Adult Anal Sphincter Complex Reconstructed from Undeformed Serial Anatomical Sections. Souglakos J, ed.
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The Mint Wash Granodiorite consists of medium to coarse-grained, weakly to strongly porphyritic granite with phenocrysts of gray to pink potassium feldspar up to in length and as much as eight percent biotite that is less than in size. This granite grades laterally into a fine grained, equigranular leucogranite with less than two percent biotite that is less than in size. The Mint Wash Granodiorite is almost everywhere undeformed.
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The scenario described above (cooling austenite to form martensite, deforming the martensite, then heating to revert to austenite, thus returning the original, undeformed shape) is known as the thermal shape memory effect. To fix the original "parent shape," the alloy must be held in position and heated to about . This process is usually called shape setting. A second effect, called superelasticity or pseudoelasticity, is also observed in nitinol.
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The Archean and Proterozoic strata are intruded by a number of mafic and ultramafic intrusions, which define the current outline of the Nipigon Embayment. They consist of relatively flat-lying and undeformed diabase sills known as the Nipigon diabase sills. These sills range in thickness from a few meters to thick in cliff sections to more than thick in drill core. They are estimated to cover an area in excess of .
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In continuum mechanics, the finite strain theory—also called large strain theory, or large deformation theory—deals with deformations in which strains and/or rotations are large enough to invalidate assumptions inherent in infinitesimal strain theory. In this case, the undeformed and deformed configurations of the continuum are significantly different, requiring a clear distinction between them. This is commonly the case with elastomers, plastically-deforming materials and other fluids and biological soft tissue.
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This section of the fault system is formed by the locally named Córdoba and Navarco Faults, which are eastern strands of the Romeral Fault System, south of the city of Armenia. These faults lie within the epicentre area of the Armenia earthquake of January 25, 1999. The faults extend through sheared cataclastic and undeformed basaltic and sedimentary Cretaceous oceanic rocks, cropping out on the eastern slope of the Central Ranges.Paris et al.
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The strong lithosphere of the indenter remains relatively undeformed and its boundaries are preserved, while the host allows deformation by lateral movement of crust both along the contact with the indenter and within the host. The indenter block is too buoyant to subduct, so crustal accommodation is achieved by either shallow underthrusting and crustal thickening, or formation and later lateral displacement of several microplates. It is possible to have a combination of the two models.
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Meridiani Planum, the part of Mars where this meteorite was found, is suspected to have once been covered by a layer of material with a thickness of as much as which has been subsequently eroded. However no evidence suggests when it impacted. To survive impact largely undeformed it must have impacted at less than ~1.5 km/s. which sets boundaries on its entry dynamics and Mars' atmosphere at the time it impacted.
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The only exception is gneiss overlain by metasedimentary and metavolcanic rocks in the southeast, which were recrystallized and metamorphosed during 1.42 billion year old orogeny. A major anorthosite- adamellite pluton intrudes the province. South of the Davis Inlet, the Hopedale Gneiss is the defining rock unit. Nain Archean gneiss is overlain to the north of the community of Nain, Newfoundland and Labrador by the undeformed Ramah Group shale, sandstone and quartzite from the Aphebian.
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Starting in 1958 U. S. Navy submarines collected upward-looking sonar profiles, for navigation and defense, and converted the information into estimates of ice thickness. Data from U. S. and Royal Navy submarines available from the NSIDC includes maps showing submarine tracks. Data are provided as ice draft profiles and as statistics derived from the profile data. Statistics files include information concerning ice draft characteristics, keels, level ice, leads, undeformed and deformed ice.
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The Aravalli Range, seen from the range's highest point at Guru Shikhar, in Rajasthan. The Indian Craton includes five major cratons. Cratons are part of continental crust made up of upper layer called platforms and older bottom layer called basement rocks. shields are part of a craton where basement rock crops out at the surface and it is the relatively oldest and most stable part that are undeformed by the plate tectonics.
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The penetration of the India into Eurasia reactivated the suture zone (which is located in the middle of the Tibetan Plateau), causing northward movement of both thrust faults and strike-slip faults. Strike-slip faults were responsible for moving mostly undeformed continental blocks eastward, away from the main convergent zone. Cross section depicting the tectonic evolution of the Bangong suture zone. 1. An oceanic backarc basin forms separating the Amdo basement from the Qiangtang terrane.
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Early to Late Proterozoic(2.5 to 0.54 billion years) calcareous and arenaceous deposits, which correspond to humid and semi-arid climatic regimes, were deposited the Cuddapah and Vindhyan basins. These basins which border or lie within the existing crystalline basement, were uplifted during the Cambrian (500 Ma (ICS 2004)). The sediments are generally undeformed and have in many places preserved their original horizontal stratification. The Vindhyans are believed to have been deposited between ~1700 and 650 Ma (ICS 2004).
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The Great Dyke acts as a strain-marker for the craton: The fact that it has been undeformed since intrusion (excluding the Musengezi area) shows that the craton had stabilised by the time the Dyke intruded.Dirks, P.H.G.M. and Jesma, H.A. 2002. Crust–mantle decoupling and the growth of the Archaean Zimbabwe craton. Journal of African Earth Sciences, 34, 157–166 Two mafic dykes, the East and Umvimeela, flank the Great Dyke to the east and west respectively.
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These are late Archean in age and are not associated with greenstone belts. They are relatively undeformed and form extensive topographic plateaus, such as the Hamersley Range.MacLeod, W. N. (1966) The geology and iron deposits of the Hamersley Range area. Bulletin (Geological Survey of Western Australia), No. 117 The banded iron formations here were deposited from 2470 to 2450 Ma and are the thickest and most extensive in the world, with a maximum thickness in excess of .
