"is by definition more gradual, and merges with the landscape to the south east. The Thames is a clear end point to the south west, whereas north east of Luton the hills decline slowly in prominence. The chalk escarpment of the Chiltern Hills overlooks the Vale of Aylesbury, and roughly coincides with the southernmost extent of the ice sheet during the Anglian glacial maximum. The Chilterns are part of a system of chalk downlands throughout eastern and southern England, formed between 65 and 95 million years ago, comprising rocks of the Chalk Group; this also includes Salisbury Plain, Cranborne Chase,"
"Chilterns"", on an outcrop hill, a contender for the most easterly in the triangular chalk belt enclosing most of South-East England all of East Anglia. The building was originally a Saxon monastery, which grew richer and more influential through the mining and selling of coprolite, fossilised dinosaur dung, once used as a fuel and also a fertilizer. The church also has a secret underground passageway, leading to the basement of a local and equally antiquated house. It is believed that there used to be more secret passages, possibly leading all the way out of the village, but they have never"
"inside the county, at the foot of the chalk Chiltern Hills, near Tring and Ashwell, there is a small strip of exposed Cretaceous Gault Clay and Upper Greensand. At 100 million years old, these are the oldest rocks in the county. Rocks get progressively younger as one moves in a south easterly direction through the county. The lowest layer of the chalk is the Chalk Marl, which, with the Totternhoe Clunch Stone above it, lies at the base of the Chiltern Hills escarpment. This is visible as a terrace projecting north-westwards, near Whipsnade and Ivinghoe. Above these beds, the Lower"
"Part of the magma chambers for the volcanoes are exposed at the surface as major intrusions of gabbro and granite. These coarse-grained igneous rocks are relatively resistant to erosion and now form the Cuillin hills. The Black Cuillin are formed of gabbro, which erodes to form the characteristically jagged outlines, although this is in large part due to the many minor intrusions, such as dykes and cone sheets that cut the gabbro. The Red Hills are formed of granite and have a more rounded topography. All pre-Quaternary rock types on the island are affected by a major swarm of dykes,"
"out from underneath the latter. This has resulted in the formation of numerous cateracts such as Niagara Falls and the High Falls of Rochester, New York which are but local manifestations of a regional geographic feature called the Niagara Escarpment. The Clinton Group (or Formation) is a widely traceable, lower Silurian lithostratigraphic unit composed primarily of shale and mudstone, though it encompasses a heterogeneous assemblage of sedimentary rock types, including conglomerate, sandstone, limestone, dolostone, and ironstone. In its designated type area in Clinton, Oneida County, New York the unit is approximately 50 meters (180 feet) thick, and composed primarily of"
"of which is v-shaped opening to the east and bounded by chalk outcrops forming hills: the North Downs to the south of London, and the Chilterns to the north. The chalk is a soft white limestone that is different in appearance to other limestones because it is porous and earthy whilst others are compact and crystalline. The chalk basin has been infilled with a sequence of clays and sands of the more recent Paleogene Period, then Neogene Period (1.6 to 66.4 million years old). Most significant is the stiff, grey-blue London Clay, a marine deposit which is well known for"
"Chilterns the two parts are separated by the hard Totternhoe Stone, which forms a prominent scarp in some places. There are few, if any, flint nodules present. These two formations are not recognised within the northern province i.e. the outcrop north from East Anglia to Yorkshire, where the entire sequence is now referred to as the 'Ferriby Chalk Formation'. The thickness of the Grey Chalk Subgroup strata varies, averaging around , depending upon the location. They often contains fossils such as the ammonites ""Schloenbachia"", ""Scaphites"", and ""Mantelliceras"", the belemnite ""Actinocamax"", and the bivalves ""Inoceramus"" and ""Ostrea"". The White Chalk Subgroup"
"bedrock of the hills is a flinty limestone. The largest town in the area is Manhattan, Kansas, and the hills can be accessed from the Flint Hills Scenic Byway, which passes through in Kansas. The rocks exposed in the Flint Hills were laid down approximately 250 million years ago during the Permian Period. During this time much of the Midwest, including Kansas and Oklahoma, were covered with shallow seas. As a result, much of the Flint Hills are composed of limestone and shale with plentiful fossils of prehistoric sea creatures. The most notable layer of chert-bearing limestone is the Florence"
