The northeastern slopes of the Kleiner Deister are characterised by marls, clays and limestones. These are the so-called Münder marls of the Upper Jurassic.
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The soil is sandy on top of beds of Keuper Marls and Bunter Sandstone.
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These strata consist of clay beds and various kinds of calcareous beds, interbedded with clayey marls.
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Alternating grey fluviatile sands and red silty marls of the Lower Freshwater Molasse at Wallenried, Switzerland.
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The soils are mainly clay-sand, with some other elements such as lime, marls and ochre clays.
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Xenic rocks, some of chalk, some of limestone, sandstone marls mica shist, and gypsum, are very fertile.
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The fossil impressions are preserved in micrite limestones, resulting in low quality preservation of fine details. Another series of species were described from compression fossils found in thin layers and concretions of micrite from the "insect bed" and older stratum of the Bembridge Marls. The marls are exposed at a number of locations along the north coast of the Isle of Wight in England. Part of the Bouldnor Formation, the marls have been dated to the Late Eocene in age.
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The Lestaillats Marls is a geologic formation in France. It preserves fossils dating back to the Cretaceous period.
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The basalt flows overlie older, distinctly lighter-colored limestones and marls, exposed along the Yarmouk River in the south.
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The Nay Marls Formation is a geologic formation in France. It preserves fossils dating back to the Cretaceous period.
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De Gruyter, Berlin and New York Prohepialus (possibly Hepialidae) has been described from the about 35-million-year-old Bembridge marls of Isle of Wight.Jarzembowski, E.A. (1980). Fossil, insects from the Bembridge Marls, Palaeogene of the Isle of Wight, southern England. Bulletin of the British Museum (Natural History) (Geology), 33: 237-293.
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Commercially important deposits occur in marls in Westphalia, and it is also found with zeolites at Oberschaffhausen, Bötzingen, Kaiserstuhl, Baden-Württemberg.
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Around the Río Chico in the Cañadón Asfalto Basin, the formation is about thick and comprises siltstones, sandstones, marls and limestones.
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This last unit is composed of alternating marls and dolomites, with some decametric decametre-scale sandstone beds close to the base.
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This layer consist of limestone, marls, and dolomites. The Devonian includes all the stages, with the early Devonian predominantly found in central Belarus.
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The unit is composed of rhythmically bedded marls, horizons of laminated organic-rich black shales, rare marly limestones, clastic turbidites, and penecontemporaneous slumps.
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Yarmouth Common with Bouldnor Cliffs in the background The basal, 20 to 23 metres, exceptionally-35 metres-thick Bembridge Marls Member is mainly composed of blueish to greenish-gray clays and marls. Interlaced are several mollusc-bearing horizons. The clays show a rhythmical, varve-like layering. The member overlies the summital mudcracks of the Bembridge Limestone Formation without any discontinuity.
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Protarabellites rectangularis and P. staufferi can, however, be found in marls and slightly deeper environments and seem to be less stenotopic than P. triangularis.
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The reed sandstone (Km2) then forms a first striking terrain level. The city itself is located on the western edge of this steep step. The reed sandstone was obtained in small quarries as quarry stone for construction purposes. The marls of the so-called Red Wall (Km3) are susceptible to weathering, only the following harder stone marls (Km4) give rise to another stage in the terrain.
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Lower down the slope, starting at the 300 meter line, is oolitic limestone, white oolite, marls, kidney- shaped limestone, and lower oolite on a layer of marl.
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87-89 Typical Toarcian sections of the Orava Succession are represented by condensed red marls, marly limestones, and/or red nodular limestones, being locally rich in ammonites.
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The Stonebarrow cliffs are of Jurassic age, becoming geologically younger further east (the rocks of Golden Cap are early Cretaceous). The bottom of Stonebarrow is home to the Black Ven Marls a layer of rocks similar to those of Black Ven. Slightly higher are the Belemnite Marls, where a number of belemnites can be found. Slightly higher up is the Green Ammonite beds, where fossils of a species of ammonite exist.
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The Muschelkalk can be up to 100 meters thick; it is divisible into three subdivisions, of which the upper and lower are pale thin-bedded limestones with greenish-grey marls, the middle group being composed of gypsiferous and saliniferous marls with dolomite. Stylolites are common in all the Muschelkalk limestones. The lithostratigraphic status of the Muschelkalk differs regionally. In Germany it is considered a group, in the Netherlands a formation.
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The Lower Muschelkalk consists mainly of limestone, calcareous marls and clayey marls. Some beds are composed of porous cellular limestone, the so-called Schaumkalk, there are also oolite beds. The Lower Muschelkalk is divided into six formations: Jena Formation, Rüdersdorf Formation, Udelfangen Formation, Freudenstadt Formation and Eschenbach Formation. The Lower Muschelkalk is sometimes called Wellenkalk, the "wave" chalk, so called on account of the buckled wavy character the bedding has received.
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The site has been attributed to either the Maksimovka or Salibez Formations and compared to the Bembridge Marls and Florissant Formation, both of which are Priabonian in age.
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The Jabaco Formation consists of yellowish calcareous marls with abundant calcareous sandstone, in places compacted into marly limestone. The Jicotea Member is correlated with the Avon Park Formation of Florida.
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One fossil taxon is known, Copromorpha fossilis Jarzembowski, 1980 from the "Bembridge Marls" of Isle of Wight, a rock formation of Oligocene age, about 35 million years old (Jarzembowski, 1980).
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It occurs interbedded with oil shales or marls (Green River Formation, US) and in boron- bearing evaporite deposits (California, US); rarely in vugs in phonolite (Point of Rocks, New Mexico).
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The Yanigua Formation is a geologic formation in Dominican Republic. The lagoonal claystones and marls preserve fossils dating back to the Miocene period.Yanigua Formation at Fossilworks.org The formation hosts Dominican amber.
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A second Emplastus species was described by Cockerell from the Bembridge Marls as Ponera hypolitha. It was moved in 1964 to the fossil genus Poneropsis, and finally to Emplastus in 2014.
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The Middle Blesa Sequence is of a fairly uniform 25-50 metre thickness. Most of the sequence consists of the Josa Member, which consists of oyster rich marls and limestones deposited in a coastal or shallow restricted bay environment. The Upper Blesa Sequence is of variable thickness from 15–70 m. The lower 1–10 m consists of continentally derived clays and marls with sandstone and conglomerate intercalations while the upper 10–60 m are dominated by carbonates.
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Hiking walkway, Tustan Hill Fort The geology of the range is deep-sea sedimentary rocks of the Cretaceous and Paleogene ages - known as flysch - composed of sandstones, siltstones, argillites, limestones, and marls.
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Ironside is married to Karen Marls Dinwiddie. Michael and Karen have two daughters: Adrienne Lynn Ironside (from Ironside's previous marriage) and Findlay Ironside (born 1998). He has survived both thyroid and prostate cancer.
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The massif of the Trois-Évêchés consists of sedimentary rock, mostly sandstones and marls, typical of the pre-Alps. The geological nature of the north of the massif relates to the Ubaye Valley.
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It was first described by Matley (1951). Matley (1951) describes the August Town Formation as fossiliferous sands, gravels and calcareous marls. The August Town Formation is a part of the Coastal Group of Jamaica.
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The Köterberg is part of the Lippe Uplands a region whose basis is formed by Mesozoic strata of Muschelkalk and Keuper. The hills itself is built on sandstones and marls of the Upper Keuper.
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Copromorpha fossilis is an extinct species of moth in the Copromorphidae family. It was described from the Bembridge Marls of the Isle of Wight, a rock formation of Oligocene age, about 35 million years old.
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The site consists of sands and marls of the middle Lias with the remains of Gault and Upper Greensand capping. There are strong outflows of springs at various junctions of the upper greensand and gault.
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In the Lower Eocene (Ypresian), another transgressive period saw the sea advance north into the Médoc and south of Oléron; in the southeast it even reached the Montagne Noire. In the Aturian Gulf, Globorotalia-bearing marls were deposited, while farther east turritella-rich marls and limestones were formed. The newly inundated areas receive sands and limestones rich in alveolinids and nummulites. Meanwhile, iron-rich sands (in the Charente) and molasses (in the Libournais and in the Agenais) were sedimented in the continental north and northeast.
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The Pudovkino Formation (Russian: Pudovkino Svita) is a Late Cretaceous (Campanian) geologic formation in Saratov Oblast of European Russia.Pudovkino Formation in the Paleobiology Database Pterosaur fossils have been recovered from the marine marls of the formation.
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The basement is formed of red clays and marls overlaid by rocks of the Lower Muschelkalk. The summits are mostly composed of basalt. In most places the rock s covered by a layer of loam soil.
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To the east is the wide fertile Severn Vale, floored by Triassic 'New Red' sandstones and marls of the Mercia Mudstone Group (formerly known as the 'Keuper Marls'), and Jurassic lias clays further east. The Triassic deposits were formed in a Sahara -like desert when the British Isles lay about 15 degrees north of the equator, whereas the clays represent deep-water sediments. The landscape here is flattish, with the only feature of note a rather weak low scarp which meanders across the vale from SW to NE marking the Triassic/Jurassic border. This is superbly illustrated at the ‘Garden Cliff’, Westbury-on-Severn (see picture), where the river Severn has sliced a convenient ‘cut-away’ section of this transition from the red Triassic marls, through the thin Penarth Group (formerly 'Rhaetic') strata, to the lias clays and limestones of the lower Jurassic.
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The White Valley name comes from the abundance of white rocks noted by James H. Simpson in 1859.Van Cott, J. W., 1990, Utah Place Names, These rocks are mostly Lake Bonneville marls in the valley floor.
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It consists of sands with sandstone concretions, layers of silts, clays and marls. Age of the formation, according to a crude 1962 estimate, is Valanginian(?) - Hauterivian - Barremian. Its thickness varies greatly, reaching 746 m in Teguldet borehole.
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Jurassic tectonostratigraphy of the Austroalpine Domain. Journal of Alpine Geology 50: 1–152. Over the marls there is a series of dark shales that had intercalated siltstones, that mark the start of the main Krempachy Marl Formation.
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Visitors come to boat, swim or snorkel, and stay at one of the lodges located near Bay Street on the waterfront, though some adventurers reserve a day or two to kayak in the Marls on trips conducted by naturalist guides. The Marls are an extensive region of pristine mangrove habitat and open shallows called "flats" that harbour a rich variety of wildlife and offer an important fisheries, for local sustenance and for sport. In 2019, Marsh Harbour was directly impacted by category 5 Hurricane Dorian, severely damaging most structures and infrastructure in the city.
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The Trafraout Formation also recovers data from the post Toarcian Anoxic events on the Marocco Basin, with changes on the carbonate reserves on the lower layers, where hemipelagic marls suggest deposition after a change of the carbon cycle.
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The soil is light brown in color and is formed by lime-bearing sand and gypsum-bearing clays, lying on a subsoil of clays and marls. Its structure is granular, weak, not very rocky and lacking in organic material.
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205 though in many parts of the Tremp Basin the formation is exposed and covered by alluvium. The formation comprises several different lithologies, as sandstones, shales, limestones, marls, lignites, gypsum beds, conglomerates and siltstones have been registered.Arribas et al.
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There are high percentages of organic matter (3,42 %) associable to the presence of charcoal generated to low temperature; probably due to the pollution or the contact with the attached landfills or the percentages of carbonate (59,6 %) with the calcareous marls.
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The Itanhaém Formation is thick,Kiang Chang et al., 2008, p.32 and consists of dark grey shales, siltstones and light grey marls, ochre-brown calcisilts and subordinated sandstones. These facies change laterally into the coarse clastics of the Florianópolis Formation.
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The Marambaia Formation is between thick,Kiang Chang et al., 2008, p.32 and consists of grey shales and light grey marls interbedded with fine-grained turbiditic sandstones. The Marambaia Formation is the deeper lateral equivalent of the Iguape Formation.
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The Chalk Group consists of a sequence of chalky limestones with some interbedded marls. The age of the sequence ranges from Cenomanian through to Campanian, The upper boundary is an unconformity across which rocks of Maastrichtian to Paleocene age are missing.
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The Mupe Member is typically 11 to 16 m thick and largely consists of marls and micrites with interbeds of calcareous mudstone. The Ridgeway Member is about 3 to 7 m thick and consists of in its western portion carbonaceous muds, marls and micrites, in the east the muds are replaced by micritic limestone. The Warbarrow Tout Member is 17 to 39 m thick and consists of limestone at the base and micrite and mudstone for the rest of the sequence, this member is the primary source of the vertebrate fossils within the formation. Elsewhere the unit is undifferentiated.
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The Upper Carixian consists of very fossiliferous (Aegoceras capricornu) marly limestone layers interlayered with grey marls. These are followed by ammonite-bearing (Amaltheus margaritatus) and oyster-bearing (Gryphaea cymbium) marls indicating a shelf environment open to the spreading Atlantic Ocean. During the Lower Domerian, a connection to the Paris Basin is breached for the first time via the Seuil du Poitou and also to the Jurassic sea of southeastern France via the Détroit de Rodez and the Détroit de Carcassonne. During the Upper Domerian, another regression sets in leaving sandy limestones very rich in fossils (Pleuroceras spinatum, Pecten aequivalvis).
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The formation consists of limestones, yellowish calcareous marls and coastal conglomerates and fine calcareous sandstones. The Loma Candela Formation was deposited in a marine environment. It overlies the Universidad Formation and is correlated with the Tallahassee and Lake City Formations of Florida.
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Manganese deposits of Hungary. Economic Geology, 54(6), 1078-1094. The formation has a laminate Shale horizon associated with the Manganese Ores, with a transition of siliceous limestones and marls to black shales. Those are completed by the marl levels, composed by lithoclasts.
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The Guarujá Formation is thick,Kiang Chang et al., 2008, p.32 and consists of oolitic calcarenites, which laterally grade to greyish ochre and brownish grey calcilutites and grey marls. These facies are interbedded with the alluvial clastics of the Florianópolis Formation.
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Marine, limnic and finally terrestrial clays, marls, limestones and sands with interbedded basalt layers dominate within the Oligocene and Miocene. The Pliocene and Quaternary river deposits consist of sand, gravel and silt, in Pliocene also lignite. The recent landscape is formed by river terraces.
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419: "The carboniferous system is surmounted, to the east of the Volga, by a vast series of marls, schists, limestones, sandstones and conglomerates, to which I propose to give the name of "Permian System," … ." The region now lies in the Perm Krai of Russia.
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The Dinlence Formation overlies the Cemaller and consists of andesites and andesitic tuffites. It is possible that the Dinlence is the Yemislicay Formation since it too contains andesites and andesitic tuffites. The Dinlence is overlain by the marls, and limestones of the Alapý Formation.
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The 'Garden Cliff' at Westbury-on-Severn. Triassic marls of the Mercia Mudstone group. The green/grey streaks, known as 'Tea Green marls' are caused by ferrous oxide formed in reducing conditions Traditional building stone in the Severn Vale is scarce, necessitating brick or half-timbered construction in the main, although along the scarp mentioned above harder limestone bands in the Lower Lias (known as 'Blue Lias') have been used in vernacular building. Towards the east side of the Severn Vale the Lias clays are overlain by the sands and limestones of the Middle Lias - well displayed on the slopes of Robinswood Hill, a Jurassic outlier overlooking the city of Gloucester.
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The Marnes d’Auzas Formation (Auzas marls) is a geological Formation in southwestern France (departments of Ariège and Haute-Garonne) whose strata date back to the Late Maastrichtian. It is about 100 metres thick and consists primarily of marls with some interbeds of sandstones. It corresponds to sediments whose depositional environment evolved from the paralic domain (coastal lagoons, tidal marsh, tidal muddy channel) at the base of the formation, towards a more continental domain (alluvial plain, fluvial channels) in its upper part. The Marnes d’Auzas Formation was deposited in the west coast of the former Ibero-Armorican Island, which included much of France and Spain.
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The coast, constituted by a sub-zone of more recent materials, Quaternary or Neogenic in age. These deposits came to rest over sand-stones and marls that comprise the coastal Mesocenozoic, a young relief, that is little accented, aided by a platform that includes superficial lavas.
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20 The formation mainly consists of marls and turbiditic sandstones and conglomerates deposited in the northeastern part of Hispaniola.Díaz de Neira, 2017, p.663 The formation overlies the Los Hidalgos Formation and is overlain by the La Jaiba Conglomerate and in places by the Villa Trina Formation.
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Pitting sometimes found has been linked to rain pitting but may have occurred during the de-gassing of the marls during drying out. The banded strata which may be red or grey pass up into blocky unstratified mudstones (broken up and allowed to resettle before consolidation).
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The Antalo Limestone, also known as the Antalo Sequence, is a geological formation in Ethiopia. It is between 300 and 800 metres thick and comprises fossiliferous limestones and marls that were deposited in a reef. Marine microfossils have shown an age between 165 and 150 million years.
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The Iguape Formation is thick,Kiang Chang et al., 2008, p.32 and consists of bioclastic calcarenites and calcirudites, containing bryozoa, echinoids, corals, foraminifera, fragmented shells, and algae remains. They are interbedded with grey-greenish clays, siltstones, marls and variegated grey fine-to-medium grained conglomerates.
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The marls of the main formation strata are covered on Ammonite fragments, intercalated with Dinoflagellates.Schlögl, J., Košt’ák, M., & Hyžný, M. (2012). First record of a gladius-bearing coleoid Teudopsis bollensis Voltz (Cephalopoda, Coleoidea) in the Toarcian of the Western Carpathians (Slovakia). Paläontologische Zeitschrift, 86(4), 367-375.