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It is most common for analysts in solid mechanics to use linear material models, due to ease of computation. However, real materials often exhibit non-linear behavior. As new materials are used and old ones are pushed to their limits, non-linear material models are becoming more common. These are basic models that describe how a solid responds to an applied stress: # Elasticity – When an applied stress is removed, the material returns to its undeformed state.
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The Eurekan orogeny terminated when seafloor spreading in the Labrador Sea ceased about 33 million years ago during the Oligocene epoch. Erosion of the orogenic mountains followed, resulting in the deposition of undeformed sediment above the eroded remnants of deformed rock. At least some of the coarse clastic sediments in the Beaufort Formation were derived from the Grantland Mountains and Princess Margaret Range, suggesting that these ranges had higher elevations during the Late Miocene or Early Pliocene times.
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Nonspecific endonucleases involved in DNA repair can scan DNA for target sequences or damage. Such a nuclease diffuses along DNA until it encounters a target, upon which the residues of its active site interact with the chemical groups of the DNA. In the case of endonucleases such as EcoRV, BamHI, and PvuII, this nonspecific binding involves electrostatic interactions between minimal surface area of the protein and the DNA. This weak association leaves the overall shape of the DNA undeformed, remaining in B-form.
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The Spawning Lake Stock in Briggs and Chambers townships contains megacrysts that reach to in diameter. It shears through the nearby fold axis of the Tetapaga Syncline, but remains undeformed by the western expression of the Net Lake-Vermilion Lake Deformation Zone. To the north and northeast, the massive Chambers-Strathy Batholith was formed during one magmatic event. It consists of intrusive rocks ranging from pink to grey quartz monzonite to granodiorite and intrudes metamorphosed volcanic rocks of the TGB.
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The Lishan Fault separates the Hsuehshan Range terrane Eocene to Oligocene sandstone and shale. The Chukou Fault (觸口斷層) provides the boundary for the Western Foothills terrane, which is shallow marine detritus from Miocene to Pleistocene. A deformation front forms the boundary with the undeformed coastal plains alluvium, which is still depositing. The Eastern Central Range terrane can be divided into the Tailuko belt on the west with greenschist metamorphism and the Yuli belt on the east with blueschist metamorphism.
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ShakeMap of the 1999 Armenia earthquake The fault section is formed by the Córdoba and Navarco Faults, which are eastern strands of Romeral Fault System, south of the city of Armenia. These faults lie within the epicenter area of the Armenia earthquake of January 25, 1999. The faults extend through sheared cataclastic and undeformed basaltic and sedimentary Cretaceous oceanic rocks, cropping out on the eastern slope of the Central Ranges of Colombia. It separates the Córdoba Complex from the Quebradagrande Complex.
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Barreirosuchus is known only from the holotype specimen MPMA-04-0012/00, an undeformed posterior portion of the skull with six teeth and a series of four vertebrae, two dorsal and two sacral. It was found 4 km from Monte Alto County, in the escarpment of the Serra do Jabuticabal, in the rural area of Monte Alto, São Paulo. It was collected from the Adamantina Formation of the Bauru Basin, which dates to the Turonian and Santonian stages of the Late Cretaceous.
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Measures of strain are often expressed in parts per million or microstrains. The true shear strain is defined as the change in the angle (in radians) between two material line elements initially perpendicular to each other in the undeformed or initial configuration. The engineering shear strain is defined as the tangent of that angle, and is equal to the length of deformation at its maximum divided by the perpendicular length in the plane of force application which sometimes makes it easier to calculate.
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The Taranaki Basin lies on the West coast of the North Island of New Zealand in the Taranaki Region, and is approximately 400 km west of the current Pacific-Australian plate boundary. It covers approximately 100,000 km2 and contains up to 9 km in sediment. The basin is divided into two main components, the Western Platform and Eastern Mobile Belt, formerly known as the Taranaki Graben. The Western Platform is a relatively undeformed, stable block compared to the Eastern Mobile Belt.
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Himalayan deformation was previously thought to stop at the foot of the Himalaya, or the northern boundary of the foreland basin (the Main Frontal Thrust). The Himalayan foreland basin was thus thought to be undeformed. Himalayan deformation has been shown to extend into the subsurface of the foreland basin, in the form of blind thrust faults, and strike-slip faults. These faults reach over 37 km south of the Main Frontal Thrust, and are responsible for several modern-day topographic highs.
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In the west, the hanging wall block of Dauki fault meets the non-folded, undeformed, near horizontal sedimentaries of Sylhet trough of Neogene. It is proposed that the Sylhet sediments were deposited in a pull-apart basin in the releasing bend of Dauki fault during the dextral strike slip movement. Thus the net slip for Dauki fault involves a vertical component and a dextral strike slip component (oblique-slip fault).V. Srinivasan (2005), The Dauki fault in Northeast India: Through remote sensing.
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Rove formation represented by prv The upper sedimentary layer is the 1,800- to 1,600-million- year-old Rove Formation. The seas and laid down the shales, slates and mudstones of the Rove Formation. Because the formation is on the northern part of the Animikie Basin these rocks escaped the crustal deformation from the Penokean orogeny that characterizes the equivalent strata of the Thomson Formation; this left the Rove Formation unmetamorphosed and lying flat. These are some of the oldest undeformed and unmetamorphosed sedimentary rocks in North America.