"why the church tower is built of brick rather than limestone carted at great expense from the quarries along the Jurassic outcrop beyond the Wolds at e.g. South Newbald and South Cave or on the Howardian Hills, north-west of Malton. It might also reflect the (dis)interest and (lack of) wealth of successive owners of the Estate. The clays that are the major constituent of Holderness, upon which Kilnwick is situated, are glacial in origin. Successive Pleistocene ice sheets swept south on a broad front from Northumbria, the Arctic Sea, and Scandinavia. The last advance – the Devensian glaciation (circa 60,000"
"continental crust. Peraluminous granites are those that contain more aluminum oxide than sodium oxide, potassium oxide, and calcium oxide combined. The batholith is composed of the Bitterroot lobe in the north and the larger Atlanta lobe in the south. The major mountain ranges in the region are part of the Rocky Mountains; they include the Bitterroot Range, Clearwater Mountains, Salmon River Mountains, and the Sawtooth Range. Major mountain peaks include 10,201 ft (3,085 m) tall Trapper Peak in the Bitterroot Mountains in Montana and 12,009 ft (3,660 m) tall Hyndman Peak in the Pioneer Mountains in Idaho. Soils derived from"
"white quartz and other phyllites and Precambrian basalt flows. The greenstone was originally formed about 570 million years ago as part of the rifting of the super-continent, Rodinia. The greenstone was later uplifted during the Alleghenian Orogeny and thrust westward, being interspersed with the sedimentary rock deposited during the Paleozoic era. Much of the mountain, being shattered rock, is home to large populations of timber rattlesnakes. There are also black bears, turkeys, and deer, as well as vultures and raptors. The name ""Catoctin"" probably derives from the Kittoctons, an American Indian tribe or clan which once lived between the mountain"
"result of quarrying - at its northwest end at an approximate altitude of 160 meters. The underlying geology of Gillies Hill is a layer of quartz-dolerite approximately 100 meters thick of the Late Carboniferous tholeiitic Midland Valley Sill-complex (Stirling Sill). The hill is one of a series of crag and tail formations that cross the Carse of Stirling separated by faults into distinct hills such as Abbey Craig, Kings Park, Sauchieburn and Stirling Castle rock. These crag and tail formations were created by glaciation that terminated about 10,000 years ago. The quartz-dolerite of the hill, highly resistance to erosion, is"
"Wiltshire. To the north of these downs, mostly in Buckinghamshire, are the Chiltern Hills, running north east. At the far south west of the formation are the Dorset Downs, notable for their rich Roman and pre-Roman archaeology, including a number of Iron Age hill forts. The Purbeck Hills fork from the Dorset Downs to run on, or near the Jurassic Coast in south east Dorset, where they form part of Lulworth Cove, White Nothe and Old Harry Rocks, some of the many famous landforms on one of England's two natural World Heritage Sites. Smooth convex curves are characteristic of the"
"north. To the south are Mississippian layers, formed between 320 and 360 million years ago. On the upper reaches of the mountain is tough Devonian sandstone, formed between 360 and 408 million years ago. It caps Brush Mountain and juts out to the north at the top of the wilderness slope. Below it lies brittle layers of older and more loose Devonian shale which is subject to erosion. The lower reaches along Craig Creek valley contain Silurian sandstone, formed between 408 and 438 million years ago and extending northwest to form Sinking Creek Mountain. This wilderness was designated by Congress"
"of essexite which is popular for making curling stones and Cramond island is made up of dolerite. Inchmickery and Inchgarvie are of igneous origin and the latter is partly made up of picrite. Studies of the landscape beneath the waters of the firth have revealed that the visible surface of Inchgarvie is only the top of a larger crag and tail structure similar in structure to Edinburgh Castle and the Royal Mile created by glacial action. The tidal islet of Eyebroughy is about to the west of Fidra. Its component rock is trachyte and Lower Carboniferous in origin. Most of"