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Chomérac is located on the eastern foothills of the Massif Central, away from the Rhône, in a large valley incised in cretaceous marls by the Payre and Vérone rivers, south east of the Jurassic limestone plateau of Les Grads and north of the Miocene basaltic plateau Les Coirons.
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It commonly splits to form a double layer with localised areas of a marl complex up to 2 cm thick. Separating the upper and lower Wootton Marls is white chalk, containing discrete nodular flints up to 40 cm thick.Chidlaw N. (); The Valley, Wold Newton, Site Report, Gloucestershire Geology Trust.
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The site is part of the East Devon dissected plateau, composed of calcareous upper greensand capped by clay, Flints and chert, and overlying Keuper marls. The north part of the site is 225 metres above sea level and the ground slopes steeply to the south down to 150 metres.
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The regression continued during the Lower Sinemurian, sedimenting intra– and supra–tidal banded limestones and dolomites. In the Upper Sinemurian (Lotharingian), more open-marine conditions established themselves due to a renewed sea-level rise; in deeper parts of the basin, fossiliferous limestones developed, whereas, on high ground, oolithic limestones accumulated. The Middle Lias (Pliensbachian) started off transgressive as well with fine-grained detrital, limey to marly sediments (ferruginous oolites, fossiliferous limestones and marls) that change over to marls. In the eastern Pyrenees, pyrite-bearing claystones formed due to a badly oxygenated environment; they contain a very diverse fauna of ammonites belonging to the French southeastern domain, whereas the ammonite population on the Atlantic side is rather monotonous.
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The dominant carbonate mineral in most marls is calcite, but other carbonate minerals such as aragonite or dolomite may be present. Scheme of the transitional lithotypes from mud (or mudstone) to lime (or limestone), illustrating the definition of marl (marlstone) as a mix of calcium carbonate and clay The lower stratigraphic units of the chalk cliffs of Dover consist of a sequence of glauconitic marls followed by rhythmically banded limestone and marl layers. The Channel Tunnel follows these marl layers between France and the United Kingdom. Upper Cretaceous cyclic sequences in Germany and marl–opal-rich Tortonian-Messinian strata in the Sorbas basin related to multiple sea drawdown have been correlated with Milankovitch orbital forcing.
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In areas unaffected by the Templeton Delta, depositional rates were low, producing a condensed section composed of organic-rich, calcareous marls, limestones, and volcanic ash beds in both South Texas and West Texas. The microfossils found within the marls are predominantly coccoliths and planktonic foraminifera, whereas the limestones contain abundant radiolaria and calcispheres (calcareous cysts produced by some dinoflagellates). Inoceramus fragments and fish bones are also found in these deposits. During the Late Cenomanian the Sabine Uplift along the modern-day Texas/Louisiana border became active, causing erosion of Eagle Ford and Woodbine sedimentsHalbouty, M. T., and J. J. Halbouty (1982) Relationships between East Texas field region and Sabine uplift in Texas: AAPG Bulletin, v.
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The marls have not preserved any Symphyta hymenopterans such as Tenthredinoidea species, suggesting that the paleotemperature of the marls was as warm or possibly warmer than either the Baltic amber or Florissant Formation forests, while the presence of the wasp family Scelionidae suggests generally mesic moisture conditions. Since the genus and first species descriptions, another series of species have been described from fossils found in Russia. The three species were described from compression fossils preserved in diatomite deposits of the Bol’shaya Svetlovodnaya site. Located in the Pozharsky District, on the Pacific Coast of Russia, the fossil bearing rocks preserve possibly Priabonian plants and animals which lived in a small lake near a volcano.
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The Upper Bedoulian Formation is a geological formation in the Murcia Region, Spain whose strata date back to the Early Cretaceous (late Barremian to early Aptian stage). The marls were deposited in an open marine environment. The lower unit ( thick) is marly with iron concretions and septaria.Upper Bedoulian Formation at Fossilworks.
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The geology of Tule Valley consists of Quaternary alluvial sediments punctuated by chalky white Pleistocene marls. The valley is a true graben in the sense that it is down-faulted by normal faults on both sides of the valley. The knolls in the valley are horsts of Silurian to Devonian carbonates.
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The Zaza Formation is a geological formation located in Buryatia (Russia). It dates to the Lower Cretaceous period. It is Aptian in age and consists of sandstones, siltstones, marls and bituminous shales, deposited in a stratified lake. It is situated on a large granite plateau in the NE of Buryatia.
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The Consuelo Formation was described by Bermúdez in 1950 based on a section of marls in the Consuelo El Tejar quarry in La Habana Province.Gutiérrez Domech, 1969, p.32 The formation overlies the Príncipe and Capdevila Formations with an unconformity,Gutiérrez Domech, 1969, p.33 and is overlain by the Tinguaro Formation.
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Fossil specimens have been found in the Lushi Formation of Mengjiapo, China, in Weisserburg, Germany and Les Saleres in the Ager Basin of Spain, the Bembridge Limestone and Bembridge Marls Formations of the Isle of Wight, Great Britain as well as the Perrière and Quercy Phosphorites Formations and La Débruge in France.
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Gypsisols have been developed on plaster marls of the trias. They sit in the gentle hills of the countryside. They have carbonates so they are classified as calcium gypsisols. They have a low content of organic matter, alkaline pH, are usually muddy clay or clay, dry hard and compact and wet plastics.
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The Sakaraha Formation consists of sandstones, marls and carbonates and represents a coastal plain environment, and is laterally equivalent to the predominantly carbonate Bemaraha Formation, which represents a coastal barrier lagoon complex. The formation is found in the northwest and in the southeast of the country and has provided a variety of fossils.
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M. Broshi and H. Eshel, "Three Seasons of Excavations at Qumran," Journal of Roman Archaeology, 17/1, 2004, pp. 321–32. In 2004, they had the opportunity to return and investigate the empty areas in the marls of Cave IV, but with little result.Bill Kurtus, Investigating History: The Dead Sea Scrolls, May 2004.
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The San Juan Formation () is a geologic formation in Argentina. The formation comprising limestones, mudstones and marls was deposited in a shallow marine reefal environment and preserves many fossils dating back to the Ordovician period. The formation overlies the La Silla Formation and crops out in the Precordillera of San Juan Province.
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The Helvetic zone consists of a number of tectonically very different units. The "Helvetic nappes" are a nappe stack that was thrusted over the molasse of the Molasse basin in the Alpine foreland. They are composed of Mesozoic marine limestone, marls and shales. The Helvetic nappes are completely detached from their former basement.
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Piotruś itself is formed of Oligocene age rocks, particularly the Menilite Beds, which contain the Mszanka Sandstones, the Jawornik Marls the Cergowa Sandstones or Shales with interbedded layers of Tylawa Limestone. Prominent ridges near the top of the mountain consist of thick-bedded layers of sandstone and conglomerate that form part of the Mszanka Sandstones.
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The Xiaowa Formation has three members. The lower member is relatively thin but is also very fossiliferous. It begins with thick-bedded grey biomicrite (fine-grained fossiliferous limestone) interbedded with greenish shale. Bivalves and crinoid fragments are the most common fossils in the biomicrite layers, which sometimes grade upwards to dark grey laminated marls.
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Charterhouse Wireless Station in the Mendip Hills To the north of Bath are Lansdown, Langridge and Solsbury hills. These are outliers of the Cotswolds. Bath is noted for its thermal waters (48 °C) that are rich in calcium and sodium sulphates. The Old Red Sandstone is a series of red sandstones, marls and conglomerates.
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The marls was colonized by pioneer species, then shrubs and trees, corresponding to a primary succession. Without human intervention, a climax community would be reached. This dynamic may eventually lead to the disappearance of related open environments, particularly heritage species. However woodlands can also play an important role in creating habitat for many species.
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The Cascate del Rio Verde in August. Cascate del Rio Verde, located in Borrello are the highest natural waterfalls in the Italian Apennines. Cascate del Rio Verde consists of three jumps for a total of over 200 meters. The panorama is made up of rocks, made up of calcarenites and marls resting on clay.
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Anthony's Church) in Davenport.Svendsen, Marls A., Davenport: where the Mississippi Runs west A Survey of Davenport History & Architecture (Davenport: City of Davenport, 1982) 11-2. The Dubuque Diocese now covered roughly the northern half of Iowa. An advocate of Catholic education, Hennessy had schools and convents established in all of the large cities in Iowa.
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For example, the rock gardens at Hessigheim. They lie on the marls and clays of the middle Muschelkalks and can sag in whole stone packages, so-called Schollen, down towards the Neckar. In the Odenwald narrow ravines and gorges lead into the Neckar from both sides, as for example, the Wolfschlucht and the Margarethenschlucht.
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3 The formation, with a minimum thickness of ,Rincón et al., 2014, p.510 has formerly been regarded as Late Oligocene in age (Wheeler, 1960), but more recent workers, regard it to be Early Miocene. The Castillo Formation at Cerro La Cruz comprises of clayey marls, interbedded with numerous thin (less than ) hardground units.
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The Hornitos Formation is a Campanian geologic formation of the Algarrobal Basin in the Atacama Region of northern Chile. The formation comprises limestones, sandstones, conglomerates, marls and tuff. Dinosaur remains are among the fossils that have been recovered from the formation, although none have yet been referred to a specific genus.Weishampel, et al. (2004).
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The Allgäu Formation is a geologic formation in Austria. It preserves fossils dating back to the Hettangian to Sinemurian stages of the Early Jurassic period, or Raricostatum to Obtusum in the regional stratigraphy. Initially and formally defined by Jacobshagen (1965).Jacobshagen, 1965 The Allgäu Formation is formerly known as spotted marls (Lias-Fleckenmergel) and spotted marly limestones (Fleckenkalk).
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In the Triassic the Ceratite beds, named after the ammonite ceratite, consist of arenaceous limestones, calcerous sandstones and marls. The Jurassic consists of two distinct units. The Kioto limestone, extends from the lower the middle Jurassic with a thickness to . The upper Jurassic is represented by the Spiti black shales, and stretches from the Karakoram to Sikkim.
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Some authors describe a third member: the Maasmechelen Member, but this is alternatively seen as part of the Eisden Member. The Opglabbeek Formation has a thickness between 20 and 60 meters. It lies stratigraphically on top of the Houthem Formation (early Paleocene calcareous sandstone). On top of it lies the Heers Formation (Middle Paleocene sands and marls).
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Located in the Pozharsky District, on the Pacific Coast of Russia, the fossil bearing rocks preserve possibly Priabonian plants and animals which lived in a small lake near a volcano. The site has been attributed to either the Maksimovka or Salibez Formations and compared to the Bembridge Marls and Florissant Formation, both of which are Priabonian in age.
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The outermost edge of the basin structure consists of harder rock layers of the Upper Keuper (Ko) Rätkeuper. In the Tertiary it came in the inner basin edges consisting of gypsum Keuper to the dissolution of plaster layers. Through this process, also called subrosion, formed hollows. These were backfilled with the weathering marls from the immediate area.
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Oligobombus cuspidatus was described by Antropov in 2014 from the Insect Bed of the Bembridge Marls in the late Eocene of the Isle of Wight, England. The fossil was described by re-examining a specimen in the Smith Collection. The collection was originally made by A'Court Smith, and purchased by the Natural History Museum in 1877 and 1883.
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Ammonites like Collignoniceras peramplum, Eutrophoceras sublaevigatus, Lewesiceras peramplum, Mammites revelieri and Spathites reveliereanum as well as nautiloids like Nautilus sublaevigatus are only rarely encountered. The microfauna is not very diversified either, present are ostracods (in the marls), textulariids and pelagic forams (Hedbergella delrioensis, Heterohelix, and Globotruncana). Some discorbids and some benthic forams like Dorothia sp., Marsonnella oxycona, Eggerella sp.
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At the base of the range is the pink/orange Notch Peak granite and monzonite, which is Jurassic in age (143 to 169 million years old).Lee et al., 1986, U.S. Geological Survey Bulletin 1622, p. 31-40.Stokes, 1986, Geology of Utah, Around Notch Peak, especially from the west side (Tule Valley side), white Lake Bonneville fossiliferous marls occur.
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The Caimito Formation (Tcm)Geologic Map, 1980 is a geologic formation in Panama. The marls, sandstones and conglomerates preserve bivalve and gastropod fossils dating back to the Late Oligocene to Early Miocene period.Caimito Formation at Fossilworks.org The name Caimito was proposed by MacDonald in 1913, named after the Caimito junction in the Panama Railroad during the construction of the Panama Canal.
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It is plausible that this fall in sea level correlates with the onset of glaciation in Antarctica at the beginning of the Oligocene. The Eocene/Oligocene boundary most likely is situated below the sequence boundary in the Lower Hamstead Member or high in the upper Bembridge Marls Member. Remark: This interpretation proposed by Hooker et al. (2009) is not accepted by all geologists.
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The Xiaowa Formation is a Carnian-age geological formation found in southern China. It is a sequence of limestone and marls from the Carnian stage of the Triassic. Its lower section was previously known as the Wayao Formation or Wayao Member of the Falang Formation. Crinoids and marine reptiles are abundant in the Xiaowa Formation, forming a lagerstätte known as the Guanling biota.
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This transitional layer consists of red sandy gypsum bearing beds interbedded with marl and limestone. Exposed areas of the older Cretaceous Germav Formation can be seen in small areas of the Mardin High. The exposed Germav consists of shale, but has and a slow transition into more marls and limestones toward the bottom of the formation toward the Lower Cretaceous Mardin Limestone.
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The Guarujá Formation () is a geological formation of the Santos Basin offshore of the Brazilian states of Rio de Janeiro, São Paulo, Paraná and Santa Catarina. The predominantly calcarenite formation with marls dates to the Early Cretaceous period; Early Albian epoch and has a maximum thickness of . The formation is the second-most important post-salt reservoir rock of the Santos Basin.
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The formation of the fault system closer to the coast caused the initial development of the Exmouth, Barrow, and Dampier sub-basins of the Northern Carnarvon Basin. Carbonate marine sediment, primarily marls, continued to be deposited at this time on the central and western portions of the plateau. Closer to the shoreline siliciclastic mud and silt were deposited from marine and deltaic environments.
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Various radiolarians under the microscope Lithologically the up to 50 meter thick Ruhpolding Formation consists of black-green to red radiolarites grading into cherty limestones, cherty marls and cherty shales. It has formed from radiolarian ooze. The ooze consolidated diagenetically to thinly layered and regularly banded cherts. The chert layers are usually separated by very thin claystone layers creating a cyclic appearance.
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Robinson, David N. (2009); The Lincolnshire Wolds. The most interesting geological feature in Wold Newton is a "marker unit" of stratigraphic value, recorded by the British Geological Survey, which can be found in the chalk pit at the west end of the Valley. The marker unit is known as the Wootton Marls. This marl is grey in colour and about 1 cm thick.
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In the Lower Eocene, Basin conditions became restricted, producing an alternating dolomite and anhydrite sequence with a consistent thickness. The mid-Eocene saw development of a wide carbonate platform, richly nummulitic, also constant in thickness. There are argillaceous limestone interbeds, marl, and occasional calcareous sandstones. The Late Eocene reflects more frequent lateral variations of interbedded limestones, dolomites, marls, and shales.
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Lithologically, these sediments are limestones, marls, glauconitic sandstones and rarely clays and conglomerates. Tskaltsitela River Geocaching. In the vicinity of Tskaltsitela river there are many natural quarries with chalcedony, barite, quartz sand, marble, basalt, agate, fireproof clays used for cement production, teshenit and other minerals. Coal mining has been under way in the vicinity of Tkibuli since mid-XIX century.
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The adjective "argillaceous" is also used to define rocks in which clay minerals are a secondary but significant component. For example, argillaceous limestones are limestones consisting predominantly of calcium carbonate, but including 10-40% of clay minerals: such limestones, when soft, are often called marls. Similarly, argillaceous sandstones are sandstones consisting primarily of quartz grains, with the interstitial spaces filled with clay minerals.
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Beds are often laminated and invertebrate fossils (gastropods, bivalves, brachiopods, echinoids and isolated coral fragments) are common in some beds, while others are devoid of fossils.D'Orazi Porchetti et al., 2010, p.8 In the south-western Majunga Basin, interbedded limestones and mudstones (shales and marls) above the Aalenian Sandstone were attributed to a Bajocian carbonate platform formed by the Bemaraha Formation.
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Lymnaea tomentosa hamiltoni is an extinct subspecies of freshwater snail, an aquatic gastropod mollusc in the family Lymnaeidae, the pond snails. This species was endemic to New Zealand.Powell A. W. B., New Zealand Mollusca, William Collins Publishers Ltd, Auckland, New Zealand 1979 The shells of these snails were found in lake marls in the southern part of the South Island.
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At the time when the limestones and dolomites of the White Jura were being deposited, this sea was divided into sponge reefs and intervening lagoons. The reef bodies and the fine-grained lagoon limestones and marls are the material from which the majority of the Franconian Jura is composed today.Stefan Glaser, Gerhard Doppler and Klaus Schwerde. (eds.): Stefan Glaser, Gerhard Doppler und Klaus Schwerd (Red.): GeoBavaria.
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The 10-meter-thick Lower Hamstead Member follows directly upon the Bembridge Marls Member with a 40-centimetre-thick olive to black seam, the Black Band. This layer is very rich in organic matter and was deposited under freshwater conditions. At its base it carries calcrete nodules and rootlets. The Black Band is overlain by roughly 4 metres of a greenish- greyish clay-silt interlayering.