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The deformation caused by the hardened ball increases with the magnitude of the force pressing against it. If the force on it is small, when the force is released both the ball and plate's surface will return to their original, undeformed shape. In this case, the stresses in the plate are always less than the yield strength of the material, so the deformation is purely elastic. Since it was given that the flat plate is softer than the ball, the plate's surface will always deform more.
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Schematic of friction stir processing. The processed metal is subjected to high strain that modifies its dendrite (grain) pattern – the dendrites are smaller and more round in the nugget zone than in the undeformed regions. Friction stir processing (FSP) is a method of changing the properties of a metal through intense, localized plastic deformation. This deformation is produced by forcibly inserting a non-consumable tool into the workpiece, and revolving the tool in a stirring motion as it is pushed laterally through the workpiece.
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This led to obduction of ophiolites on the northern margin of the Lhasa terrane This period of obduction is generally accepted to mark the end of oceanic subduction beneath southern Qiangtang and the onset of Lhasa-Qiangtang collision. An important feature of the Bangong suture is the Amdo basement. This exposure of pre-Mesozoic crystalline basement is ~100 km long and ~50 km wide. Geology of the Amdo records Mesozoic metamorphism, magmatism, and exhumation and is composed of orthogneisses and metasediments which are intruded by undeformed granitoids.
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These strata unconformably overlie Archean strata of the Superior craton and Proterozoic Richmond Group. The unconformity between the Early Proterozoic Nastapoka Group and the underlying Archean Superior craton lies just inland of Nastapoka arc as defined by the edge of arcuate eastern coastline of Hudson Bay. The unconformity consists of undeformed stromatolite-bearing dolomites overlying either foliated Archean granodiorite or the tilted and eroded strata of the Richmond Gulf Group. A thin, conglomeratic quartz sandstone separates the dolomites from the underlying strata and forms the base of the Nastapoka Group.
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The Cimitarra Fault splays from the Palestina Fault in a northeasterly direction on the eastern border of the Central Ranges of the Colombian Andes, passes north of Barrancabermeja,Paris et al., 2000b and possibly connects to the Bucaramanga-Santa Marta Fault in the northeast.Plancha 5-06, 2015 The fault displaces Jurassic to Cretaceous volcanic rocks, Mesozoic igneous rocks, a Tertiary erosion surface in the Central Ranges, and late Quaternary sediments. Portions of the fault are pre-Pliocene in age, since it is locally covered by undeformed Pliocene sediments.
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The timing of when this folding occurred is debated, and the driving force is not fully understood. Some geologists relate the deformation of the Jabal Hafit anticline to the early Miocene Zagros Collision, which is currently active and is caused by the Arabian Plate colliding with the Eurasian Plate. However, the Jabal Hafit Anticline is not actively deforming, and undeformed Miocene sedimentary rocks around the anticline indicate that no deformation has occurred recently. Sedimentary evidence indicates that the Hafit structure developed during the late Oligocene to early–middle Miocene.
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Yet Lorence G. Collins does not agree with the assumption of the K-feldspar being primary magmatic and the myrmekite being formed due to deformation-induced Na-Ca-metasomatism. His sampling beyond the shear zone revealed an undeformed, felsic biotite diorite whose primary plagioclase was being replaced from the inside out by K-feldspar due to K-metasomatism. The deformations were therefore more or less continuous and had not only affected the shear zone but also the older plutonic country rocks, thence bringing about a metasomatic change in mineralogy.
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In a continental collision, a subducting tectonic plate pushes on the plate above it, making the rock fold, often to the point where thrust faults form, and a mountain chain rises. On the upper plate, the land between the mountains and the undeformed continent bends downward, forming a foreland basin. If the basin forms slowly, as in the northern Appalachians, it fills with shallow-water sediments. If it forms rapidly, as in the east side of the North American Cordillera, then sea water may rush in, and the first sedimentary deposits are deep water deposits.
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In a series of subsequent papers, Basilevsky and colleagues extensively developed a model that Guest and Stofan (1999) termed the "directional history" for Venus evolution. The general idea is that there is a global stratigraphy that progresses from heavily deformed tessera, to heavily deformed, then moderately deformed plains, and then to undeformed plains. Most recent activity is focused near major rift zones that tend to intersect with large shield volcanoes. The interpretation of tessera as older continental-style cratons is supported by geological analysis of Ashtar Terra and its surroundings.
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Drop-hammer forging usually only deforms the surfaces of the workpiece in contact with the hammer and anvil; the interior of the workpiece will stay relatively undeformed. There are a few disadvantages to this process, most stemming from the workpiece being in contact with the dies for such an extended period of time. The workpiece will cool faster because the dies are in contact with workpiece; the dies facilitate drastically more heat transfer than the surrounding atmosphere. As the workpiece cools it becomes stronger and less ductile, which may induce cracking if deformation continues.
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On the north, the basin extends offshore into the southern Kara Sea. > On the west, north, and east, the basin is surrounded by the Ural, Yenisey > Ridge, and Turukhan- Igarka foldbelts that experienced major deformations > during the Hercynian tectonic event and the Novaya Zemlya foldbelt that was > deformed in early Cimmerian (Triassic) time. On the south, the folded > Caledonian structures of the Central Kazakhstan and Altay-Sayan regions dip > northward beneath the basin’s sedimentary cover. The basin is a relatively > undeformed Mesozoic sag that overlies the Hercynian accreted terrane and the > Early Triassic rift system.