"pyroclastic rocks, sills and dikes. These volcanic rocks range from basalts to rhyolites, with the majority classifying as basaltic andesites and andesites. They are closely related to the calc-alkaline volcanic centres of the Pemberton Volcanic Belt, indicating that the volcanic rocks comprising Chipmunk Mountain were created as a result of volcanism in the Canadian Cascade Arc. The volcanic rocks have been dated to be million years old, which correlates with the time of Pemberton Belt volcanism. Chipmunk Mountain Chipmunk Mountain is a mountain in southwestern British Columbia, Canada, located southwest of Bralorne. It has an elevation of and a topographic"
"and the gneisses underlying the Bentley Supergroup volcanics. The caldera is in two parts, an overlying volcanic edifice composed primarily of porphyritic rhyolite and dacite with occasional vent complex agglomerates, which shows prominent circular ring-complex faults, and the Winburn Granite which underlies the caldera and is primarily exposed in the east as a pink, potassium-feldspathic porphyry granite, the lower margins of which are weakly tectonised. The whole caldera edifice is tilted to the southwest, which is why the Winburn Granite is exposed along the east and northeast. The Skirmish Hill Caldera is poorly exposed along the southern margin of the"
"part of the town is built on the Coulard Hill which consists of pale grey and yellow sandstones and with these is associated a cherty and calcareous band, known as "" 'the cherty rock of Stotfield' "". This rock is a form of silica that contains micro-crystalline quartz. Also in the calcareous band of the Stotfield rock there is limestone with nodular masses of flint, crystals of galena (lead ore) and iron pyrites. The quarry on the east side of the town that produced the stone for the building of Branderburgh produced the largest variety and total numbers of fossil"
"and fire as well as the effects of global warming are the major variables that they considered. The Peak is formed almost exclusively from sedimentary rocks dating from the Carboniferous period. They comprise the Carboniferous Limestone, overlying Gritstone and the Coal Measures which occur only on the extreme margins and infrequent outcrops of igneous rocks including lavas, tuffs and volcanic vent agglomerates. The general geological structure is that of a broad dome, whose western margins have been most intensely faulted and folded. Uplift and erosion have effectively sliced the top off the dome to reveal a concentric outcrop pattern with"
"Hills are the most impressive. This line is considered to mark the edge of two terranes – two once separate fragments of the Earth's crust now joined as one – the Wrekin Terrane to the west and the Charnwood Terrane to the east. The main face of Gullet Quarry shows a cross-section through the Precambrian rock and exhibits many rock types including diorite, granite, gneiss, schist, pegmatite and dolerite. The evidence of the complex history of earth movements which formed the Hills can be seen by multiple joints, fractures, faults and shears, which make identifying changes in rock types difficult."
"Batholith. They are typically sandy loam to clay loam surface soils with clay or parent rock at depth. The town of Dalveen is in the north of the Granite Belt. Other villages include Applethorpe, Amiens, Ballandean, Glen Aplin, Passchendaele, Thulimbah, Pozieres, and Wallangarra, in the south at the border with New South Wales. Liston is a small village in New South Wales that is considered part of the Granite Belt. The area is Queensland's premier wine region and home to the Queensland College of Wine Tourism. Many of the fifty-plus wineries in the region have enjoyed significant success with Shiraz,"
"names. The Black Mountains are composed almost exclusively of rocks assigned to the Old Red Sandstone and dating from the Devonian period. This thick sedimentary sequence comprises sandstones, mudstones, siltstones and numerous thin limestones. The exception is the summit area of Pen Cerrig-calch where a thin sequence of Carboniferous rocks occur, an outlier of the more extensive outcrop to the south of the Usk valley. The lower slopes of these hills are formed from the mudstone-rich St Maughans beds at the top of which lies a calcrete - a discontinuous limestone band known as the Ffynnon Limestone. Above this are"
"Mountain contains shale that originated as mud on the seafloor of a former ocean. This same shale formation forms rocks in other locations throughout southwestern British Columbia. The most common rocks that comprise Whistler Mountain are andesite and dacite lava flows. These lava flows and the associated shale form part of a rock assemblage called the Gambier Group. This geologic group was created within a shallow underwater basin about 100 million years ago during the Early Cretaceous period. Granular material, such as clay, sand and silt, was carried into the ancient ocean by rivers that existed during the Cretaceous period."