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The Helvetic nappes () are a series of nappes in the Northern part of the Alps and part of the Helvetic zone. They consist of Mesozoic limestones, shales and marls that were originally deposited on the southern continental margin of the European continent. During the Alpine orogeny they were thrusted north over a décollement and at the same time were internally deformed by folding and thrusting.
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25-33 Later sinistral transtension and lateral extension modified the structure of the belt during the Late Miocene and Pliocene. Extensional deformation on the eastern and western edge of the belt interacted with development of the Vienna and Transcarpathian basin. After the marine regression at the end of Miocene younger marls and turbidites were eroded faster than more competent Jurassic limestones forming distinctly looking klippes.
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The Chulec Formation (Ki-chu) is a geological formation in Peru whose strata date back to the Albian. The formation has a thickness of about and comprises limestones, marls and calcareous sandstones that were deposited during a marine transgression from the west.15 km east of Huanzala Mine at Fossilworks.org Pterosaur remains and ammonites are among the fossils that have been recovered from the formation.
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During the Upper Lias (Toarcian), the sea reached a high stand, continuing with the fine-grained detrital sedimentation and depositing black pelagic marls (marnes noires and schistes esquilleux). Towards the end of the Lias, regressive tendencies again became noticeable. Falling sea levels continued right into the Middle Jurassic. Near Pau an oolite barrier started to grow that extends all the way north to Poitiers.
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In the 1960s, the Army transmitted the first photograph via facsimile (fax) to Puerto Rico from the site using the Courier satellite. In 1823/1824, long before the land became a test site, a Late Pleistocene/early Holocene mastodon was excavated from a peat bog on the south side of Poplar Brook. Fossil vertebrate remains were also found from the Tertiary marls along the brook.
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Château de Beynac is built on Upper Coniacian limestone Geologically, the Périgord noir area is situated entirely in a sequence of gently southwest-dipping sediments that form part of the Aquitaine Basin. The series comprises Jurassic, Cretaceous, Eocene and Oligocene. The river valleys are infilled by alluvial sediments of Quaternary age. The Jurassic sediments belong to the inner platform facies and consist of limestones, dolomites and marls.
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The stratigraphic column begins with the Lower Jurassic Liassic at about 4700 m followed by the Late Jurassic Dogger, the gas producing dolomite in the Portland Group, Purbeckian-Waeldian sandstone, and Valanginian-Neocomian limestone and dolomite, followed by the Albian-Aptian marls and limestones.Winnock, E., and Pontalier, Y., 1970, Lacq Gas Field, France, AAPG Memoir 14: Geology of Giant Petroleum Fields, Tulsa: AAPG, pp. 375-378.
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Wete District is on Pemba Island and nearby islands in the Indian Ocean off the coast of East Africa. The islands themselves are composed of sedimentary rocks deposited during the Neogene and Quaternary consisting of mostly limestones and sandstones with marls and some shale, as well as unconsolidated sands and clays. The sediments are nearly flat laying producing a gently undulating and rolling plain.
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The Itanhaém Formation () is a geological formation of the Santos Basin offshore of the Brazilian states of Rio de Janeiro, São Paulo, Paraná and Santa Catarina. The predominantly shale formation with marls, siltstones and sandstones dates to the Early Cretaceous period; Early Albian epoch and has a maximum thickness of . The formation is the reservoir rock of the Tambaú Field in the Santos Basin.
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During this upper Jurassic period, the deposition of oolitc limestones, shales and carbonated cemented sandstones were deposited in the basin. The deposition of these sandstones creates ideal seismic reflectors to aid in the understanding of formations deep within the Jeanne d'Arc Basin. In the middle Kimmeridgian the deposition of the Egret source rock occurred. This source rock is composed of marls and organic rich laminated shales.
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The India–Madagascar–Seychelles separations appear to coincide with the eruption of the Deccan basalts, whose eruption site may survive as the Réunion hotspot. The Seychelles and the Maldives are now separated by the Central Indian Ridge. During the initial break-up in the Early Jurassic a marine transgression swept over the Horn of Africa covering Triassic planation surfaces with sandstone, limestone, shale, marls and evaporites.
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Both rock types enclose the same fauna as the first member. The second member likewise can change its facies to calcarenites of the beachrock type. (These calcarenites persisted near Paussac and near Toulon (Périgueux) right from the lower Angoumian onwards). The upper Angoumian closes with about 5 m (to as much as 15 m in places) of grey to yellow, platy, marly limestones interlayered with yellow marls.
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In addition, examination of their context of deposition shows that the objects are not in 'special' locations, but were discarded, often in middens. A study of the fabric of the figurines by Chris Doherty (pers. comm.) has shown that they are made of local marls and that they are unfired or low fired. Many have survived only because they were accidentally burned in hearths and fires.
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The Ariri Formation, originally deposited as flat evaporite layers, has undergone extensive diapirism and canpoy formation during the Albian to Paleocene. The Ariri Formation is in the thick and may be up to thick in other areas of the basin. It is predominantly composed of evaporites. The formation is characterized by thick intervals of white halite, associated with white anhydrite, ochre greyish calcilutites, shales and marls.
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Nizza vines are sun-demanding and normally occupy the best-exposed slopes that face from southeast to west; the valleys are excluded. The production area is the focus of the so-called Tertiary Piedmont Basin, a hilly region that originated from the lifting of the seabed during the late Tertiary epoch; the soils are calcareous, of medium depth, and characterized by sandy-clay marls and stratified sandstones.
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The site has exposures in the Raglan Marls (topmost) of the Lower Devonian time period (up to the level of the Psammosteus Limestone). The section includes calcrete profiles and a complex sand-body. The sandstone has fish fragments. The outcrop is significant for research in assessing the extent of marine tidal influence on the sequence in the Lower Old Red Sandstone (below the Psammosteus Limestone).
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Uplighter lamp, white and brown Italian alabaster, base diameter 13 cm (20th century) In Europe, the centre of the alabaster trade today is Florence, Italy. Tuscan alabaster occurs in nodular masses embedded in limestone, interstratified with marls of Miocene and Pliocene age. The mineral is worked largely by means of underground galleries, in the district of Volterra. Several varieties are recognized—veined, spotted, clouded, agatiform, and others.
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By 22 million years ago, the Alpine foreland was flooded again due to tectonic subsidence. A shallow (intertidal) marine environment formed from Lyon to Vienna. In this environment the third formation, the Upper Marine Molasse (German: Obere Meeresmolasse), was formed. It consists of marine sands, clays and marls and new fan conglomerates and is of Burdigalian to Langhian age (early Miocene, 22 to 16 million years old).
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Generally the same sedimentary types are present in the marls as are in the waterstones but with less arenaceous and more argillaceous material. An irregular rhythm is discernible, each sedimentary cycle is well developed and have banded or stippled beds at the base. It is in this banded stratum that features such as sun cracks are found. Ripple marks are less common but they are evidence of deposition in shallow water.
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Amongst the fish Amia sp. and other amiids have been found The fossil contents of the Bembridge Marls Member are quite varied, with freshwater species like Lymnaea and Unio and marine taxa like Melanopsis, Meretrix and Ostrea. The Bembridge Insect Bed at the base of the member is a marly sand layer with a very rich insect fauna and many leaves. This layer constitutes a lagerstätte with very good preservation.
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According to Haynes, 'black mat' is a general term that also includes the similar other deposits of various shades of grey or even white, because some Younger Dryas marls and diatomites are actually white to grey in colour. Also, at least at the Murray Springs Clovis Site, raised levels of radioactivity were associated with the mat. This radioactivity had not been there before the mat formed. Magnetic grains were also found.
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The Seaspray Group lies unconformably above the Latrobe Group, and was deposited in the Oligocene to the Miocene. This group makes up the majority of the seals in the region due to the unconformity with the Latrobe Group, as well as the low permeability of the rock types, which include shales, marls, limestones, calcareous claystones, siltstones, and sandstones. The typical depositional environments of these rock types, are low energy marine environments.
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The Hibernian Greensands Group is a late Cretaceous lithostratigraphic group (a sequence of rock strata) in Northern Ireland. It is Cenomanian to Santonian in age. The name is derived from the characteristically coloured marls and sandstones which occur beneath the chalk particularly along the Antrim coast. The strata are exposed on or near to both the northern and eastern coasts of Antrim and also between Portrush and Dungiven within County Londonderry.
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Part of the formation in the west is composed of carbonates (domal stromatolites with an east to west orientation and thin laminae of less than ). The stromatolites occur in a wide zone, reaching from east of the Uniab Fault to east of the Bergsig Fault system. The eastward sections comprise oolitic conglomeratic horizons of up to thick. The carbonates (mudstones and marls) are overlain by silty, partly calcareous shales.
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In Flanders, sands, gravels and marls predominate, covered by silts in places. The coastal strip is sandy but a short way into the hinterland, the ground rises towards the Vale of Ypres, which before 1914 was a flourishing market garden. Ypres is above sea level; Bixschoote to the north is at . To the east the land is at for several miles, with the Steenbeek river at near St Julien.
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In some locations, such as Gaissau, the Saubach Formation is dominated by red condensed limestones with only minor marl intercalations. In 1997 the name Saubach Formation was suggested, representing originally a series of Green Bituminous Marls on the Unken Sincline, identical to the strata of the Saubach Member of the Adnet Group.Krainer, K., & Mostler, H. (1997). Die Lias- beckenentwicklung der Unkener synklinale (nördliche Kalkalpen, salzburg) unter besonderer berücksichtigung der scheibelberg Formation.
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This reflected its place in the industrial revolution which came very late to Bromyard, partly because it took so long to connect the town to the railway system. A sandstone quarry was opened at Linton, just east of the town, in the 1870s, but the hopes for extensive sales of good quality building stone were disappointed and by 1879 it was producing bricks and tiles from the Old Red Sandstone marls.
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Fault, on the coast of Somerset near Carhampton The Triassic rocks consist of red marls, sandstones, breccias and conglomerates which spread over the older rocks. The Dolomitic Conglomerate is an old shingle beach of Keuper Marl age. The Rhaetic Beds are full of fossils due to invasion of the Jurassic Sea. The Lias consists of clays and limestones, the latter being quarried and are famous for their fossils.
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The Praia Azul Member, formerly known as the Sobral unit/member is 80 to 130 metres thick and consists of tabular marls and mudstones, with rare sandstones bodies.There are three distinct laterally extensive (>20 km) thin shelly carbonate horizons within this member, indicating brief marine transgressions. South of Santa Cruz primarily consists of sandstone with rare conglomerate. The age is considered to be latest Kimmeridigan to earliest Tithonian.
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Panorama The little rainfall that occurs is usually torrential, so that the ground, consisting of marls and sandstone with little vegetation, is unable to retain moisture. Instead, the rain causes erosion, forming the characteristic landscape of badlands. Arroyos formed by torrential rain harbor the scarce vegetation, as well as fauna such as swifts, hedgehogs, jackdaws, pin-tailed sandgrouse, blue rock thrushes, stone curlews, trumpeter finches, and crested larks.
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The Lias Group or Lias is a lithostratigraphic unit (a sequence of rock strata) found in a large area of western Europe, including the British Isles, the North Sea, the Low Countries and the north of Germany. It consists of marine limestones, shales, marls and clays. Lias is a Middle English term for hard limestone, used in this specific sense by geologists since 1833.Oxford English Dictionary, s.v. "lias".
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The strata of the formation is composed by grey-blue marl & limestones. The formation overlies Sinemurian to Pliensbachian deposits of the Orava Unit, where there is disposed a southwest bedding dipping. The lowermost part of the strata recovers spotted limestone beds & alternations of dark Marls that are equivalent to the uppermost Allgäu Formation.Gawlick, H.-J., S. Missoni, F. Schlagintweit, H. Suzuki, W. Frisch, L. Krystyn, J. Blau, and R. Lein. 2009.
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This Bembridge Marls species was described from a set of five solitary wings from males and females. The female forewings have lengths ranging between while the smaller male wings are generally . The vein structure is similar to that of E. britannicus though the wing size of the latter is smaller. E. kozlovi also differs in the proportioning of the triangular rm cell, which is longer than in E. britannicus.
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The territory of Rodez is packed with geological diversity. It straddles on the ancient base of Ségala composed of acidic siliceous earths of Les Rougiers to soil consisting of red argillite, and causses composed of limestones and marls. The city was built on a conical isolated terrain, locally called Le Piton, and gradually spread to the surrounding slopes. It is located in a level 2 zone of seismicity, in other words at a low level.
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There are marls present in some of these formations and bands of flint nodules occur to varying degrees in each of these units. The main outcrop of the Chalk forms the South Downs, the West Sussex portion of which runs broadly westwards from Brighton to the county's western border with Hampshire. Further outcrops are concealed beneath Quaternary sediments in a discontinuous low-lying strip from Worthing, north of Chichester to the Hampshire border.
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The aquifer at the origin of this plateau is at the seat of sandstone beds infraliasic of the Lower Rhaetian. The lower bed is made of iridescent marls from the Upper Keuper. The springs which flow out of this aquifer are at an elevation of about . The dominant east-west direction of the middle to lower course of the Apance, notwithstanding a southerly-oriented diversion, results from the orientation of main faces of the sides.
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Exclusively nonmetamorphic sedimentary successions are composed especially of limestones and marls. In the Jurassic period, the ocean that opened in the area of the Pieniny Klippen Belt is called the Vahic Ocean (or the South Penninic). Its preserved sedimentary successions are in the present erosion cut known only from the Vahic unit. The Vahic domain was bounded from the North by the slopes of the Oravic, and from the South by the Tatric unit.
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Thomas was stationed near Constantine, and was friends with Tissot between 1874 and 1880. When he told Tissot of his findings, Tissot was very interested. Tissot said he was not surprised, because he had always thought these marls or limestones must have phosphate since they produced the best corn fields in the province. Tissot reproduced this observation in a note on Algerian mineralogy he wrote for the Paris Exposition Universelle of 1878.
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Above these he found hard sandstone, alternating marls and soft sandstones from the Late Miocene or the Pliocene, and then an upper layer of sand and clay sandstones rich in fossils. He then studied the very difficult regions of Mateur, Beja and Kef. He confirmed earlier observation of phosphate deposits with commercial potential. At Djebel Zaghouan in Tunisia Le Mesle found Jurassic terrain in which Kobelt had discovered Perisphinctes Kobelti from the Oxfordian age.
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Geologisch- Paläontologische Mitteilungen Innsbruck, 22, 1–41. Later was showed that the Saubach Member and the Saubach formation belong to a unique entity, that can be called by both names, and represent a series of marls deposited on marginal marine to Pelagic environments, linked with the Red Marl of the Sachrang Formation.Gawlick, H., Missoni, S., Schlagintweit, F., Suzuki, H., Frisch, W., Krystyn, L., ... & Lein, R. (2009). Jurassic Tectonostratigraphy of the Austroalpine domain.
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The fold trends follow more or less the pyrenean direction or parallel to the thrust fronts, but turn NE-SW near the Segre River (e.g. the Oliana Anticline). The sedimentary succession in the Ebro Basin shows Paleozoic rocks at the base followed by uppermost Cretaceous/lowermost Paleocene red beds and Eocene limestones, marine marls, and Upper Eocene evaporites (Cardona evaporites). The lower Oligocene is conglomeratic and pro-grades southward into evaporite and lacustrine deposits.
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In the western Pyrenees, the marine sedimentation also carried on during the Eocene. In two subsiding basins on both sides of today's chain, limestones, marls, foraminiferous sandstones, and sandstones with a benthic fauna were sedimented. The Eocene sedimentary successions along the French northern edge of the Pyrenees (in the North Pyrenean Zone) are fairly thin and full of facies changes. There, short-lived transgressions and regressions can be followed into the Languedoc.
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The Tereñes Formation or Tereñes Marl is a Late Jurassic (Kimmeridgian) geologic formation in Asturias, Spain. The grey marls of the formation were deposited in a lagoonal environment at a muddy coast along a temporary inland sea. The lower section of the formation comprises silty and chalky sandstones with desiccation cracks and ripple marks, then becomes a bituminous, prominently ostracod-bearing, pelecypod shell chalk, lime chalk marl and marl.Tereñes Formation at Fossilworks.
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The Tristel Formation is a stratigraphic formation of the northern-central Alps, deposited between the late Barremian and the early Aptian of the Early Cretaceous. It consists of thickly banked limestones, marls and shales. It is the lowest formation of the Bündnerschiefer and belongs to the Rhenodanubic Group. Outcrops can be found in the Engadin window, the Tauern window, the Rechnitz window, and many localities of the Penninic realm of the eastern and western Alps.
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Prohepialus is an extinct genus of insect of uncertain phylogenetic placement. It was originally identified as a moth in the family Hepialidae; however, Simonsen, Wagner & Heikkilä (2019) considered it more likely to be a symphytan wasp. It contains only one species, Prohepialus incertus, which was described from a Thanetian crater lake diatomite (Paleocene) in Menat (Puy-de-Dôme), France. A second specimen is known from the Bembridge Marls (Eocene) in the United Kingdom.
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The cliffs either side of Eype and the coastal stretch between Thorncombe and Watton Cliff provide the best view. The base of the middle Lias is composed of three thick layers of calcareous sandstone beds separated by marls. These resistant bands form massive buttresses along the sea-cliffs and, where eroded, boulder aprons on the foreshore. Above these three layers is the Eype clay, which was probably deposited in deeper, calmer waters.