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The basement is composed of foldbelts that were > deformed in Late Carboniferous–Permian time during collision of the Siberian > and Kazakhstan continents with the Russian craton. The basement also > includes several microcontinental blocks with a relatively undeformed > Paleozoic sedimentary sequence. The sedimentary succession of the basin is > composed of Middle Triassic through Tertiary clastic rocks. The lower part > of this succession is present only in the northern part of the basin; > southward, progressively younger strata onlap the basement, so that in the > southern areas the basement is overlain by Toarcian and younger rocks.
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Sneaking back to the Recreation Room, the trio discover a group of Argolins, led by Pangol, performing dangerous experiments in order to perfect a secret project, under the guise of entertainment. Meanwhile, Brock and Klout bring a new offer from a mysterious organisation called West Lodge. It is then, while tearing up the offer, that Pangol reveals the secret of his past and the reason he is the only young Argolin in the Hive. He was the only successful, undeformed child from a cloning experiment meant to save the Argolin using the Recreation Generator.
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The average modal composition is 28% quartz, 25% potassium feldspar, 38% plagioclase, 8% biotite, and 1% accessory minerals, including magnetite, titanite, zircon, hornblende, apatite, and muscovite. There are three generations of deformation preserved in the contact aureole that indicate regional deformation. Microstructure and foliation in the aureole indicate east-west compression and north-south extension during and shortly after pluton emplacement, but the pluton interior is undeformed. Pluton emplacement involving heating to ~650°C at pressures of 2-3 kbars, corresponding to a depth of 7-10 km.
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A pressure shadow (also called strain shadow) is a term used in metamorphic geology to describe a microstructure in deformed rocks that occurs adjacent to a relatively large, undeformed particle, such as a porphyroclast. Pressure shadows often appear in thin sections as pairs of roughly triangular regions that are elongated parallel to the foliation around a clast of a different mineral.. Pressure shadows that contain fibrous mineral textures are also termed pressure fringes or strain fringes. Pressure shadows regions (indicated by dashed lines) around porphyroclasts in a deformed granodiorite.
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Note that the lowest drag, which corresponds to 'optimal' performance, is close to the undeformed 'baseline' design of the airfoil at (0,0). After designing a sampling plan (indicated by the gray dots) and running the CFD solver at those sample locations, we obtain the Kriging surrogate model. The Kriging surrogate is close to the reference, but perhaps not as close as we would desire. In the last figure, we have improved the accuracy of this surrogate model by including the adjoint-based gradient information, indicated by the arrows, and applying GEK.
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A large triangular area surrounding Richmond Gulf, which includes a short segment of the Nastapoka arc, is underlain by about of undeformed, pink and red, mainly fluvial, feldspar-rich sandstone that is interbedded with minor beds of conglomerate and basaltic, subaerial, lava flows. These strata, which are known as the Richmond Gulf Group, rest unconformably on Archean crystalline rocks of the Superior craton and are now preserved by downfaulting only within the Richmond Gulf Graben. The graben, its faults, and the Richmond Gulf Group are unconformably overlain by the strata of the Nastapoka Group.Chandler, F.W. and Schwarz, E.J., 1980.
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The Laxfordian was originally recognised from the presence of deformation and metamorphism of the Scourie dykes. The Laxfordian can be divided into an early event before 1.7 Ga, associated with retrogression of the Scourie gneisses from granulite to amphibolite facies and a later event with local further retrogression to greenschist facies, part of which may be Grenvillian in age (about 1.1Ga). The early event is particularly associated with shear zones in which the deformed Scourie dykes form amphibolite sheets within the reworked gneisses. The original mineralogy of the dykes is also changed to an amphibolite facies assemblage, even where they remain undeformed.
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Tessellated Pavement, a Permian bedding plane In the Permian, glacial conditions predominated with, icecaps on the land, and ice floating on the sea, as a result of which tillite is found at the base of the Permian deposits. Mudstone with dropstones was formed in the sea areas, particularly in the eastern half of Tasmania. This eastern zone is known as the Tasmania Basin. The rocks are undeformed and cover the central part of the state, most of the east coast, down to the south coast, and with extensions to the north coast near Launceston and Devonport.
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Retrieved on 2007-10-18 The formation is a rare alkaline-suite that formed as a result of submarine rifting during the Paleoproterozoic period.Volcanology and geochemistry of the Bravo Lake Formation, Baffin Island, Nunavut. Retrieved on 2007-10-18 The Bravo Lake Formation is surprisingly undeformed by the Himalayan-scale forming event during the Trans- Hudsonian orogeny. The stratigraphy of the Bravo Lake Formation starts with a basic section of iron-oxide rich sandstones, psammites, and semi-pelites which cover a series of deformed pillow lavas which expand in viscosity towards the west, and volcanic/clastic deposits and ultramafic sills.
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Quaderni del Parco Nazionale del Gargano, 48 pp., Foggia. The Apulia Platform, which is part of the stable and relatively undeformed foreland of the Apennine thrust belt, is bounded on both sides by basinal deposits; westward the margin is buried under the Apennine thrust sheets, to the east the adjacent paleogeographic domains are the vast Ionian Basin to the south and the Umbria-Marche Basin to the north. To the west, the Apulia Platform plunges downfaulted underneath the terrigenous sediments of the Apennine foredeep; to the southeast, the Jurassic–Early Cretaceous margin lies 20–30 km offshore from the present Apulia coastline.
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Anorthosite intrusions partly obscure it in places, but a mylonite zone marks it northern boundary. Structural geologists divide it into the undeformed sedimentary and volcanic rocks Kaniapiskau Supergroup in the Labrador Trough (including gabbro sills and plutons) in the west and high-grade anorthosite and gneiss in the east. Virtually all of southern Labrador belongs to the major Grenville Province, which underlies much of eastern Canada and the northern US. Extensive faulting and mylonite marks its northern boundary with the other structural provinces. Archean gneisses were metamorphosed again during the Grenville orogeny and intruded by anorthosite-adamellite plutons.