"Bilger's Rocks Bilger's Rocks is a park in Clearfield County, Pennsylvania, USA, near the town of Grampian in Bloom Township. The surrounding area is intricately laced with hills, mountains, and river valleys that generally follow the Appalachian mountain range in a northwest to southeast direction. The area of the park is located along the Allegheny section of the mountains, approximately southwest of the highest point on Interstate 80 east of the Mississippi River. The creation of the sandstone seen exposed at Bilger's Rocks was during the Carboniferous Period that lasted from 354 to 290 million years ago. The rocks exposed"
"""its have defined what decades of moviegoers think of when they imagine the American West."" The area is part of the Colorado Plateau. The elevation of the valley floor ranges from above sea level. The floor is largely siltstone of the Cutler Group, or sand derived from it, deposited by the meandering rivers that carved the valley. The valley's vivid red color comes from iron oxide exposed in the weathered siltstone. The darker, blue-gray rocks in the valley get their color from manganese oxide. The buttes are clearly stratified, with three principal layers. The lowest layer is the Organ Rock"
"is from 1500 feet to 1800 feet. The ridge goes in a northeast-southwest axis. Beyond this ridge,there are series of rolling hills and small ridges underlain by Silurian and Devonian aged rocks. The Kittatinny Ridge was created about four hundred million years ago when a small continent that was long and thin collided with proto North America. The strike caused folding and faulting which cause the Silurian Shawnagunk conglomerate which is made mostly of quartz, to rise out of a shallow sea. The heat from pressure caused the quartz to bend, and silica melted the quartz granules together along with"
"ridges, are part of the same Paleozoic anticline rock formation consisting of older Ordovician Bald Eagle Formation Sandstone and Juniata Formation Shale, and younger Silurian Tuscarora Formation Quartzite. During the Appalachian orogeny, these layers folded up with the underlying and overlying layers into the Nittany Arch. The arch was a Himalayan scale mountain that towered above what is now Nittany Valley, where the oldest rock layers from deep within the eroded mountain are now exposed. The Tuscarora Quartzite is more resistant to erosion than Bald Eagle Sandstone, and both are more durable than the Juniata Shale sandwiched in-between. Softer rock"
"geology is responsible for the quality of Malvern's spring water. The hills consist of Precambrian igneous and metamorphic rock, the oldest of which are about 670 million years old. The rocks are characterised by low porosity and high secondary permeability via fissures. Malvern water is rainwater and snow meltwater that percolates through fissures created by the pressures of tectonic movements about 300 million years ago when advancing sedimentary layers of Silurian shale and limestone were pushed into and under older Precambrian rock. When the fissures are saturated, a water table forms and the water emerges as springs around the fault"
"it the Erie Shale, but it was discovered that the name ""Erie Shale"" was preoccupied (already in use). Ohio State University professor of geology Charles S. Prosser further described the formation in 1903, and proposed the name ""Chagrin Shale"" because the shale presented such excellent outcroppings near the Chagrin River. Dr. Prosser's suggested nomenclature was adopted. The Chagrin Shale is, generally speaking, a grey or greenish-gray argillaceous shale consisting of gray siltstone, silty gray shale, soft gray clay shale, and (uncommonly) grayish-black shale. The primary minerals in the shale are chlorite, illite, kaolinite, and quartz. Thin to massive beds of"
"from a central vent. These are overlain by thick mafic alkaline lava flows and at least 30 small cinder cones. Hawaiite is the dominant rock type, but alkali olivine basalt and spinel lherzolite-bearing basanite is also present. They merge laterally with lavas of the much older Chilcotin Group, which surrounds the Anahim Volcanic Belt. However, the exact nature of the relationship between the Anahim Volcanic Belt and the Chilcotin Group is unknown. Exposed in the middle of the mountain range is an assemblage of deformed andesite to dacite lava flows and volcanoclastic sediments. These basement rocks were created during the"
"alternatives exist further south. Mountains on southeastern Ellesmere Island are principally made of granitic gneiss, migmatic, undifferentiated intrusive and volcanic rocks. They are typified by being highly eroded, with conspicuous deep vertical fissures and narrow ledges. The Arctic Cordillera form the eastern edge of the Canadian Shield, which covers much of Canada's landscape. Precambrian rock is the major component of the bedrock. Mountains of volcanic rock range in age from 1.2 billion to 65 million years old. The Late Cretaceous Ellesmere Island Volcanics has been uncertainly associated to both the early volcanic activity of the Iceland hotspot and the Alpha"
"they are mainly composed of volcanic rocks in the basalt to andesite composition range, with few rocks of more felsic composition than dacite. Changes in magma composition have also occurred in the American portion of the Cascade Arc. The Coquihalla Volcanic Complex began its formation when large pyroclastic flows were erupted on an erosional surface. Emptying of the shallow magma chamber caused tilting of the unconformity on the Eagle pluton, which is situated to the southeast. Concomitant with faulting, tilting and subsidence, avalanche breccias repeatedly slid off oversteepened exposures of the Pasayten Group and Eagle pluton. After volcanic activity deposited"
"the North American craton. It is subdivided into two formations: the Sulphur Mountain Formation at the base and the Whitehorse Formation at the top. The Sulphur Mountain Formation consists of dolomitic and calcitic siltstones, silty dolostones, dolomitic limestones, and very fine-grained dolomitic quartz sandstones. The Whitehorse Formation consists of dolostones, dolomitic siltstones and limestones, and dolomitic and calcitic quartzites. Spray River Group The Spray River Group is a stratigraphic unit of Triassic age. It is present on the western edge of the Western Canada Sedimentary Basin in the foothills and Rocky Mountains of western Alberta. It was originally described as"