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From Dunraven to Aberthaw, the coastal cliffs feature blue and brown argillaceous limestones, shales, and marls. As far as East Aberthaw, the cliffs are under , and in some places not more than . For a short distance east of Pleasant Harbour in East Aberthaw, there are wooded cliffs about 300 yards from the high-water mark of ordinary tides. West of the port of Aberthaw there is an expanse of alluvial ground protected by embankments.
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The Krol group of rocks, comprising slates, marls, sandstones, limestones and dolomites with a few small dykes intrusives, is the dominant geological formation of the lake's surroundings. The lake is deduced to have been formed tectonically. Balia Nala, which is the main stream feeding the lake is along a fault line and the subsequent streams align parallel to major joints and faults. 26 major drains feed the lake including the 3 perennial drains.
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The lake, long and wide, was formed as the result of a landslide, which blocked the valley though which the Tortum River flowed. At the same time, the water sought a new outlet over a fault with a drop of . The hollow left in the Kemerlidağ slope on the left of the valley by the fall of rock is still clearly visible. Tortum Lake is surrounded by limestone marls of the Cretaceous period.
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STAMPA The Bellori outcrop displays about 20 m of limestones with intercalated clays and marls rich in organic matter and sometimés fossil wood (coal) and amber. The limestones are well stratified, with beds 10 cm to more than one metre thick, whereas the clayey levels range between 3 and 40 cm in thickness.Cyclical variation in paleoenvironments of the Rotzo formation (Lower Jurassic, Lessini Mts., N Italy) / Neri, Mirco; Papazzoni, Cesare Andrea; Vescogni, Alessandro; Roghi, Guido.
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These littoral facies rocks can change into iron-rich oolites along their margins. The sequence finishes again with hardgrounds. The third and last sequence of the Lias sets in during the Lower Toarcian without any detrital deposits at its base, the sediments being black ammonite-bearing marls (with Harpoceras falciferum and Hildoceras bifrons). Towards the end of the Toarcian and the beginning of the Aalenian, the sediments turn into sandy limestones indicating another regression.
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The Lower Kimmeridgian sediments are sedimented close to the shore, they bear oysters, urchins, and ripple marks. The second sequence of the Malm starts in the Upper Kimmeridgian, only in places does it show regressive traits, nevertheless the sedimentary character changes. Laid down are breccias and the sediments also show synsedimentary reworkings; periodically interbedded limestones and marls carrying lignite horizons begin to form. The sediments can be dated by the ammonites Aulacostephanus and Aspidoceras orthocera.
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In the Périgord and in the Quercy, the Sidérolithique accumulated—iron-rich sediments that resemble laterites indicating a subtropical climate. During the Upper Eocene (Priabonian), a regression set in. The Subpyrenean Basin became completely filled with the erosional debris of the rising Pyrenees. In the Médoc, nummulite-bearing marls and limestones were still being laid down, but east of Bordeaux already continental molasses appeared that change farther south into gypsum-bearing formations.
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The portion south of the Col de Saint-Michel consists mainly of scree with a Jurassic limestone ridge. The east escarpment, is composed of Valanginian marls and marbles, with scree and Cretaceous limestone at the base.Geological Map of France, from the website of the French government's Geological and Mineral Research Office. South of the Col de Saint-Michel pass, a change in the strike-slip fault deflects the ridge line to run northeast-southwest.
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These sediments deposited as result of a regional marine transgression swept over the Horn of Africa during the initial break-up of Gondwana. Resultant rocks include sandstone, limestone, shale, marls and evaporites (Adigrat Sandstone, Antalo Limestone, Amba Aradam Formation). A third major plantion surface and unformity formed in the following a tectonic event in the Early Cretaceous that tilted carbonates in the Tigray and Dire Dawa-Harar areas. On top of this surface lies a series a fluvial sediments.
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The karst complex of Ojo Guareña, consisting of 110 km of galleries and its caves formed in carbonatic materials of Coniacian which are situated on a level of impermeable marls, is the second largest of the peninsula. This geological configuration has allowed upwellings of mineral-medicinal or thermal water, used now or in the past, in Almeida de Sayago, Boñar, Calabor, Caldas de Luna, Castromonte, Cucho, Gejuelo del Barro, Morales de Campos, Valdelateja and Villarijo, among other places.
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The Unken Member of the Formation Recovers Deep Basinal Deposits, while the Salzburg member is related with Epicontinental to Shallow Nearshore Waters. On the After the Pliensbachian-Toarcian locally is observed a significant decrease in the Crinoid skeleton elements, also that of the Ophiurida; the Echinoids take their place, where really blossomed at that time. Pedicellaria are observed very often. On the Bächental bituminous marls there is a great abundance of saturated Hydrocarbons in the hexanesoluble fraction.
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Methyl and Methylene where found along long-chain paraffinic molecules (n-alkanes). Benzenemethanol resins are especially strong for the Benzene-Methanol fraction. While the occurrence of charred Organic Matter is commonly connected to Wildfire activity, the presence of Alginite as the dominant maceral group in Bächental bituminous marls suggests a mainly marine algal source. The main maceral found is Lamalginite, which may derive from thin-walled planktonic and benthic organisms, including Green Algae, Cyanobacteria, and Bacterial mats.
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Cadney Moss is in Wales, and has been largely reclaimed for agriculture and forestry. Whixall Moss and part of Bettisfield Moss sits above bedrock composed of fine red silt and sand, forming an impermeable layer once known as Upper Keuper Marls. To the north-west of these, the bedrock is composed of Upper Keuper Saliferous Beds, which contain rock salt. Both rock types were re-classified in 2008, and are now part of the Mercia Mudstone Group.
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The only known specimen of Borchgrevinkium has been recovered in Early Devonian (Lochkovian) deposits of the Taymyr Peninsula in Siberia, Russia. It was found alongside specimens of the chasmataspidids Dvulikiaspis menneri, Heteroaspis stoermeri and Skrytyaspis andersoni, as well as indeterminate eurypterids like Acutiramus. The lithology (physical characteristics of the rocks) of the place has been described as dark gray marls with gypsiferous and dolomitic; rich in dolomite occurrences. The fossils were collected below the Early Devonian-Middle Devonian boundary.
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The sediments are mainly epicontinental deposits of lacustrine character, as well as limestones, marls and dolomites with marine or littoral faunas. The basin was under tension during this period and as a result long horsts and graben structures of different subsidence rates were created following more or less the trend of the Variscan fractures. Its northern side is rimmed by the relatively stable Aquitanian shelf. The basin probably is caused by crustal thinning infiltrating from the Atlantic domain.
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It is located within Volhynian-Podolian tectonic block and noted with close to the surface occurrences of rocks of the crystalline basement. Here could be found limestone, marls, sandstones, shales, as well as granites and gneisses that are overlaid with loesses. The area surface is mostly raised gentle rolling hill loess plain. After the physical and geographical categorization of Ukraine, it belongs to West-Podolian region of West Podolian Province of the Podolian Forest-steppe zone.
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The borough is within the Hampshire Basin, with an underlying geology of mainly Cretaceous chalk. Soil in the borough is principally of poor to moderate agricultural quality although high grade land is present in pockets. The south of the borough has acid soils and gravels, but poorly drained clays predominate in the north. Most of the borough is covered by a series of clays and marls, with sandy and lignitic beds, part of the Bracklesham Group of beds.
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There the Cretaceous succession includes Barremian and Aptian–Cenomanian limestones and marly limestones with abundant concretions of black chert. The Upper Jurassic succession begins with thin-bedded Kimmeridgian–Oxfordian cherty limestones, marls, sandstones and clays, which are identified in the lower part of Krubera Cave. Above lies the thick Tithonian succession of thick-bedded limestones with marly and sandy varieties. Sandy limestones are particularly abundant through the upper 1,000 m sections of deep caves of the Ortobalagan Valley.
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The island is composed entirely of mudstones and sandstones of late Silurian/early Devonian age assigned to the 'Milford Haven Group' of the Lower Old Red Sandstone. This suite of rocks was formerly known as the 'Red Marls'. The strata are folded into a syncline with an east–west axis hence the rocks on the north coast dip inland i.e. to the south, at 25° to 40° whilst those on the south coast also dip inland i.e.
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The formation is named from the village of Blue Anchor on the coast of west Somerset. It consists largely of green to grey mudstones and siltstones (which gave rise to the earlier name of this sequence, the Tea-green Marls) and varies from around 5m to 67m in thickness. Though common to all other areas, the Blue Anchor Formation is absent through erosion in the Stafford Basin and in Lancashire. It is of late Norian to early Rhaetian age.
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The area is notable for its abundance of Neolithic rock carvings dating from 7000 to 5000 BC. North of Djelfa town there is an imposing physical feature known as Rocher de Sel (English: Salt Rock) that resulted from the erosion of rock salts and marls by rain. To the west of the town Megalithic funerary structures are found. During the Roman Empire a Roman town called Fallaba was built on the site of Djelfa.Fallaba at www.gcatholic.
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Bombus cerdanyensis was described from Late Miocene lacustrine beds of La Cerdanya, Spain in 2014. Calyptapis florissantensis was described by Theodore Dru Alison Cockerell in 1906 from the Chadronian (Eocene) lacustrine – large shale of Florissant in the US. Oligobombus cuspidatus was described by Alexander V. Antropov in 2014 from the Insect Bed of the Bembridge Marls in the Eocene of the Isle of Wight, England. The fossil was described by re-examining a specimen in the Smith Collection.
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The Togopi formation on the onshore of the peninsula is mainly made of marls and preserves Plio-Pleistocene sedimentary sequences which have a relatively high coral diversity. Based on organic geochemical and petrological analyses, both formations of Sabahat and Ganduman found to be gas-prone source rocks. The narrow continental shelf fronting the coastal areas of both Dent and Semporna Peninsulas also could be exposed to future tsunamis with the active fault in the eastern coast.
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The very steep-sided V-shaped valleys that are typical of the Keuper Uplands are known here as klingen. Such klingen occur in the petrographically harder sandstone beds of the keuper, for example in the Stubensandstein. These rocks are able to resist significantly the erosion forces (especially side erosion) of water. In less erosion-resistant rocks of the keuper like the clays or marls, the valleys are more deeply carved out so that many wider-profiled valley are formed.
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The name has gone through many changes since being recorded as "Rodemesc" in the Domesday Book and "Raumersche" in 1355. The name is thought to be of dual origin, "Rode" being from the Old Norse for "red", and Mesc from "Old English" meaning "Marsh". This led to "Red Marsh", from its situation in the Permian System of red sandstones and marls which run through the area. Localised clays outcrop and the area was formerly known for its potteries.
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Amphibolite need not be derived from metamorphosed mafic rocks. Because metamorphism creates minerals entirely based upon the chemistry of the protolith, certain 'dirty marls' and volcanic sediments may actually metamorphose to an amphibolite assemblage. Deposits containing dolomite and siderite also readily yield amphibolite (tremolite-schist, grunerite-schist, and others) especially where there has been a certain amount of contact metamorphism by adjacent granitic masses. Metamorphosed basalt creates ortho-amphibolite and other chemically appropriate lithologies create para-amphibolite.
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To the south and south-west of the settlement the relief is soft and without significant hills. To the north, north-west and east it is full of hills, some as high as 290 metres. The river Aloupos, to the north of the village, and the Ovgos (Ovkos) to the south have eroded the landscape. The geology is dominated by the calcareous sandstones, sands, sandy marls, Kythrea Flysch and recent revived affairs of Olokainis of geological period.
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Marl is limestone with a high proportion of clay minerals. The eroded material was washed into the sea or deposited in the interior of the island of the Pla de Mallorca, bright marls in the north-east of the island and ferrous clays in the middle of Mallorca, which gives the soil its characteristic reddish colour."Ein Felsen, der aus dem Meer gewachsen ist" [German], interview with geologist Rosa Mateos in Mallorca Magazin 13/2009, pp. 62-63.
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On top of this is seasonally flooded forest deposits indicated by organic rich mudstones containing leaves of Acer cf. viminalis and Platanus s. Tabular bodied transgressive beach deposits are interbedded with fine-grained sediments and lignite, alluding to fresh-water lacustrine like environment. Animal life fossilized in lacustrine marls consist of few Oligocene ostracods and mollusks – indicative of fresh or shallow brackish water – suggesting the basin had very shallow waters even in its most open condition.
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The single known queen of E. biamoensis is the only Emplastus gyne described from Bol’shaya Svetlovodnaya. Overall the species has a body length of The queen is distinct from the other Bol’shaya Svetlovodnaya species due to the forward set smallish eyes, whereas the two other species have large eyes. The species is smaller than the queens from the Bembridge Marls and Radoboj which range between . The petiole is smaller than that of E. britannicus and E. gurnetensis.
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Boquillas Formation - stratigraphy The Boquillas Formation is a geologic formation deposited during the Late Cretaceous in modern-day West Texas. It is typically composed of alternating marls and limestones with thin volcanic ash beds (bentonites). It was named for outcrops near the former Boquillas post office in Big Bend National Park. The term Boquillas Formation has been used for rocks that outcrop from Del Rio, Texas to as far west as Doña Ana County, New Mexico.
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The Rif microcontinent shifted westward and collided with the African Plate in the Oligocene and the Miocene, generated the complex Rift overthrust. Seismic studies have found that Carnian sandstones, mudstones and conglomerates from the Triassic, lie unconformably atop the microcontinent's crystalline basement rock in north Morocco. The Miocene and Pliocene marls and carbonates of the Doukkala sub- basin are overlain by Quaternary rocks. Further west, Quaternary rocks cover Middle Cretaceous sedimentary rocks, which lie unconformably atop Triassic and Paleozoic units.
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The presence of altered Celadonite, suggest volcanogenic solutions as the most probable source, where the high amounts of dissolved manganese of continental origin was translated to the epicontinental margins of the Tethys. On the Bächental bituminous marls had a bulk mineralogy where the Calcite is the most abundant fraction (49%), followed by Phyllosilicates (35%), Quartz (11%) and Pyrite (5%).Gesteine, B., Schichten, B., Schichten, S., Schichten, H., & Gosau, K. (1988) An Organic Geochemical Study of Austrian Bituminous Rocks.Jb. Geol. B.-A.
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The Infrahelvetic complex consists of Mesozoic cover rocks, most notably massive limestones from the European continental shelf. These limestones have a shallower marine facies than contemporary sediments from the Helvetic nappes since they were originally deposited north of those units. The Triassic and Permian consist of dolomites, marls and conglomerates. In contrast to the completely detached Helvetic nappes, the Infrahelvetic complex is still lying conformably on top of a Hercynian basement which forms the external massifs of the Aar and Gotthard nappes.
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The Roxby Formation, previously known as the Permian Upper Marls, is a formation from the Guadalupian-Early Triassic of eastern England (formation dies out at Nottinghamshire). The formation is made up largely of mudstone and siltstone, reddish brown, with subordinate sandstone.BSmith, D B, Harwood, G M, Pattison, J and Pettigrew, T H. 1986: A revised nomenclature for Upper Permian strata in eastern England. 9-17 in Harwood, G M and Smith, D B (editors): The English Zechstein and Related Topics.
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The lower section of the lower member represents a relatively well- oxygenated pelagic environment. The lower member then transitions to a section of darker and more clastic layers indicative of anoxic conditions and reduced reef activity. Most of the articulated crinoids and vertebrate fossils of the Guanling biota hail from a dark grey micrite at the base of the lower member's upper section. This is followed by dark grey marls and black shale rich in bivalves, ammonoids, and slightly radioactive clay minerals.
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The Souar Formation dates to the end of the Eocene and is made up of marine clay, marl, sand and gypsum. The Fortuna Formation in the Cap Bon area records the Oligocene with sandy limestone and marls, overlain by coarse sandstones and quartz pebbles, although it fades out in southern Tunisia. Other Cenozoic units include the Ain Grab Group and Oum Domil Formation. Quaternary stratigraphy, from the last 2.5 million years, includes quartz sands, rich in bivalves, as well as oolitic sands.
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In Belgian lithostratigraphy the Hannut Formation is one of the two formations of the Landen Group. The other formation is the younger Tienen Formation (continental and lagoonal sands and clays from the late Thanetian age), which is normally found on top of the Hannut Formation. In the northern and eastern parts of Flanders the Hannut Formation lies stratigraphically on top of the Heers Formation (middle Paleocene sands and marls). The Hannut Formation correlates with parts of the Landen Formation in the Netherlands.
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The Gorgany range is mostly strongly-layered sedimentary rock (a type called flysch), that fractures into debris fields known locally as 'gorgan'. The full vertical range of the central Carpatians are represented, with altitudes in the park ranging from 710 to 1754 meters above sea level. The range runs from northwest to southeast, on Cretaceous and Quaternary conglomerates, sandstones, clay and marls. There are 30 mountain streams in the park, forming a dense network that feed into the Bystrytsia River.
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The deepening of the rift is recorded by the lower Miocene Rudeis Formation. The lower part, consisting of marls and sandstones, is overlain by coarse sandstones and conglomerates reflecting a rapid increase in rift topography at that time. The Kareem Formation saw the first development of evaporites, indicating basin restriction, followed by open marine shales, as coarse clastic deposition began to reduce in the middle Miocene. Shales, anhydrite, halite and reefal limestones of the uppermost middle Miocene Belayim lie unconformably on the Kareem.