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The Bylot Supergroup in Baffin Island and Bylot Island is six kilometers thick with a combination of undeformed volcanic, clastic and carbonate rocks deposited during a phase of renewed rifting. The Borden Peninsula is divided into horst and graben structures by normal faults from local rifting and subsidence 1.27 billion years ago. The Nanisivik Mine extracts zinc and lead from these carbonates. The Bylot Supergroup is known as the Fury Group and Hecla Group along the Fury and Hecla Strait, where it overlies Archean and Paleoproterozoic rocks with nearly six kilometers of material, likely deposited over the span of 75 million years.
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In its plainest form, it states that in undeformed stratigraphic sequences, the oldest strata will be at the bottom of the sequence. This is important to stratigraphic dating, which assumes that the law of superposition holds true and that an object cannot be older than the materials of which it is composed. In the simplest way to explain it that is possible, sedimentary rock that has not been moved around will have the oldest layers on the bottom, meaning that any fossils found inside will be older or newer depending where they are in the rock.
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Deposition resumed in the Cambrian period and continued through the Paleozoic era, creating nine major formations which together are 4,000 feet (1,200 m) thick (the only geologic period in the Paleozoic not represented is the Silurian). This unit was laid down in a shallow sea and later became a discontinuous mix of dolomites, limestones, sandstones, and shales. The layers of this unit are relatively undeformed for their age even though periodic upwarp exposed them to erosion, creating uncomformities. Fossilized brachiopods, bryozoans, corals, and trilobites are found in the carbonate rock layers with the best examples found outside the park in the Alaska Basin.
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Crustal shortening is observed to extend farther inland than in normally dipping subduction zones; the Sierra Pampeanas are over 650 km east of the trench axis. Flat slabs have been used as an explanation for the Laramide Orogeny and the central Altiplano-Puna region. Another interesting feature that may be associated with the flat slab subduction of the Nazca Ridge is the Fitzcarrald arch located in the Amazonian Basin. The Fitzcarrald arch is a long-wavelength, linear topographic feature extending from eastern Peru to western Brazil beyond the Subandean thrust front into an undeformed area and rising ~600 masl.
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A complex crater, caused by collision of a hypervelocity body with another larger than itself, is typified by the presence of a dome at the centre of the site of impact. These domes are typically large-scale (on the magnitude of tens of metres) and thought to be the result of post-impact weakening of the overlying strata and basement. Weakening is integral for the vertical uplift required to create a dome to take place, as it allows vertical displacement to happen unconstrained by the original rigidity properties of the undeformed rock.Lana, C., Roger L. Gibson, and Wolf Uwe Reimold.
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The upper part of the Sault Plat watershed is in a piedmont region that falls from an elevation of around in the north down to in the south. The piedmont region has rounded rocky hills, the highest being in elevation. Below the piedmont is a coastal plain wide that falls from an elevationof in the north to an escarpment almost high along the sea. The bedrock is magmatic, mostly an undeformed assembly of granite and pegmatite, with a band of migmatite more than wide that runs from east to west across the center of the watershed.
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Some lava flows from this stage were unstable and collapsed, covering the northern parts of the volcano with debris. This effusive activity eventually oversteepened the cone, causing its southern sector to collapse. During this collapse and landsliding, large toreva blocks developed from sectors of the cone which slid down undeformed, while other material from the cone formed the hummocks in the sector collapse deposit; there was no explosive eruption at the time of the collapse. The configuration of the deposit indicates that the debris entered the Salar when it was filled with water; the height of the tufa deposits imply that water levels were about above sea level.
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The Cordillera de los Frailes stretches along the north-eastern parts of Potosí Department bordering the north-western Chuquisaca Department. It consists of mainly two parts: the western region is a volcanic field of subhorizontal, undeformed ignimbrites dating back to upper Miocene, about 5 to 23 million years from today; the eastern part, the so-called Maragua Syncline which is much older, is a mountain range of sedimentary rock of Cretaceous-Paleocene origin in a north- south thrust. The Cordillera de los Frailes borders Poopó Lake in the northwest and stretches between a line Challapata-Macha-Ravelo in the north and Río Mulato-Potosí-Betanzos in the south.
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This mechanism is different from flow in a subduction channel in that the exhuming sheet is strong and remains undeformed. A variant of this mechanism, in which the exhuming material undergoes folding, but not wholescale disruption, was suggested for the Dabie orogen,where exhumation-related stretching lineations and gradients in metamorphic pressure indicate rotation of the exhuming block;Hacker, B. R., Ratschbacher, L., Webb, L. E., McWilliams, M., Ireland, T. R., Calvert, A., Dong, S., Wenk, H.-R., and Chateigner, D., 2000, Exhumation of ultrahigh-pressure continental crust in east–central China: Late Triassic–Early Jurassic tectonic unroofing: Journal of Geophysical Research, v. 105, p. 13339–13364.
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In some studies, a detergent, enzyme, or drug is used to disturb the cytoskeleton, thereby altering, or sometimes completely eliminating, the tractions generated by the cell. First, a continuous displacement field is computed from a pair of images: the first image being the reference configuration of microspheres surrounding an isolated cell, and the second image being the same isolated cell surrounded by microspheres that are now displaced due to the cellular-generated tractions. Confocal fluorescence microscopy is usually employed to image the cell surface and fluorescent beads. After computing the translational displacement field between a deformed and undeformed configuration, a strain field can be computed.
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For example, a point on a horizontal beam can undergo both a vertical displacement and a rotation relative to its undeformed axis. When there are M degrees of freedom a M x M matrix must be used to describe the stiffness at the point. The diagonal terms in the matrix are the direct-related stiffnesses (or simply stiffnesses) along the same degree of freedom and the off-diagonal terms are the coupling stiffnesses between two different degrees of freedom (either at the same or different points) or the same degree of freedom at two different points. In industry, the term influence coefficient is sometimes used to refer to the coupling stiffness.
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Over 50 genera of Oreodonta have been described in the paleozoological literature. However, oreodonts are widely considered to be taxonomically oversplit, and many of these genera may prove to be synonymous. The last researchers to fully review oreodont taxonomy, C. Bertrand Schultz and Charles H. Falkenbach, have been criticized for erecting excessive numbers of genera, based in part on apparent anatomical differences between different specimens that were actually taphonomic deformations due to postburial forces. Undeformed skulls would be placed in one genus, while skulls crushed from side to side would be placed in a second genus and skulls crushed from front to back would be placed in a third genus.
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Laxfordian event Laxford is in the region of the Lewisian gneiss complex, deformed by Moine Thrust, which occurred during the Caledonian Orogeny. To the south are Scourian high-grade metamorphic rocks, some 3,000 million years old, intruded with undeformed Scourie dykes 2,400 million years ago whereas to the north are lower-grade metamorphic rocks, which were later deformed and metamorphosed during the Laxfordian orogeny. At Laxford, layers of pink granite and pegmatite intruded into hot gneiss about 1,750 million years ago. Alternating layers of black mafic gneiss and grey felsic gneiss are to be seen, cut across by steeply dipping sheets of granite and pegmatite.
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In terms of recognising orogeny as an event, Leopold von Buch (1855) recognised that orogenies could be placed in time by bracketing between the youngest deformed rock and the oldest undeformed rock, a principle which is still in use today, though commonly investigated by geochronology using radiometric dating. Based on available observations from the metamorphic differences in orogenic belts of Europe and North America, H. J. Zwart (1967) proposed three types of orogens in relationship to tectonic setting and style: Cordillerotype, Alpinotype, and Hercynotype. His proposal was revised by W. S. Pitcher in 1979 in terms of the relationship to granite occurrences. Cawood et al.
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By contrast, the overlying sedimentary rocks that ascend to the ground surface are undeformed and include units from the Riphean (an Eastern European stratigraphic division dating to the transition from the Proterozoic), Paleozoic, Mesozoic and Cenozoic. Potassium-argon dating of glauconite from the lowest units gives an age of 1.01 billion to 590 million years ago, with units 100 to 150 meters thick, overlain by 700 meter thick conglomerate, sandstone and siltstone. A six-meter thick sandstone in the west is the only Ordovician rock unit in the country. Silurian deposits are common in Moldova, mainly clay and carbonates 150 meters thick in north and grading to as much as 900 meters in the southwest.
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This gives it better flight characteristics with a higher sectional density, and the projectile retains velocity better at longer ranges than an undeformed shell of the same weight. As with the APCR, the kinetic energy of the round is concentrated at the core on impact. The initial velocity of the round is greatly increased by the decrease of barrel cross-sectional area toward the muzzle, resulting in a commensurate increase in velocity of the expanding propellant gases. The Germans deployed their initial design as a light anti-tank weapon, 2,8 cm schwere Panzerbüchse 41, early in the Second World War, and followed on with the 4.2 cm Pak 41 and 7.5 cm Pak 41.
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Example of restored and balanced section from National Wildlife Refuge 1002 Area, Alaska In structural geology section restoration or palinspastic restoration is a technique used to progressively undeform a geological section in an attempt to validate the interpretation used to build the section. It is also used to provide insights into the geometry of earlier stages of the geological development of an area. A section that can be successfully undeformed to a geologically reasonable geometry, without change in area, is known as a balanced section. Comparably a palinspastic map is a map view of geological features, often also including present-day coastlines to aid the reader in recognising the area, representing the state before deformation.
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The Ruby Mountains are part of the Basin and Range Province that formed as a result of extension of the North American plate. Normal faults on the eastern and western flanks of the range separate it from the basins on either side of it. The Ruby Mountains are an example of a metamorphic core complex, and middle and lower crustal rocks have been exhumed to the surface in the footwall of a large detachment fault. A mylonitic shear zone can be traced along the fault on the western margin of the Ruby Mountains, marking the contact between the igneous and metamorphic rocks in the core complex and the undeformed sedimentary rocks around it.
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It was collected from the Bairro Cachoeira locality at the base of the Serra da Água Limpa, about 8 km northwest of Monte Alto city of northern São Paulo, from the Adamantina Formation. In 2013, this specimen was reassigned to the closely related notosuchian genus Caipirasuchus, creating the combinatio nova Caipirasuchus montealtensis. The type species of the genus, C. paulistanus, is known only from the holotype specimen MPMA 67-0001/00, an almost complete and undeformed skull and mandible with teeth (only three teeth are missing) and partial postcranium, from a single individual. It was found on the São Francisco Farm, in Homem de Mello, the rural area of Monte Alto County, also from the Adamantina Formation.
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Mandibular symphysis of the first three named species Caipirasuchus was first named by Fabiano V. Iori and Ismar S. Carvalho in 2011 and the type species is C. paulistanus. The generic name is derived from Portuguese word Caipira which refers to the rural inhabitants of the Brazilian states, covering almost all of the Bauru Basin, and Greek souchus meaning "crocodile". The specific name is derived from "paulista", the designation for the residents of São Paulo State, where the holotype was found. C. paulistanus is known only from the holotype specimen MPMA 67-0001/00, an almost complete and undeformed skull and mandible with teeth (only three teeth are missing) and partial postcranium from a single individual.