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The site is on the north edge of the Forest of Dean and provides extensive exposures in the Brownstones of the Old Red Sandstone late Lower Devonian period. The sequence of muds, silts, sandstones and conglomerates provides a contrast with the sandstone sequences in the Brownstones (higher) and the Red Marls (lower). The size of the rivers appears to have increased during the Lower Old Red Sandstone period in South Wales. The proportion of channel sands which have been preserved have increased.
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To the north of the N 065-striking fault the basement rocks consist of Plagioclase-bearing paragneisses. In some places these are intruded by small granodiorite bodies belonging to the Piégut-Pluviers Granodiorite or by leptynites of Ordovician age. The flatlying sediments surrounding the village center are mainly of Jurassic age and comprise Lias as well as Dogger limestones. The Lias is composed of Hettangian (sandstones, coarse sandstones and conglomerates), Sinemurian (oolithic limestones, sometimes dolomitic) and Toarcian (claystones and grey marls).
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The Bracklesham Group (formerly Bracklesham Beds), in geology, is a series of clays and marls, with sandy and lignitic beds, in the middle Eocene of the Hampshire Basin and London Basin of England. The type section of the Bracklesham Group is the sea cliffs at Whitecliff Bay on the Isle of Wight, and it is also well developed on the mainland. The Group gets its name from a section at Bracklesham in Sussex. The thickness of the deposit is around 120 m.
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These strata are the Catalan Bay Shale Formation (youngest), Gibraltar Limestone, Little Bay Shale Formation (oldest), and Dockyard Shale Formation (age unknown). These strata are noticeably faulted and deformed. Predominantly of shale, the Catalan Bay Shale Formation also contains thick units composed of either brown calcareous sandstone, soft shaly sandstone interbedded with bluish-black limestone, and interlayered greenish-gray marls and dark gray cherts. The Catalan Bay Shale Formation contains unidentifiable echinoid spines and belemnite fragments and infrequent Early Jurassic (Middle Lias) ammonites.
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Quants Reserve is a nature reserve north west of the village which consists of a grassland clearing in a forestry plantation. It is well known for its butterflies — among the species which occur are Duke of Burgundy, marsh fritillary and wood white. In 1988 an area of 50.6 hectares (126.0 acres) was designated as a Biological Site of Special Scientific Interest. Ringdown is a biological Site of Special Scientific Interest where outcrops of both Cretaceous Upper Greensand and underlying Triassic Keuper Marls occur.
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Vine-planted parcels are rather steep and climb up to 478 m height (near Osenbach). The lower part of the slopes consists of layers of limestones or marls covered by loess where the slope is rather smooth. Finally, the plain consists of a thick layer of alluvium deposited by the Rhine (silt and gravels). This zone is very more fertile than the two previous with an important aquifer mainly close to the surface (less than 5 m deep): the Upper Rhine aquifer.
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In: Walter Freudenberger, Klaus Schwerd (Red.): Erläuterungen zur Geologischen Karte von Bayern 1:500 000\. Bayerisches Geologisches Landesamt, Munich, 1996 (online ), p. 259-265 The western two-thirds of Franconia is dominated by the Triassic with its sandstones, siltstones and claystones (so-called siliciclastics) of the bunter sandstone; the limestones and marls of the Muschelkalk and the mixed, but predominantly siliciclastic, sedimentary rocks of the Keuper. In the Rhön, the Triassic rocks are overlain and intruded by volcanic rock (basalts, basanites, phonolites and trachytes) of the Tertiary.
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This sequence is overlain by bluish-grey marls and black silty shales with conglomeratic intercalactions. Museo Virtual - Geositio Puerto Plata type section - SGN A second outcrop in Puerto Plata shows a less typical debris flow setting, with a varied sedimentological character. Museo Virtual - Geositio Puerto Plata - SGN ;Hermanas Mirabal The section of La Toca Formation in Hermanas Mirabal Province displays a thick series of matrix supported conglomerates. The clasts of these massively bedded conglomerates are characterized by two main lithology types; tuff and limestone.
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At full tide, most of the exposure is inaccessible, not be examined in the cliff-face after a spell of wet weather. The clays and marls, by oxidation and weathering, give rise to red clay-ironstone nodules; and various stages in the consolidation of these may be observed. LXIV. Note on some abnormally large spores formerly attributed to Isoetes At several Tertiary/Quaternary several large spores began to appear. The origin of these spores was unknown as they were a lot larger than any know Isoetes.
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Dolichoderus pinguis is known from a single ant found in Russia. The specimen was described from a compression fossil preserved in diatomite deposits of the Bol’shaya Svetlovodnaya site. Located in the Pozharsky District, on the Pacific Coast of Russia, the fossil bearing rocks preserve possibly Priabonian plants and animals which lived in a small lake near a volcano. The site has been attributed to either the Maksimovka or Salibez Formations and compared to the Bembridge Marls and Florissant Formation, both of which are Priabonian in age.
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He first appears having won a swimming trophy, a fact that Rory is very excited about. He has a love/hate relationship with Marla. After Marla's ex Jay Kelso returned on her 18th Birthday, Elliott has told Marla how he feels and has told her that he will give her some space to think about who she wants to be with, soon competing with Jay for Marla's affection. Elliott gives Marls his car to practise driving as he says he's going to go away for a bit.
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Mixosaurus panxianensis was discovered in the Middle Triassic of the Guizhou Province, China. The specimens have been found in the Guanling Formation, which consists of thinly bedded bituminous limestones and marls. The specimens found have important Mixosaurid characteristics such as a long sagittal crest along the top of the skull but is seen as a different species because there is no external contact between the jugal and the quadratojugal. Articulated skeletons have been found and the centra of the vertebrae are higher than they are long.
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The Landen Group is stratigraphically on top of the Bertaimont Formation or Heers Formation (marine marls, sands and clays of Selandian to Thanetian age). In the Belgian lithostratigraphy, the Landen Group is overlain by the Ieper Group, marine clays and sands of Ypresian age. The Landen Group shares its name with the Landen Formation in the lithostratigraphy of the Netherlands. However, this Dutch formation contains not only the equivalents of the Belgian Landen Group but also strata that correlate with the Belgian Opglabbeek Formation and Heers Formation.
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Vertical deepening of the valleys is relatively high, determined by geological structure (layers consisting of sandstones, clays, marls, conglomerates etc.). Vertical deepening is accompanied by an active torrential erosion, mitigated or stabilized by the level of afforestation. The commune is crossed by three major subunits of relief: Șimișna-Gârbou Hills, Prisnel Peak and Almaș-Agrij Depression, all running across the Someș Corridor. This leads to a very pronounced transition for relief and other geographic components, giving a note of specificity to geographical area of the commune.
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Ringdown () is a 4.0 hectare (9.9 acre) biological Site of Special Scientific Interest west of Burnworthy in the Blackdown Hills of Somerset, notified in 1990. The site is located on a valley side in the Blackdown Hills where outcrops of both Cretaceous Upper Greensand and underlying Triassic Keuper Marls occur. Amongst the vegetation present are two species which are very restricted in South West Britain, white beaksedge (Rhynchospora alba) and dioecious sedge (Carex dioica). This site is the only known location for the latter in Somerset.
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Near its source it flows through a landscape of high altitude moorlands, through deep valleys of Miocene era limestone, characterised by clays, marls and dolomitic limestone. It has one reservoir, La Tajera, with an extension of 409 ha near Cifuentes. It crosses the villages of Luzón, Anguita, Luzaga, Cortes de Tajuña, Brihuega and Renera in Guadalajara province and enters Madrid province at Ambite; it then passes close to Orusco, Carabaña, Tielmes, Perales de Tajuña and Morata de Tajuña, before joining the Jarama near Titulcia.
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Thin pelagic layers separated individual turbidites. As determined by microfossils, each individual layer often represents several tens of thousands of years of pelagic sedimentation in a deep sea, abyssal environment. Depending on the carbonate compensation depth at the time of deposition, these layers consist either of calcareous ooze, marls, or clay. During the last 2.6 million years within the region of the Madeira Abyssal Plain, carbonate compensation depth has been closely controlled by the general circulation of ocean currents and has oscillated in phase with climatic shifts.
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The nature reserve of Ghirardi is located in the southwestern part of the Province of Parma (Emilia-Romagna Italy, between the towns of Albareto and of Borgo Val di Taro. The area dates back to the Jurassic period. During sedimentation there were frequent tectonic upheavals, for which the area is characterized by folds and faults (among which, the most noticeable is situated along the river Rizzone). The formations that we can find in the oasis are: - Palombini clays; - Ranzano sandstones; -marls of the mount Piano.
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F. paleosibirica is known from a group of ants found in Russia. The specimens were described from compression fossils preserved in diatomite deposits of the Bol’shaya Svetlovodnaya site. Located in the Pozharsky District, on the Pacific Coast of Russia, the fossil-bearing rocks preserve possibly Priabonian plants and animals which lived in a small lake near a volcano. The site has been attributed to either the Maksimovka or Salibez Formations and compared to the Bembridge Marls and Florissant Formation, both of which are Priabonian in age.
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On the shallow shelf-domain east of the reefs, neritic limestones were deposited in the north and dolomites in the south; in the Quercy, even supratidal lignite- bearing limestones were formed. In the western domain open towards the Atlantic, the pelagic sediments comprise ammonite-bearing limy marls very rich in filamentous microfossils (bryozoans). The first sequence in the Dogger (note: sequences are only distinguished in the eastern shelf-domain) starts transgressing in a restricted environment during the Bajocian with dolomite. In places, Aalenian is reworked.
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G. macrops is known from a single ant found in Russia. The specimen was described from a compression fossil preserved in diatomite deposits of the Bol’shaya Svetlovodnaya site. Located in the Pozharsky District, on the Pacific Coast of Russia, the fossil-bearing rocks preserve possibly Priabonian plants and animals which lived in a small lake near a volcano. The site has been attributed to either the Maksimovka or Salibez Formations and compared to the Bembridge Marls and Florissant Formation, both of which are Priabonian in age.
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G. magnus is known from a single ant found in Russia. The specimen was described from a compression fossil preserved in diatomite deposits of the Bol’shaya Svetlovodnaya site. Located in the Pozharsky District, on the Pacific Coast of Russia, the fossil-bearing rocks preserve possibly Priabonian plants and animals which lived in a small lake near a volcano. The site has been attributed to either the Maksimovka or Salibez Formations and compared to the Bembridge Marls and Florissant Formation, both of which are Priabonian in age.
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Formica biamoensis is known from a single ant found in Russia. The specimen was described from a compression fossil preserved in diatomite deposits of the Bol’shaya Svetlovodnaya site. Located in the Pozharsky District, on the Pacific Coast of Russia, the fossil-bearing rocks preserve possibly Priabonian plants and animals which lived in a small lake near a volcano. The site has been attributed to either the Maksimovka or Salibez Formations and compared to the Bembridge Marls and Florissant Formation, both of which are Priabonian in age.
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The rocks of the Austin Chalk consist of recrystallized, fossiliferous, interbedded chalks and marls. Exposures of Austin Chalk are mainly seen in quarries, roadcuts, and stream beds where water eroded the soil. Austin Chalk outcrops can be seen throughout Dallas, and extend south underneath I-35 down into Austin and San Antonio. Volcanic ash layers are present in the Austin chalk, and dates obtained from radioactive minerals in these ash layers indicate they were deposited by wind from distant erupting volcanoes around 86 mya.
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This site is designated due to its biological qualities. SSSIs in Wales have been notified for a total of 142 different animal species and 191 different plant species. This predominantly sessile oakwood on red marls of the Old Red Sandstone and Silurian mudstones, is a remnant of a once older and larger woodland at Minwear described in Elizabethan times as a “great wood or forest”. Scarce plants include: the hay-scented buckler-fern (Dryopteris aemula) and wood spurge (Euphorbia amygdaloides), the wild service tree (Sorbus torminalis), crab apple (Malus sylvestris) and aspen (Populus tremula).
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August Stein und Julius Schäfer from Düsseldorf founded the coalmine "Auguste Victoria" in 1898 based in Düsseldorf and coal production was planned on the claims "Hansi 1" and "Hansi 2". On 1 May 1900 the depths began and in 1903 the head office moved to Marls urban district Hüls. At the end of 1905 coal production began on the pit "AV 1". Eponym for the mine was Augusta Victoria of Schleswig-Holstein, (1858–1921) the last German empress and wife of Emperor Wilhelm II. The coalmine was one of the highly productive mines in Germany.
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This trend has been observed by looking at the chemistry of both biogenic and abiogenic carbonates, dating them, and analyzing the conditions under which they were formed. Various studies have examined these relationships and concluded that the mineralogy of both biogenic (major carbonate sediment and rock-forming organisms) and abiogenic marine carbonates (limestones and marls) throughout Phanerozoic time has generally been synchronized with calcium carbonate mineralogies expected from seawater magnesium/calcium ratios reconstructed from derivatives of ancient seawater trapped in halite crystals in the geologic record (fluid inclusions).
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Later in the Paleogene, another phase of orogeny affected the Pieniny Klippen Belt. It squeezed the former nappe stack and the rocks of different rheology (competent limestones, soft flysch, and marls) were deformed in different ways, which caused the rupture of more dense rock and ductile deformation of the less dense rock. Complicated arrangement of particular tectonic units was later affected by strike-slip motion in the area of the Peri-Pieniny Lineament in the Miocene. Consequent erosion dissected the rigid limestone tectonic lenses to the shape of protruding klippes (e.g.
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Global anoxia during the latest Pliensbachian and the earliest Toarcian occurred in close association with regional drowning of the lower Liassic platforms and localized deposition of basinal marls. From Toarcian times, carbonate platforms of the Azilal Formation developed in the margins of the central High Atlas basin, whereas the basin axis was occupied by a mixed carbonate-siliciclastic platform system prograding eastward to basinal deposits. This mixed system progressively graded to an extensive shallow water carbonate platform of the Anoual Formation, Bajocian to early Bathonian in age that is recognized throughout the central High Atlas.
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About 220 m million years ago (during the Carnian) evaporites settled out in lagoons and grabens—variegated, gypsum–bearing, iron-rich clays, gypsum, anhydrite, dolomitic marls, dolomites, rock salt as well as potassium and magnesium salts occur. The evaporites served later as major decollement horizons. At the limit, Upper Triassic/Hettangian doleritic tholeiites (ophites) formed in the Pyrenees and in the southern Aquitaine Basin, indicating further movements along the fracture zones (submarine fissure eruptions and sills in unsolidified Keuper sediments). The sedimentation during the Jurassic is characterised by the growth of a carbonate platform.
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The lower member concludes with a sequence of dark grey laminated marls incorporating conodont fossils and silty quartz grains. The middle member of the Xiaowa Formation is by far the thickest unit and includes thick-bedded grey limestone and marl layers interbedding with each other. Sediment deformation is characteristic of layers in this member, while fossils are represented mainly by occasional bivalves and ammonoids. The middle member represents a deep-water environment influenced by tectonic events which disturb sediment layers and create distant turbidites that periodically supply increased clastic material.
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The Bembridge Beds The beds which yielded the rich flora to be described occur on the north- west coast of the Isle of Wight, in Gurnard Bay and Thorness Bay, about two miles to the south-west of Cowes. With few exceptions, all the plants were obtained from these localities. The exposure shows a variable series of clays and marls rich in selenite. These can be seen in the cliff when the section is not obscured by vegetation and landslides, and on the foreshore when the tide is low.
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The limestones feature micrites, sparites, oolites and also limestones rich in siliciclastics that were deposited near the shoreface. The marls were formed near the continent and are occasionally rather rich in lignite, once mined near Allas-les-Mines. The Jurassic rocks crop out along the northern edge of the Périgord noir near Terrasson- Lavilledieu, where they are separated from the Upper Cretaceous by the southeast-striking Cassagne Fault. They are also found within the Saint- Cyprien Anticline — a southeast-striking tectonic upwarp near Le Bugue and Saint-Cyprien.
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Graded sandstone to mudstone overbank deposits (complete with ripple marks) occur near channel deposits. Extensive successions of laminated or massive mudstone are common, often containing slickensides, calcareous nodules or layers (marls), and/or hematite nodules. These types of thick mud/marl layers likely formed in more quiet parts of the floodplain isolated from turbulent channels. The floodplain was seemingly more active during the deposition of the Lower Ntaware Formation, as coarser sandstone channel fills are prevalent in that section while extensive mudstone layers are more common in the Upper Ntaware Formation.
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Mounted skeleton and fossils, Dinosaur Isle The first bones of Neovenator were discovered in the summer of 1978, when a storm made part of the Grange Chine collapse. Rocks containing fossils fell to the beach of Brighstone Bay on the southwestern coast of the Isle of Wight. The rocks consisted of a plant debris bed within the variegated clays and marls of the Wessex Formation dating from the Barremian stage of the Early Cretaceous, about 125 million years ago. They were first collected by the Henwood family and shortly afterwards by geology student David Richards.
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In the course of the Deep Sea Drilling Project and the Ocean Drilling Program, two research drillings were done so far, the DSDP 368 and the ODP 659. At the DSDP 368 location which was drilled 985 meters deep, it is divided into three units, the first unit composes of marls and oozes, the second composes of turbidites and the third composes of black shales, they lie above pelagic limestones and the oceanic crust. In that area are five basaltic sills. DSDP 368 is east of the island of Boa Vista.
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This unit splits the flagstone sequence into two parts known regionally as the Lower and Upper Orcadian Flagstone formations. In mid- Givetian times, the dominant lake environment gave way to mainly fluvial conditions, with the main sediment type changing from flagstones to sandstones. In parts of the basin, the sequence consists almost entirely of sandstones, mainly fluvial in origin, such as the Dunnet Head and Hoy Sandstones. Elsewhere, such as in Orkney in the Eday Group, the sequence shows more variety with major intercalations of marls and flagstones, marking the local return of lacustrine conditions.