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Their gravitational field would deform the horizon of the black hole, and the deformed horizon could produce different outgoing particles than the undeformed horizon. When a particle falls into a black hole, it is boosted relative to an outside observer, and its gravitational field assumes a universal form. 't Hooft showed that this field makes a logarithmic tent-pole shaped bump on the horizon of a black hole, and like a shadow, the bump is an alternative description of the particle's location and mass. For a four- dimensional spherical uncharged black hole, the deformation of the horizon is similar to the type of deformation which describes the emission and absorption of particles on a string-theory world sheet.
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Palaeoproterozoic rocks of the eastern and central Gawler Craton are overlain by relatively unmetamorphosed clastics of the Corunna Conglomerate, the Gawler Range Volcanics, the Pandurra Formation, and thin platformal late Proterozoic and Cambrian sediments of the Stuart and Spencer Shelves. In and around the Gawler Ranges, the volcanics and older rocks were intruded by Hiltaba Suite granites which are closely associated with formation of the giant Olympic Dam orebody of the Eastern Olympic Copper-Gold Province. Although relatively undeformed, the Gawler Range Volcanics, which extend from the centre of the craton to its eastern margin, represent a major period of crustal deformation ca. 1590 Ma which heralded the final consolidation and stabilisation of the craton as it is seen today.
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Babibasiliscus is an extinct genus of casquehead lizard (family Corytophanidae) that lived in what is now Wyoming during the early Eocene, approximately 48 million years ago. The genus is known from a single species, Babibasiliscus alxi, which was named by paleontologist Jack Conrad in 2015 on the basis of a fossilized skull from the Bridger Formation in the Green River Basin. The name Babibasiliscus comes from the Shoshoni word babi, meaning "older male cousin", and Basiliscus, a modern-day genus of casquehead lizards. The specimen is undeformed and nearly complete except for the tip of the snout and the top of the skull, making it unclear whether the distinctive bony crest of living corytophanids was present in prehistoric relatives like Babibasiliscus.
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Jotnian sediments rests on what is known as Subjotnian rocks which include weathered rapakivi granites and the Hogland Series. Amantov and co-workers comments about the terms Jotnian and Postjotnian that: At large scale, Jotnian sediments are classified as being part of a "quasiplatform" group of sediments of the East European Platform not being metamorphosed enough to be part of the "protoplatform" and not being undeformed enough to be part of the "cataplatform" category. By analogy to the established Sub-Cambrian peneplain that extends across much of Fennoscandia there have been suggestions of the existence of an exhumed Subjotnian peneplain. This surface actually exists but its extent is very limited, represented as small valley plains at Sveg and along the Västerdalälven-Dalälven system.
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They formed as granite magma, and related pegmatite fluids, filled crack-systems as magma migrated through the crust. The chemical composition of the granite and pegmatite comprising these dike swarms is indicative of the partial melting of the metasedimetary and metavolcanic rocks of the Granite Gorge Metamorphic Suite both in-place and at greater depth, in the crust. These dikes exhibit a wide variability in the degree that they have been deformed from straight and nearly undeformed - to varying degrees of folding, stretching, and shearing. The variable degree of the deformation of these structures is interpreted to indicate that these dike swarms were emplaced during a period of significant mountain building and crustal thickening that was possibly associated with continental collision.
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Also, loose earth, grit, and other particles easily entered the gun through these open-sided magazines, an ever-present risk in the muddy environment of the trenches. An insistence on using only good, undeformed magazines with strong springs was the most practical solution to this problem. Chauchat gunners were also known to load their magazines with 18 or 19 rounds, instead of the maximum 20, in order to avoid the dreaded first-round failure to feed. The Chauchat's long recoil system is often cited as a source of excessive stress on the gunner when firing, though recent and extensive firing tests have demonstrated that it is the Chauchat's ergonomics and its loose bipod, rather than its recoil, that makes it a difficult gun to keep on target beyond very short bursts.
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The Two Medicine Formation is a geologic formation, or rock body, that was deposited between 83.5 ± 0.7 Ma and 70.6 ± 3.4 Ma (million years ago), during Campanian (Late Cretaceous) time, and is located in northwestern Montana and southern Alberta. It crops out to the east of the Rocky Mountain Overthrust Belt, and the western portion (about thick) of this formation is folded and faulted while the eastern part, which thins out into the Sweetgrass Arch, is mostly undeformed plains. Below the formation are the nearshore (beach and tidal zone) deposits of the Virgelle Sandstone, and above it is the marine Bearpaw Shale. Throughout the Campanian, the Two Medicine Fm. was deposited between the western shoreline of the Late Cretaceous Interior Seaway and the eastward advancing margin of the Cordilleran Overthrust Belt.
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The exact locality is not stated but the specimens were most likely collected from the quarry where they had previously been recorded as annelid tracks. The probable depositional environment of the quarry strata, as envisaged by Rattigan (1967) and other workers, was a shallow periglacial lake which received sediment influxes via turbidity currents. Low velocity traction currents modified the surface of these lake bed deposits, and ice-rafted pebbles (derived from moraines) were dropped into them at intervals from melting floes and icebergs. Crowell and Frakes (1971) consider that this glaciation was of alpine type and took place at a (late Carboniferous) latitude of 45-50 degree S. Perhaps the most spectacular features exposed in the quarry are localised contorted beds interstratified between apparently undisturbed layers and laterally continuous with undeformed planar strata.