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It then runs along Kedleston Road which it leaves and goes behind Woodlands Community School and Laburnum Crescent and finishes at Allestree Park. The geology of the area consists of thick sandstones and marls formed in desert conditions in the Triassic period, some 250 million years ago, and thin-bedded sandstones and shales formed 300 million years ago in the Carboniferous period. Most of Britain at this time was a huge delta carrying vast amounts of sediment. These belong to the Millstone Grit formation which makes up much of the Peak District.
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Blackdown and Sampford Commons have extensive surviving examples of the heathland, carr woodland and marshy grassland habitats that have developed on the acidic soils overlying the Greensand and Keuper Marls of the Blackdown Hills. The heathland supports a typical invertebrate fauna, including a wide variety of butterfly species, and with spiders notably abundant. The site is regionally important for birds which favour heathland habitats. Quants, a grassland clearing in a forestry plantation well known for its butterflies including Duke of Burgundy, marsh fritillary and wood white, is a candidate for Special Area of Conservation (cSAC).
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The geology of the House Range is dominated by gray Cambrian to Devonian carbonate rock which was intruded by a pink Jurassic granitoid in the central part of the range. In the Wheeler Amphitheater, away from the intrusion, the Lagerstätte that contains the well- preserved fauna is found in the Cambrian section of the range. Evidence of Lake Bonneville's presence is found both in shorelines and white marls at the base of the range. The main structural component to the range is a large basin-bounding fault on the west side.
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These alluvial environments were gradational towards the east, with the shallow marine carbonates of the Guarujá Formation, and further to the open basin with the siltstones of the Itanhaém Formation. Biostratigraphical data and its relations with the Guarujá Formation point towards an Albian age. The depositional environment of the Guarujá Formation has been interpreted as a tidal flat, like this present-day example in Oregon, United States. ;Guarujá Formation The Guarujá Formation is thick and consists of oolitic calcarenites, which laterally grade to greyish ochre and brownish grey calcilutites and grey marls.
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The continental sandstones and siltstones of the Abu Zenima Formation represent the earliest syn-rift deposits of late Oligocene (Chattian) to early Miocene (Aquitanian) age. Locally the Abu Zenima Formation is capped by basalts. The lower Miocene age conglomerates, sandstones and marls of the Nukhul Formation were deposited in shallow marine conditions as the sea began to flood the developing rift. The Nukhul Formation overlies the Abu Zenima Formation in some place but elsewhere is probably age equivalent, reflecting a diachronous change to marine conditions within the rift.
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New Delhi: Indian National Scientific Documentation Centre, 1974. Pages 9–28. Zhdanko Mountain Ridge Crystalline rocks crop out at several capes; Cretaceous limestones, containing an abundant and specific fauna of gigantic ammonites, occur at Dui on the west coast; and Tertiary conglomerates, sandstones, marls, and clays, folded by subsequent upheavals, are found in many parts of the island. The clays, which contain layers of good coal and abundant fossilized vegetation, show that during the Miocene period, Sakhalin formed part of a continent which comprised north Asia, Alaska, and Japan, and enjoyed a comparatively warm climate.
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Teixell, A., Arboleya, M. L., Julivert, M., & Charroud, M. (2003). Tectonic shortening and topography in the central High Atlas (Morocco). Tectonics, 22(5), n/a Across the Toarcian-Bajocian strata, there was a great deposition of marine shales as Marls, Calciturbidites and Reefal Limestones, that where accumulated in the Central High Atlas, while on the west margin around the Massif Ancien terrestrial, specially fluvial sedimentation dominated. The present Red Beds of Azilal indicate various marine transgressions across the Toarcian-Aalenian boundary, after ending its sedimentation on the Bathonian.
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The Austin formation consists of recrystallized, fossiliferous, interbedded chalks and marls. Exposures of Austin chalk are mainly seen in quarries, roadcuts, and stream beds where the water eroded the top soil. Austin chalk is the well known white rock that the city of Dallas sits on. Volcanic ashes are present in the Austin chalk, and were deposited by wind from distant erupting volcanoes and erupting igneous intrusions around 86 Ma. These eruptions occurred along a 250 mile long by 50 mile wide belt of submarine volcanoes, which are located in present-day south-central Texas.
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On top of the Ozan marl is two thin beds known as the Wolfe City Sandstone and Pecan Gap Chalk. The Wolfe City Sandstone is known in the city of Rockwall, Texas for its sandstone dikes that protrude into the surface, and gives a surface expression of a wall built of rocks. The very top of the Taylor has a 300-foot section of marls known as the Marlbrook Marl. The last beds of the Cretaceous, which are also deposited directly over the Taylor formation and found east of Dallas are the Navarro beds.
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Two important towns are located in the immediate area of the range, Bou-Saada to the north at the feet of the mountains and Djelfa in the middle of the range at an elevation of 1,208 m. North of Djelfa town there is an imposing physical feature known as Rocher de Sel (English: Salt Rock) that was formed from the erosion of rock salts and marls by rain. To the west of the town Megalithic funerary structures are found. Neolithic art is widespread in different caves and walls throughout the range.
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The facies dividing reef-zone persists into the Malm. In the western domain, initially ammonite-bearing marls and limestones were deposited, whereas in the eastern domain the sediments are calcareous dolomites. The retreat of the Jurassic sea became noticeable during the late Tithonian with dolomites and breccias in the Adour Basin, evaporites in the Charente, extremely littoral sediments in the Quercy, lacustrine limestones in the Parentis Basin, and anhydrites in the Gers. The seaways that had opened in the Lias closed again and a single reef persisted in the Périgord at La Tour-Blanche.
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They have a small head, with similar mandibles to the females, and likewise similar short antenna scapes. Unlike the females, the legs of the males are long and fairly thin. The species names britannicus and ovigerus were not given etymologies by Cockerell, while the name emeryi was coined by Donisthorpe as a patronym honoring the Italian entomologist Carlo Emery, who gave input Donisthorpe on the Isle of Wight fossils, and for his work on Sicilian amber ants. Overall individuals of E. britannicus are the most numerous ant fossils in the Bembridge Marls.
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Gurney Slade quarry Gurney Slade quarry, is a limestone quarry near Gurney Slade between Binegar and Holcombe, on the Mendip Hills, Somerset, England. Gurney Slade quarry exhibits pale to very dark grey Carboniferous Limestone overlain by red and purple-coloured Triassic breccias and marls with a small faulted block of overlying Lower Jurassic breccias forming an angular unconformity with the Carboniferous Limestone. There is abundant vertical sediment infilled fissures and joints (Neptunian Dykes). The rocks contain varying amounts of calcite mineralization, and there is common fossil material associated with the Carboniferous and Jurassic limestones.
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The site has been attributed to either the Maksimovka or Salibez Formations and compared to the Bembridge Marls and Florissant Formation, both of which are Priabonian in age. At the time of description, the holotype male specimen, number PIN 3429/1112 was preserved in the A. A. Borissiak Paleontological Institute collections, part of the Russian Academy of Sciences. The fossil was first described by the trio of paleomyrmecologists Gennady Dlussky, Alexandr Rasnitsyn and Ksenia Perfilieva. In the type description, Dlussky, Rasnitsyn and Perfilieva named the species P. oligocenica, with the specific epithet derived "Oligocene" the possible age of the site.
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Most of the land is made almost entirely of boulder clay with the exception of the slim bands of limestone, marls and sands along the valley of the Willow Brook. The village lies on the South East side of the Willow Brook river and to the North West of Deenethorpe is the local church called St Peter's Church located in Deene. Deenethorpe Lane runs through the entire village with the exit to the North onto the A43. The other main road is Benefield Road cutting across the village from East to West which also exits onto the A43.
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In southern Europe, the Cretaceous is usually a marine system consisting of competent limestone beds or incompetent marls. Because the Alpine mountain chains did not yet exist in the Cretaceous, these deposits formed on the southern edge of the European continental shelf, at the margin of the Tethys Ocean. Stagnation of deep sea currents in middle Cretaceous times caused anoxic conditions in the sea water leaving the deposited organic matter undecomposed. Half of the world's petroleum reserves were laid down at this time in the anoxic conditions of what would become the Persian Gulf and the Gulf of Mexico.
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Water and gravel erosion on the slope of an escarpment Klingen occur especially in the small catchment areas of heavily forested low mountain regions, carved out by erosion processes even today, where, as a result of the alternating layers of porous sandstones or limestones on top of impervious clays and marls, small springs arise. Hillsides are often undercut which may trigger small or medium- sized landslips or even mudflows. In southwestern Germany these processes occur especially in the small, steep-sided valley that flow into the Rhine system. In harder, jointed (and therefore pervious) rocks, landslips are rarer.
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Rusk Holm, Faray and Holm of Faray lie beyond the Sound of Faray to the north west and beyond them is the larger island of Westray. In common with its neighbouring isles, Eday is largely formed from Middle Devonian Old Red Sandstone deposited in the Orcadian Basin. The Eday Group is the name for a substantial sequence of sandstones that is found at many locations in Orkney, for which Eday and the area around Eday Sound are the type area. In places it is up to thick, and is largely composed of yellow and red sandstones with intervening grey flagstones and marls.
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Argaka () is a village in the Paphos District of Cyprus, located 7 km northeast of Polis Chrysochous. From a geological perspective, it is located upon the calcareous sandstones, the sands, and the marls of the Pleistocene period as well as the lavas and the magma rocks (northeast of the settlement). From a morphological aspect, what stand out are the coastal, alluvial plain, one or two marine terraces, and a slope that steadily ascends up to 500 metres. Several streams flow down from the slope toward the sea, indeed with a relatively large one flowing next to the village.
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The site has been attributed to either the Maksimovka or Salibez Formations and compared to the Bembridge Marls and Florissant Formation, both of which are Priabonian in age. At the time of description, the holotype male specimen, number PIN 3429/103 was preserved in the A. A. Borissiak Paleontological Institute collections, part of the Russian Academy of Sciences. The fossil was first described by the trio of paleomyrmecologists Gennady Dlussky, Alexandr Rasnitsyn and Ksenia Perfilieva. In the type description, Dlussky, Rasnitsyn and Perfilieva named the species P. petrosum, with the specific epithet derived the Latinized Greek petros meaning "stone".
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From a geological point of view, the Lappwald, which reaches a height of 211 m on the Heidberg, is a hollow, that only appears like a raised horst due to the sharply downfaulted terrain it is surrounded by. In the Cretaceous, a period of some 71 million years, the sea washed chalk, marls and sands in several flood phases into the Helmstedt and Schöppenstedt hollow and thus covered the underlying rock. Further flooding by the sea in the succeeding Tertiary era created large areas of bog in the Helmstedt Basin that were transformed under sub-tropical climatic conditions into massive brown coal deposits.
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The site has been attributed to either the Maksimovka or Salibez Formations and compared to the Bembridge Marls and Florissant Formation, both of which are Priabonian in age. At the time of description, the holotype specimen, number PIN 3429/1157 was preserved in the A. A. Borissiak Paleontological Institute collections, part of the Russian Academy of Sciences. The fossil was first described by the trio of paleomyrmecologists Gennady Dlussky, Alexandr Rasnitsyn and Ksenia Perfilieva. In the type description, Dlussky, Rasnitsyn and Perfilieva named the species L. incognitum, with the specific epithet derived from the Latin "incognitum", which means unknown.
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The fossiliferous beds of the Roca Formation were discovered by G. Rohde Windhausen (1914), who was also the first author to describe these sediments. Schiller (1922) took samples of one section along the Zanjón Roca, from the northern part of General Roca to Horno de Cal (lime kiln). This author proposed to name the lime kiln as the "classic area", and the westward cliffs from the lime kiln as the "model area" of these beds. The lithological composition of this type locality contains gray- yellowish and highly fossiliferous limestones, with greenish claystones and marls, and abundant gypsum at the top.
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He had argued that the igneous rocks were younger than the Silurian sediments which then formed and made their way up. However, Anne discovered an outcrop of conglomerate containing fragments of igneous hills near the Dingle Quarry in Malvern, proving Murchison's theory as incorrect. Malvern hills contain many rocks that have Precambrian (Malvernian) igneous obtrusions that are put together by “ Sienitic” rocks. A cross-section of the Malvern Hills can be observed to contain Triassic, and Cambrian sandstones as well as marls located on the eastern side, and Cambrian and Silurian sediments located on the west side.
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Resurrection of Christ, typical Nottingham alabaster panel from an altarpiece set, 1450–1490, with remains of the paint Gypsum alabaster is a common mineral, which occurs in England in the Keuper marls of the Midlands, especially at Chellaston in Derbyshire, at Fauld in Staffordshire, and near Newark in Nottinghamshire. Deposits at all of these localities have been worked extensively. In the 14th and 15th centuries its carving into small statues and sets of relief panels for altarpieces was a valuable local industry in Nottingham, as well as a major English export. These were usually painted, or partly painted.
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The Ketleri Formation is only in southwestern Latvia and northwestern Lithuania. Per Erik Ahlberg, Ervīns Lukševičs, and Oleg Lebedev collected Ventastega material both from the Ketleri locality where the original material was found, but also from another locality in the Ketleri formation, the Pavāri locality. The Ketleri locality is at the Venta river near the former Ketleri hamlet, while the Pavāri locality is across the Ciecere river from the former Pavāri hamlet. The formation itself is composed of sand, sandstone, clay, and dolomitic marls, with the formation being 45m thick in Lithuania and 41-56m thick in Latvia.
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The Grey Chalk Subgroup (formerly the Lower Chalk minus the Plenus Marls) is usually relatively soft and greyish in colour. It is also the most fossiliferous (especially for ammonite fossils). The strata of this subgroup usually begin with the 'Glauconitic Marl Member' (formerly known as the Glauconitic or Chloritic Marl), named after the grains of the green minerals glauconite and chlorite which it contains. The remainder of the subgroup is argillaceous in its lower part (the West Melbury Marly Chalk Formation (formerly the 'Chalk Marl') and becomes progressively purer in the 'Zig-zag Chalk Formation' (the former 'Grey Chalk').
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During the Lower Oligocene (Rupelian), a permanently marine environment persists in the south with marls and sands rich in nummulites, lamellibranchs, and echinids. The anomiid-bearing limestones of the southern Médoc are lagoonal deposits. After a short-lived advance at the beginning of the Chattian with seastar-bearing limestones in the northern Médoc and in the Libournais and with mammal-bearing molasses in the Agenais, the sea made a big retreat at the end of the Oligocene. This retreat was accompanied by tectonic movements creating trains of deeper-seated anticlines in the central and northern Aquitaine Basin.
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At (53.42056, 2.38778), above sea level, Carrington Moss lies along the southern edge of the Lancashire Plain, an area of Bunter sandstones overlaid with marls laid down during the Late Triassic period. These rocks are themselves overlaid by a layer of boulder clay deposited during the last ice age, about 10,000 years ago. The combination of the flat topography and the underlying clay resulted in extensive peat bogs developing along the Mersey Valley, and overflowing beyond the valley. Along with large parts of Chat Moss and Holcroft Moss, Carrington Moss began to form during the Flandrian period from 7100 to 5000 BP.
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The Collón Curá Formation () is a Middle Miocene fossiliferous geological formation of the southern Neuquén Basin in northwestern Patagonia and the western Cañadón Asfalto Basin of central Patagonia, Argentina. The formation crops out from the southern Neuquén Province, the western Río Negro Province to the northern Chubut Province. The formation, with a maximum thickness of , comprises tuffs and sandstones with minor siltstones, marls and limestones, deposited in a fluvial, deltaic and shallow to deep lacustrine environment in small basins separated by faults. The formation dates from the Langhian to earliest Tortonian epochs of the Middle to Late Miocene, typically Colloncuran.
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The formation comprises several lithologies, from sandstone, conglomerates and shales to marls, siltstones, limestones and lignite and gypsum beds and ranges between in thickness. The Tremp Formation was deposited in a continental to marginally marine fluvial-lacustrine environment characterized by estuarine to deltaic settings. The Tremp Basin evolved into a sedimentary depression with the break-up of Pangea and the spreading of the North American and Eurasian Plates in the Early Jurassic. Rifting between Africa and Europe in the Early Cretaceous created the isolated Iberian microplate, where the Tremp Basin was located in the northeastern corner in a back-arc basin tectonic regime.
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It correlates magnetostratigraphically with the upper part of chron C 13r and biostratigraphically with the calcareous nannoplanktonzone NP21. The member therefore belongs to the upper Priabonian and has an absolute age of 34.0 to 33.75 million years BP. The Bembridge Marls Member was mainly sedimented in fresh or brackish water as indicated by cirripedia and gastropods like Terebia. The lower section of the member is of estuarine origin, whereas the upper section was laid down by rivers inhabited by prosobranchs like Viviparus. Relatively short-lived marine inraids are recognizable in horizons like the Bembridge Oyster Bed 1.5 metres above the base and a limestone band with bivalves like Corbicula and Nucula.
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The archaeological excavations at Wadi al-Hasa have contributed to a rethinking in archaeology of use of the use of tools made from bone or bone- like material. Some of the evidence at the site of Ain el-Buhira, a site located at the eastern end of the wadi. The site is characterized by a lake, and sediments and stone formations like marls and tufa formations that give insight into the drainage system that was built at the wadi in the Upper Pleistocene period, between 24000 and 19000 BP. Coinman suggests (in 1996) that both bone and blade technologies were more common in this period than previously thought.
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Despite its distinctive nature, the Kupferschiefer is not ranked as a formation but is officially declared a sub-unit of the Werra Formation, the lowest formation of the Zechstein Group, overlying the Rotliegend Group. The unit has been dated to 257.3 ± 1.6 Ma, placing it in the Wuchiapingian stage of the Late Permian. The Kupferschiefer comprises black shales, bituminous marls, mudstones and limestones deposited mostly in an open marine setting, with the borders of its extension deposited in a shallow marine environment. At time of deposition, the area what is now northern Europe was covered by an enclosed sea; the Zechstein sea, characterized by anoxic conditions.
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Coastal rock barrens are found on flat rocky surfaces either immediately adjacent to the coast or within the interior of islands in the Florida Keys. Sinkholes are cylindrical or conical depressions with steep limestone walls, found in karst rockland areas. Soils, when they exist, consist of calcareous marls and organic debris on the surface, within solution depressions, and in crevices in limestone. Elevations on the Miami Rock Ridge vary from greater than above sea level in the vicinity of Biscayne Bay to less than above sea level in the Long Pine Key area of Everglades National Park, with an average elevation of approximately , and varying in width from .
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The range is part of the Styrian-Lower Austrian Limestone Alps and is separated from its neighbouring groups by the Mürz valley (part of the tectonically active Mur-Mürz Furrow), the upper reaches of the Mürz (main settlement: Mürzsteg) and the road over the Styrian Seeberg Pass. It is described by geologists as a ridge-and-basin facies. The majority of its rocks date to the Triassic period and include Wetterstein Dolomite, Hallstatt Limestone and Mürztal strata (dark, hornstein- dominated limestones and marls with foraminifers, brachiopods and other fossils). The south of the range belong to the greywacke zone (rocks from the New Palaeozoic and the Lower Triassic).
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Thrust of the Carpathians on their foreland caused a flexure of the lower continental plate under the frontal part of the nappes. This flexured area, called the Carpathian Foredeep, was filled by thick formations of molasse, prevailingly marls, sandstones and conglomerates that were formed in the Oligocene to Miocene periods by erosion of the growing Carpathians. Nevertheless, the foredeep is not generally folded; flysch nappes thrusted from the south partially folded the rock underneath. The whole zone of the foredeep is developed in the foreland of the Alps, and runs through the Moravia to the Ostrava Basin and further East to Poland, Ukraine, and Romania.
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The Hassi Messaoud oil field is a Cambrian sandstone reservoir 270 m thick in a dome 3300 m deep and 1300 km2 in area of the Oued Mya structural basin.Balducchi, A., and Pommier, G., 1970, Cambrian Oil Field of Hassi Messaoud, Algeria, AAPG Memoir 14: Geology of Giant Petroleum Fields, Tulsa: AAPG, pp. 477-478. The top of the dome is marked by an unconformity at the base of the Triassic, Mesozoic sediments consisting of salt, anhydrite, shale, limestone, dolomite and marls, all overlain by Mio-Pliocene sandstone.Balducchi, A., and Pommier, G., 1970, Cambrian Oil Field of Hassi Messaoud, Algeria, AAPG Memoir 14: Geology of Giant Petroleum Fields, Tulsa: AAPG, pp.
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Most of the depositional margins of the German realm were on Pelagic marine settings, where the oxygen was the object of different changes along the layers, due to climate conditions and sea current effects. Outside the Shales, there are other types of lithology present, such as the light grey marls of the Aschgraue and Blaugraue Mergel that occur at the base of the Posidonia Shale section, which are related to sea bottom environment with a large period of well and suitable oxygen conditions, reflected on the presence of organic matter. The Black Shales are the opposite, with anoxic bottom effect and a detailed negative effect on the biota.
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Black Down and Sampford CommonsBlack Down Common is so spelt by the Ordnance Survey, but the SSSI citation spells it Blackdown Common. () is a biological Site of Special Scientific Interest in Devon and Somerset, notified in 1952. Blackthorn The Little Breach reserve, which forms part of the SSSI is an area of heathy grassland on Greensand, with some blackthorn and birch, noted for its butterflies and moths. Blackdown and Sampford Commons have the finest and most extensive surviving examples of the heathland, carr woodland and marshy grassland habitats that have developed on the acidic soils overlying the Greensand and Keuper Marls of the Blackdown Hills.
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A small area of rocks originating in the Permian Period occurs near Lancaster, Morecambe and Glasson Dock though it is entirely obscured by recent deposits and is known only from borehole cores. These are the Collyhurst Sandstone of the Appleby Group and the sandstones, mudstones and evaporites of the overlying Cumbrian Coast Group. There are also narrow bands of these rocks (Manchester Marls and Collyhurst Sandstone) to the north and south of Preston though again they are generally buried beneath glacial till. Another small outlier of early/lower Permian rocks is centred on the village of Ireby and extends across the county boundary into North Yorkshire.
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The lake left behind a layer of lacustrine sediment that blankets the Jordan Valley with terraces of sediment up to 40 m thick. These sediments are commonly called marls and are composed of layers of true loam and calcareous silt loams mixed with other chemicals and salts. At its height, the lake covered several other basins in the area with a maximum area of ca. 2000 km2, a length of 200 km and a width of no more than 17 km. The formations were named the Lisan deposits and first described by Lartet in 1869 after visiting the Dead Sea in the Spring of 1864.
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The majority of the of the heath is managed with joint financial input from Clinton Devon Estates, government grants and the East Devon Pebblebed Heaths Conservation Trust, which employs full-time wardens and volunteers to look after the terrain. The Estate opened the heathland to public access "for air and exercise" following a legal deed it signed in 1930. The underlying geology of the area is mostly Bunter Pebblebeds of Triassic age, though there is some New Red Sandstone and marls of Permian age. Notable breeding bird species that have been recorded on the site include the European nightjar, Eurasian hobby and Dartford warbler.
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It stands at the foot of a mountain, where there is a cave called Belda, which is located on the north side of the town and belonging to mountain range called the "Sierra del Camorro." The mountain range consists of limestone and marls from the Jurassic period at a height of 907 meters. Situated on the summit of this mountain is a Paleolithic site leaving open the possibility in the past the existence of a castle and its forts, which were destroyed by the Moors. Within the cave, the existence of at least three lakes and numerous galleries is known of, which shows kilometers of stalactites, formed over decades.
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Though the hadrosaur sculpture was allowed to decay and crumble, some fragments have recently been located, all that now survives of Hawkins' ill-fated American dinosaur models. Extant drawings by Hawkins, along with other records, indicate that the Paleozoic Museum would have included life-sized restorations of the theropod Laelaps (=Dryptosaurus), the hadrosaurid Hadrosaurus, the plesiosaur Elasmosaurus, and the mosasaur Mosasaurus (all from the Upper Cretaceous marls of New Jersey), along with glyptodont models, a pair of giant ground sloth, giant Pleistocene elk, mammoths, and extinct mammalian carnivores. Hawkins models from the Crystal Palace exhibition have survived and can be seen today in Sydenham Park.
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The site has been attributed to either the Maksimovka or Salibez Formations and compared to the Bembridge Marls and Florissant Formation, both of which are Priabonian in age. At the time of description, the part and counterpart holotype queen specimen, numbers PIN 3429/1178 and PIN 3429/1173, was preserved in the A. A. Borissiak Paleontological Institute collections, part of the Russian Academy of Sciences. The fossil was first described by the trio of paleomyrmecologists Gennady Dlussky, Alexandr Rasnitsyn and Ksenia Perfilieva. In the type description, Dlussky, Rasnitsyn and Perfilieva coined the genus name Agastomyrma from a combination of the Latin agastus which means "pleasing" and Greek Myrmica meaning "ant".
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This strongly disturbed depositional environment with a coexistence of open marine facies and muds deposited under reducing conditions in a restrictive setting seems to coincide with a first sedimentary individualisation of the Pyrenean realm. The event has received its name Virgulian from the oyster Exogyra virgula. During the Tithonian, the shrinkage of the basin became even more evident, only to end in a nearly complete withdrawal of the sea from the Aquitaine Plateau before the close of the Tithonian (the south is not affected by this). During the Tithonian, iron-bearing calcareous oolites interbedded with marls, as well as dolomite and border facies deposits develop—dated by Gravesia portlandicum.
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The Belsa Formation is found within the Maestrazgo Basin. Within the stratigraphic sequence it overlies Jurassic rocks in a syn-rift unconformity, and underlies the Alacón Formation. The formation is up to 150 metres thick and is divided into three distinct unconformity bounded units, which are called the Lower, Middle and Upper Blesa Sequences. The Lower Blesa sequence varies greatly in thickness from less than 10 m up to 100 m is divided up into two members, the lower Cabezo Gordo Member, which consists of red clays and the upper Morenillo Member, which consists of limestones and marls, both of these sequences were deposited in a continental setting.
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Hayden gave the name "Santa Fe Marls" to the extensive sedimentary beds in the valley of the Rio Grande near Santa Fe during his 1869 survey of New Mexico and Colorado. He likened these to the badlands of South Dakota and correctly determined that they were upper Tertiary in age and were much younger than the Galisteo Formation beds which they overlie. He noted their great thickness, which he observed to be at least .Hayden 1869 By 1936, the Santa Fe Formation had been traced from central New Mexico into southern Colorado.Wilmarth 1936 Two years later, Bryan recognized that it extended at least from the San Luis Basin to beyond El Paso and was extensively faulted and deformed.
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37-39 La Toca Formation is cropping out in the northeast of the geologic map, while it is also present in the neighboring municipalities of Imbert and San Francisco Arriba. The formation in this area comprises rhythmic alternations of ochre fine-to- medium-grained, locally grading to course-grained sandstones and greyish clayey and ochre marls. This succession is locally cut by meters thick microconglomerates and conglomerates with rounded and subrounded clasts. Analysis of the clasts in San Francisco Arriba shows the clasts consist of up to ten percent of volcanic rock fragments, mainly limestone fragments (23-42%), quartz (8-33%), chert of up to five percent and minor metamorphic rock fragments.
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Early-Mid Jurassic (170 Ma) This formation is part of a near-shore to epicontinental marine-influenced deposits, coeval in age with the Sachrang Formation, that was more likely a linked pelagic deposit. After the drowning of the local Rhaetian reef slope and in the adjacent basin, Sinemurian–Toarcian local members were formed as a sequence of increasingly near pelagic sedimentation during the middle and late Liassic. The Coeval on the lowermost part Scheck Member has evidence of a series of large scale tectonic activities culminating during the late Pliensbachian and early Toarcian, probably linked to the Vulcanism of the adjacent Irkut Basin. In contrast to the "Adneter Mergel", the Saubach Formation lacks grey marls.
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Chaohusaurus is found in the same strata as Cartorhynchus Bed 633 of the Majiashan Quarry, the locality where Cartorhynchus was found, is a layer of grey argillaceous (clay-bearing) limestone located above the base of the Upper Member of the Nanlinghu Formation. It is defined above and below by layers of yellowish marls. In terms of ammonite biostratigraphy, this bed belongs to the Subcolumbites zone. High-resolution date estimates have been produced for the Olenekian-aged strata exposed in the Majiashan Quarry based on isotopic records of carbon-13 cycling and spectral gamma ray logs (which measure the amount of radiation in rocks of astronomical origin); Bed 633 in particular was estimated at 248.41 Ma in age.
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Early-Mid Jurassic (170 Ma) The Marne di Monte Serrone was first defined by Pialli in 1969.Pialli, 1969 The formation is characterised for be one of the most complete sections of the Toarcian paleobiographical strata around Europe.Palliani & Mattioli, 1994 It is also one of the best places on southern Europe where the strata shows the effects of the Lower Toarcian anoxic event (TAE). The formation also provides data about the changes after the Toarcian AE, with changes on the deposited micritic limestones and marls, what shows a local sedimentary response to the Toarcian climatic perturbation induced by the Vulcanism of the Southern Karoo-Ferrar that boiled the carbon cycle and change the mechanism of Earth climate.
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In soils rich in silica but not in salts, such as those of the Sierra Morena and the Montes de Toledo, spurge appears, accompanied, in the warmest places, by oleanders and tamarisks. In the lowlands further inland, above all in the marls and clay soils, field elms (Ulmus minor) and poplar groves are more common, with occasional ashes and willows. At the bottom of granite valleys and on the siliceous riverbanks, there are very typical formations of ash with Pyrenean oak, especially at the foot of thin interior mountain ranges. The sheltered gorges of the Serranía de Cuenca have mixed riparian forests of lime and hazel trees, with ashes, willows and Wych elm (Ulmus glabra).
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Kermack refrained from naming the animal or nominating a type specimen, as preparation of the fossils was still ongoing. The specimens were eventually named and thoroughly described by P. J. Crush in 1984, with the generic name Terrestrisuchus chosen to emphasise the terrestrial lifestyle of this crocodylomorph, and the specific name from the Latin gracilis for its light, graceful build. The Pant-y-ffynnon Quarry is composed mostly of Carboniferous limestone, but the fossils of Terrestrisuchus were recovered from Triassic sedimentary rocks that were deposited within fissures in the limestone (such as sandstones and marls). The age of the deposits has been historically debated, with older literature suggesting a Carnian to Norian age.
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The blue lias cliffs at Lyme Regis Formed somewhere between 185 Ma and 204 Ma, in what was then a shallow marine environment, the Lower Lias Lias is composed of Blue Lias, Black Ven Marls and Green Ammonite Beds (Charmouth Mudstone Formation). Mostly covered by lush vegetation, it forms the floor of Marshwood Vale in the west of Dorset and can be seen in stream beds, where the land has been excavated, and along the coast to the west of Seatown. The sides of the vale are mainly made from the clays and sands of the upper and lower Lias while younger strata from the Cretaceous Period (145–66 Ma), crown the higher points.Ensom (p.
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According to the Cultural Landscape Office of the Decentralization of the City of Cusco, the seven colors of the mountain are due to its mineralogical composition: the pink color is due to red clay, fangolitas (mud) and arilitas (sand); the whitish colouring is due to quartzose, sandstone and marls, rich in calcium carbonate; the red is due to claystones (iron) and clays belonging to the Upper Tertiary period; the green is due to phyllites and clays rich in ferro magnesian; the earthy brown is a product of fanglomerate composed of rock with magnesium belonging to the Quaternary period; and the mustard yellow color comes from the calcareous sandstones rich in sulphurous minerals.
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Around 11 specimens that might possibly be Bombini, some poorly documented, had been described by 2011; some (such as Calyptapis florissantensis from Florissant, USA, and Oligoapis beskonakensis from Beskonak, Turkey) dated from the Oligocene. In 2012 a fossil bumblebee, Bombus (Bombus) randeckensis was described from the Miocene Randeck Maar in southwestern Germany and confidently placed in the subgenus Bombus. In 2014, another species, Bombus cerdanyensis, was described from Late Miocene lacustrine beds of La Cerdanya, Spain, but not placed into any subgenus, while a new genus and species, Oligobombus cuspidatus was described from the late Eocene Bembridge Marls of the Isle of Wight. The species Bombus trophonius was described in October 2017 and placed in Bombus subgenus Cullumanobombus.
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At (53.4629, -2.4316), Chat Moss lies at the southern edge of the Lancashire Plain, an area of Bunter sandstones overlaid with marls laid down during the Late Triassic period. Those rocks are themselves overlaid by a layer of boulder clay deposited during the last ice age, about 10,000 years ago. The combination of the flat topography and the underlying clay resulted in extensive peat bogs developing along the Mersey Valley, and overflowing beyond the valley. The bogs in the area between the River Glaze in the west, and Worsley and Eccles in the east, to the north of what was the River Irwell – now the Manchester Ship Canal – are known collectively as Chat Moss.
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Map of the Bzyb River region Clays, marls, dolomites, and sandstones are encountered at the Bzyb River which flows down from a height of () in the western part of the Caucasus Major near and flows into the Black Sea at in two branches. Its valley borders the Bzyb Range, Gagra Range and some other ranges of Caucasus Major. The Bzyb River separates Arabika from the adjacent Bzyb Range, an outstanding karst area with many deep caves. An upper tributary of the river is the Jimsa River which flows in the area of the mountain of the same name. The Bzyb’ basin has the Lake Ritsa, which forms the headwaters of the Iupshara River.
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On the Aquitaine Plateau in the north, an interior shelf was constructed as far south as the line La Rochelle- Angoulême-Périgueux-Figeac. On this shelf the generally detritic transgression sediments of the Hettangian normally comprise a base conglomerate, arkoses, and fairly thick layers of sand- and mud-stones rich in plant material. The rest of the Hettangian is made up of marine sediments deposited in a restricted environment (lagoonal) evolving towards a lacustrine facies (green shales, coloured marls, dolomitic limestones and platy limestones rich in dwarf fossils, and evaporitic interlayers). The sediments of the Sinemurian are again fully marine and carry a pelagic fauna (soft banded limestones and hard lithographic limestones).
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The ground moraine and terminal moraine depositions of the Nauen Plateau are partially overlain by marls and glacial sands, left behind by the waters of the thawing ice sheet about 15,000 years before the end of the Weichsel glaciation. The glacial shaping of the relief resulted in a succession of glacial drift, confined space in a change from clays, tills, sands and gravels. On the slopes of the plateau above the Havel lowlands, layers of sand, 10 metres thick, occur at the surface near Groß Glienicke, Kladow and Gatow, such as at the Gatow hill of Windmühlenberg, on the Gatow Heath or near Karolinenhöhe. The dry, nutrient-poor sand here is ideal for the extreme habitat needed for dry grassland.