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They studied wedge indentation with a 90 degree included angle into a single nickel crystal (and later the included angles of 60 degree and 120 degree were also available by Dahlberg et al.). By comparing the orientation of the crystal lattice in the after-deformed configuration to the undeformed homogeneous sample, they were able to determine the in-plane lattice rotation and found it an order of magnitude larger than the out-of-plane lattice rotations, thus demonstrating the plane strain assumption. The Nye dislocation density tensor has only two non-zero components due to two-dimensional deformation state and they can be derived from the lattice rotation measurements. Since the linear relationship between two Nye tensor components and densities of geometrically necessary dislocations is usually under-determined, the total density of geometrically necessary dislocations is minimized subject to this relationship.
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Furthermore, two distinct structural levels can be seen in this section, an upper level comprising the majority of the mass of the Lewis thrust sheet which is characterized by broad open folds in relatively undeformed rocks, and a fairly thin lower level consisting of stacked imbricate, southwest-facing, sigmoidal thrust fault slices, bounded below by the Lewis thrust, and above by a separate bedding-parallel thrust called the Tombstone thrust. These culminations progressively stack up and accommodate significant lateral crustal shortening associated with the compression along the Lewis thrust fault. Another extremely similar section of this duplexing is seen at another outcrop in the Waterton Lakes area in Southwest Alberta. In addition to duplexes seen in windows, the Lewis thrust also shows isolated remnants of the eastern edge of the upper plate( klippes) located at Chief Mountain in Montana and Crowsnest Mountain in Alberta.
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Geological map of the Hebridean Terrane showing distribution of rocks of the Lewisian complex Undeformed Scourie dyke cutting Lewisian Gneiss, about 1.6 km west of Scourie foliated amphibolites) cutting grey gneiss of the Scourie complex, both deformed during the Laxfordian tectonic event and cut by later (unfoliated) granite veins - road cutting on the A838 just north of Laxford Bridge The main outcrops of the Lewisian complex are on the islands of the Outer Hebrides, including Lewis, from which the complex takes its name. It is also exposed on several islands of the Inner Hebrides, small islands north of the Scottish mainland and forms a coastal strip on the mainland from near Loch Torridon in the south to Cape Wrath in the north. Its presence at seabed and beneath Paleozoic and Mesozoic sediments west of Shetland and in the Minches and Sea of the Hebrides has been confirmed from the magnetic field, by shallow boreholes and hydrocarbon exploration wells.C.Michael Hogan. 2011.
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The Aravalli Range joins two of the ancient earth's crust segments that make up the greater Indian craton, the Aravalli Craton which is the Marwar segment of earth's crust to the northwest of the Aravalli Range, and the Bundelkand Craton segment of earth's crust to the southeast of the Aravalli Range. Cratons, generally found in the interiors of tectonic plates, are old and stable parts of the continental lithosphere that has remained relatively undeformed during the cycles of merging and rifting of continents. volcanic arc and geological process of undersea subduction during tactonic collusion global convergent boundary of plate margins It consists of two main sequences formed in Proterozoic eon, metasedimentary rock (sedimentary rocks metamorphised under pressure and heat without melting) and metavolcanic rock (metamorphised volcanic rocks) sequences of the Aravalli Supergroup and Delhi Supergroup. These two supergroups rest over the Archean Bhilwara Gneissic Complex basement, which is a gneissic (high-grade metamorphism of sedimentary or igneous rocks) basement formed during the archean eon 4 Ga ago.
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The Narryer Gneiss Terrane has undergone many high-grade polyphase deformation events, with the most notable being at 2600 to 2700 Ma associated with granite-greenstone magmatism in the Yilgarn Craton, following an event at ~3350 Ma of amphibolite facies, resulting in widespread re-equilibration of geochronometers, preceded by a deformation loosely constrained to ~3680 Ma and another predating the Meeberrie Gneiss and postdating the Manfred Complex, between 3680 and 3730 Ma. Older structural grain is preserved in areas of low stress in subsequent deformations; the 2700 to 2600 Ma Yilgarn Craton associated deformation has overprinted most other deformations, resulting in rotation of previous structures into parallelism with NE-trending upright folds and metamorphic banding. Proximal to the Proterozoic orogens and thrust belts, the gneiss belt has become variably overprinted by later deformations. In the Bryah-Padbury Basin fold-thrust belt, Yarlarweelor Gneiss rafts exist as undeformed thrust plates of pelitic schist bounded by discrete mylonite zones, as well as deformed heavily overprinted gneiss blocks caught up within shear zones, some of which appear to preserve the unconformity surface.
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While the Hawaiian archipelago faces a significant threat from even relatively minor local events, the threat to other trans-Pacific regions has been deemed "exaggerated".. Particularly, the larger, more powerful, and more dramatic landslides seen around the Hawaiian Islands are a type of landslide called debris avalanches, where the material in the slide has broken up into pieces small enough to flow as a relatively narrow (typically less than 50 km wide), fast-moving stream that can run-out as far as .. Debris avalanches, or flows, "commonly represent a single episode of rapid failure",. where the potential energy of the slide is released suddenly, and could cause giant tsunamis., citing Geological Society of America Special Paper 229 (1988). On the other hand, slumps are largely intact and undeformed blocks that are wider (up to 110 km) and thicker (about 10 km) than debris avalanches, and generally slow moving.. Slumps commonly move on a concave surface, with the head dropping down almost vertically (as seen at the Hilina Pali and related cliffs), and the toe thrusting upward.
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