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By the Triassic, the Permian Zechstein Sea had retreated and the climate had become a little wetter giving a gentle transition making the Permian-Triassic boundary uncertain in northern England as there are no fossil horizons or facies changes that make a definitive separation possible as there in continental Europe. The horizon however is characterised by a succession of red marls (calcareous mudstones) deposited on coastal flats, followed by the Sherwood Sandstone (formerly Bunter Sandstone). The 'British Isles' were not islands, but had an intra-continental position within Pangea. The area that now constitutes Great Britain was drifting northwards as Pangea rotated, was at a latitude of 10° – 20° north, equivalent to the latitude of the present day Sahara desert.
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The site has been attributed to either the Maksimovka or Salibez Formations and compared to the Bembridge Marls and Florissant Formation, both of which are Priabonian in age. At the time of description, the part and counterpart holotype specimen, PIN 3429/1183 & PIN 3429/1164 was preserved in the A. A. Borissiak Paleontological Institute collections, part of the Russian Academy of Sciences. The fossil, an isolated head of a queen, was first described by the trio of paleomyrmecologists Gennady Dlussky, Alexandr Rasnitsyn, and Ksenia Perfilieva. In the type description, Dlussky, Rasnitsyn, and Perfilieva named the species G. incertus, with the specific epithet derived from the Latin incertus meaning "doubtful". G. incertus is distinguished from the other two species of Gesomyrmex described from Bol’shaya Svetlovodnaya in several ways.
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After a southeasterly re-advance of the sea in the Berriasian via a small strait east of Pau, which deposited 100 m of inter– to sub–tidal limestones and a sandy to clayey detrital border facies, emersion set in during the Neocomian. During Valanginian and Hauterivian times, clayey marls on top of the emerged horsts were transformed under ferralitic climatic conditions into bauxites, which were fossilised by later transgressions. After another marine transgression from the east during the Barremian, the elongated graben regions in the Pyrenean domain received 200 to 300 m of marine shelf sediments of the Urgonian facies, such as dolomites, algal limestones, foraminiferous limestones, and rudist limestones. The Urgonian facies can perdure in the Corbières and in the South Pyrenean Zone into the Albian.
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He was the third son of Francesco Fornasini, a medical doctor, and his wife Carlotta (). He studied natural sciences at the University of Bologna, under the guidance of Giovanni Capellini (1833-1922), the Professor of Geology there. In 1877, he graduated with honours as dottore (in effect, PhD), on the basis of a thesis which argued from the sequence of the fossil record that certain chalks, marls and clays in the Savena valley near Bologna dated from the Pliocene (5.3-2.6 Ma) rather than, as had previously been thought (including by Capellini), from the Miocene (23.0-5.3 Ma). That same year, Capellini published a paper about this discovery which relegated Fornasini's contribution to that of an assistant and which passed off Fornasini's conclusions as his own.
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View from the Eiserner Steg into the depths of the gorge The gorge around 1900 The gorge in winter In the Triassic, about 240 million years ago, on the bed of a shallow sea, dark grey, relatively hard layers of Alpine muschelkalk, so- called Wurstelkalk, were laid down in the area of the present day Partnach Gorge. On the bead-like strata of this rock the traces of the burrowing and feeding of marine animals can still be seen. Importantly, about 5 million years later, softer marls were deposited in the same marine basin, which today are known as Partnach Strata (Partnach-schichten). In the course of the subsequent Alpine mountain folding the so-called Warnberg Saddle (Warnberger Sattel) was formed from these rock strata.
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Evidence for anoxia include the high amounts of organic matter, lack of evidence for benthic organisms (fossils or trace fossils), and enrichment in the redox proxies molybdenum and vanadium. After the significant drop in sea level (marine regression) associated with deposition of the Woodbine during the Early Cenomanian, the sea level began to rise (marine transgression), allowing for the deposition of Lower Eagle Ford organic-rich marls in South Texas and limestones of the Terrell Member of the Boquillas Formation in West Texas starting at about 96 million years ago. Gardner, R. D., M. C. Pope, M. P. Wehner, and A. D. Donovan (2013) “Comparative stratigraphy of the Eagle Ford Group in Lozier Canyon and Antonio Creek, Terrell County, Texas”: GCAGS Journal, v. 2, p. 42-52.
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Approximately from the late Berriasian to late Albian (120 to 100 Ma), the Iberian Plate was an isolated island, separated from current southern France by a mostly shallow sea with a deeper pelagic channel in between the southwestern Eurasian and northeastern Iberian coasts. The present-day area of the Pyrenees with an area of in those times was much larger due to the various episodes of compressional tectonic forces and resulting shortening afterwards. The Tremp Basin, alternatively called Organyà Basin, was the depocenter of sedimentation during the late Early Cretaceous, showing an estimated vertical sedimentary thickness of comprising mostly hemipelagic marls and limestones,García Senz, 2002, p.7 deposited in a back-arc basin setting with normal faults parallel to the Pyrenean axis,García Senz, 2002, p.
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The site has been attributed to either the Maksimovka or Salibez Formations and compared to the Bembridge Marls and Florissant Formation, both of which are Priabonian in age. At the time of description, the holotype adult specimen, number PIN 3429/104 was preserved in the A. A. Borissiak Paleontological Institute collections, part of the Russian Academy of Sciences. The fossil was first described by the trio of paleomyrmecologists Gennady Dlussky, Alexandr Rasnitsyn and Ksenia Perfilieva. In the type description, Dlussky, Rasnitsyn and Perfilieva named the species P. aberrans, with the specific epithet derived the Latin aberrans meaning "aberrant" or "to deviate". P. aberrans is one of two Pachycondyla species that were described by Dlussky, Rasnitsyn and Perfilieva from Bol’shaya Svetlovodnaya, the other species P. oligocenica being described from a male.
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The most active part of the Zagros is the 'Simply Folded Belt', which is characterised by large folds formed above a layer of late Neoproterozoic to Early Cambrian Hormuz salt, which locally reaches the surface in the crests of some anticlines as salt diapirs. The sedimentary rocks above the salt layer comprise a basal Cambrian conglomerate and a thick sequence of limestones of Palaeozoic to Upper Cretaceous age, known together as the 'Competent Group' due to their relatively high competence, followed by a sequence of mechanically weaker marls and interbedded limestones of latest Cretaceous to Lower Miocene age topped by Neogene sandstones and conglomerates. There is evidence of intermediate level detachment at some of the weaker layers, leading to folds at different stratigraphic levels have different locations, orientations or wavelengths.Nissen et al.
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H. Tintant says that most of the waters of the Bèze come from underground drainage of the immense karst plateau consisting of rauracian and sequanian limestones forming a quadrilateral limited to the north by the impenetrable Argovian marls from Crécey-sur-Tille to Occey and the valley of the Vingeanne. Covered by dry valleys and perforated with numerous funnels (several hundred in the Velours forest alone), this plateau, which measures more than , is covered with very permeable rocks with a small but discernible slope to the south. The underground river feeding the Bèze at its source probably collects 50% of the annual rainfall on the plateau. Fluorescein tests carried out by the Speleo- Club of Dijon in 1970 showed that the waters of Venelle colored those of the Bèze in the caves of the spring.
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Eagle Ford stratigraphic column Outcrop of the Eagle Ford and Austin Chalk Contact off Kiest Blvd, 1/2 mile east of Patriot Pky in Dallas County The Eagle Ford Group (also called the Eagle Ford Shale) is a sedimentary rock formation deposited during the Cenomanian and Turonian ages of the Late Cretaceous over much of the modern-day state of Texas. The Eagle Ford is predominantly composed of organic matter-rich fossiliferous marine shales and marls with interbedded thin limestones. It derives its name from outcrops on the banks of the West Fork of the Trinity River near the old community of Eagle Ford,Hill, R. T. (1887) The topography and geology of the Crosstimbers and surrounding regions in North Texas: American Journal of Science, v. 33, no.
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Walton Hill, Polden Hills The Poldens are a low narrow ridge of late Triassic / early Jurassic mudstones (often referred to as clay) alternating with limestones. The south-southwest facing scarp is formed by a succession of rocks, lowermost of which are the mudstones of the Mercia Mudstone Group (formerly known as the Keuper Marl), overlain in the west by more mudstones of the latest Triassic age Blue Anchor Formation (formerly ‘Tea Green Marls’), a thin unit recorded from Puriton Hill east to the vicinity of Stawell. Elsewhere the overlying layer is that of the earliest Jurassic (Rhaetian) age Westbury Formation (formerly known as the Rhaetic clays or Westbury Beds) consisting of mudstones and limestones. Stratigraphically above these are the mudstones and limestones of the Blue Lias, forming the north-northeasterly directed dip-slope of these hills.
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Early-Mid Jurassic (170 Ma) The Jurassic sedimentation is subdivided on several different units, with drastic changes in the Northern Calcareous Alps. During the Toarcian, carbonate platforms collapsed and several types of bottom reliefs where generated due to tectonic activity, where on the submarine swells the red nodular limestones with an exposure of 20 m of the Adnet Formation were deposited on zones of basinal sedimentology, know due to the presence of grey limestone and marl on an up to 200 m layer of the Allgäu Formation. The marls of the Sachrang Formation are part of the Lower Toarcian "Black Shale deposition", contemporaneous of other events on central Germany and England. The Sachrang Formation was geologically divided in the Sachrang Member, that presents typical development of a basinal area and the Unken Member, with benthic microfossils with suboxic water influence.
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There is a clear low frequency of Vitrinite and Inertinite, what suggests that terrestrial inputs of organic matter to be of less importance, although, the main part of OM contained in the basal mudstone, including charred material, was derived from terrestrial sources. This Mudstone contains charred organic material typically connected to Wildfires along with large amounts of expandable Smectite possibly derived from alteration of volcanic ash, what indicated a clear contribution of volcanic-derived detritus during deposition of the Bächental bituminous marls, whose genesis was probably linked to the rift history of the Valais, Briançonnais and Piemonte-Liguria domains (Sinemurian-Callovian), and the Toarcian break-up of the Ligurian-Penninic oceanic realm.G. Mohn, G. Manatschal, O. Müntener, M. Beltrando, E. Masini Unravelling the interaction between tectonic and sedimentary processes during lithospheric thinning in the Alpine Tethys margins Int. J. Earth Sci.
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In 1845, the Nottingham Enclosure Act was obtained, which allowed the city to expand onto the surrounding land. The water companies had been in open competition for more than a decade, with no legal boundaries to define which areas each could supply, but to meet the challenges of the enlarging city, the Nottingham Water Act was also obtained in 1845, which formally merged the three companies into one, to be known as Nottingham Waterworks Company. Hawksley, as the most prominent engineer involved with any of the original enterprises, became consulting engineer for the new company, a position that he held until it was taken over by the Corporation in 1879. Nottingham sits on top of a huge area of Bunter sandstone, which holds large volumes of groundwater, which is prevented from seeping lower by an underlying layer of impermeable Permian marls.
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The most active part of the Zagros is the Simply Folded Belt, which is characterised by large folds formed above a layer of late Neoproterozoic to Early Cambrian Hormuz salt, which locally reaches the surface in the crests of some anticlines as salt diapirs. The sequence of sedimentary rocks above the salt layer comprises a basal Cambrian conglomerate beneath a thick sequence of limestones of Palaeozoic to late Cretaceous age, known together as the "Competent Group" owing to their relatively high mechanical strength, overlain by a sequence of weaker marls and interbedded limestones of latest Cretaceous to early Miocene age, topped by Neogene sandstones and conglomerates. There is evidence of intermediate level detachment at some of the weaker layers, which means that folds at different stratigraphic levels may have different locations, orientations, or wavelengths.Nissen et al.
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The Albacora field consists of several producing horizons of Albian to Miocene sandstone turbidites, with an area of 235 km2.Candido, A., and Cora, C.A.G., 1992, The Marlim and Albacora Giant Fields, Campos Basin, Offshore Brazil, AAPG Memoir 54, Halbouty, M.T., editor, Tulsa: American Association of Petroleum Geologists, Reflection seismology in 1972 disclosed a faulted anticline and seismic amplitude bright spot, which was drilled by wildcat 1-RJS-297 in 1984 and discovered oil. The stratigraphy of the Campos Basin starts with the Lower Cretaceous Lago Feia Formation a source rock, followed by the Albian Macae Formation consisting of shallow water carbonates overlain by late Albian shales, marls, calcilutites, and turbidite sandstones. From this formation through most of the Cenozoic, the Campos Formation was deposited, consisting of deep water turbiditic sandstones and shales, the main producers in the Albacora and Marlim fields.
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The Marlim field consists of a single Oligocene producing horizon of sandstone turbidites, with an area of 152 km2.Candido, A., and Cora, C.A.G., 1992, The Marlim and Albacora Giant Fields, Campos Basin, Offshore Brazil, AAPG Memoir 54, Halbouty, M.T., editor, Tulsa: American Association of Petroleum Geologists, Reflection seismology in 1972 disclosed a faulted anticline and seismic amplitude bright spot, which was drilled by wildcat 1-RJS-219A in 1985 and discovered oil. The stratigraphy of the Campos Basin starts with the Lower Cretaceous Lago Feia Formation a source rock, followed by the Albian Macae Formation consisting of shallow water carbonates overlain by late Albian shales, marls, calcilutites, and turbidite sandstones. From this formation through most of the Cenozoic, the Campos Formation was deposited, consisting of deep water turbiditic sandstones and shales, the main producers in the Albacora and Marlim fields.
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If one ignores, for the moment, the influence of the mountains, the typical Mediterranean peninsular forest is made up of evergreen trees: oak forests, cork oaks, wild olives, juniper, and so on. These are accompanied or replaced in the warmer regions and eroded by forests of Aleppo pine (Pinus halepensis) and in areas of sandy ground and fixed sand dunes by juniper and stone pine forests. Exceptions to the rule are the more arid region in the southeast, the lower regions of the provinces of Murcia and Almeria, where the only vegetation is the European fan palm (Chamaerops humilis), and thorny thickets of blackthorn and at higher altitudes, Kermes oak groves and mastic (Pistacia lentiscus). The same can be said of the salty or endorheic zones, with great differences in temperature, such as the depression of the Ebro, Hoya de Baza and the chalky marls further inland.
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Artist's impression The fossil record of P. pervetus includes many complete skeletons from Green River Formation sites (Early Eocene), suggesting that the birds nested in colonies and possibly were liable to succumb to botulism, similar to many colony-nesting waterfowl or shorebirds today. P. isoni is known from the Late Paleocene Aquia Formation (Maryland, 61-62 MYA) humerus (USNM 294116) and a fingerbone (USNM 294117) that were initially described, as well as from the humeri that were initially believed to be from Headonornis (BMNH PAL 3686, 5105, 6240). As these are Late Eocene or even Early Oligocene (BMNH PAL 5105, Bembridge Marls) in age, they possibly belong to a distinct taxon. P. recurvirostris is a disputed species possibly synonymous with P. pervetus; it is known from a partial wing (KUVP 10105) found in Colton Formation Eocene sediments of the Wasatch Plateau near Ephraim, Utah.
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He spent much of his time improving methods for analytical chemistry, and applying them to problems in chemical analysis. The mineral liebigite He examined various problems in agricultural chemistry, including the composition of soils, the value of marls and fossil bones, and the growing of cotton. As a result, he was selected by Secretary James Buchanan to go to Turkey, in response to a request from the Sultan of Turkey for a scientific advisor on cultivating cotton. Between 1846 and 1850, Smith investigated the mineral resources of Turkey, for Turkey's government, and he discovered deposits of coal, chrome ore, and the famous emery deposits of Naxos. In Turkey he also discovered liebigite,STUDIES OF URANIUM MINERALS (II): LIEBIGITE AND URANOTHALLITE, Howard T. Evans, Clifford Frondel (Massachusetts Institute of Technology; Harvard University); 1950.The crystal structure of Liebigite, K. Mereiter, Mineralogy and Petrology (Volume 30, Number 4 / December 1982), 18 November 1982.
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The deep parts of Krubera display a more pervasive conduit pattern with a mixture of phreatic morphology, characteristic of the zone of high-gradient floods, which can be up to 400 m above the low-flow water table, and vadose downcutting elements that are observed even below the water table. The core part of the Arabika Massif is composed of the Upper Jurassic succession resting on the Bajocian Porphyritic Series, which includes sandstones, clays and conglomerates at the top, and tuff, tuffaceous sandstones, conglomerates and breccia, porphyry and lava. The Porphyritic series forms the non-karstic basement of Arabika, which is exposed only on the northern and eastern outskirts, locally in the bottoms of the Kutushara and Gega River valleys. In the central part of Arabika the Cretaceous cover (Valanginian and Hauterivian limestones, marls and sandstones) is retained only in a few ridges and peaks, but it lies intact through the low-altitude ridges to the south-west of the central part.
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Precipitation and groundwater react with such rocks as dolomite, limestone, and marble, dissolving the rock and forming small fissures and chambers allowing more water to enter and the dissolve the carbonic rock. Being able to identify the different types of rock that caves are likely to form in can provide a great deal of background into a cave's likely history, and thus these rock formations will be further discussed moving east to west across the state. Coastal Plain – this is the area of Maryland extending from just west of the Chesapeake Bay to the Atlantic Ocean: Precambrian rocks are mostly overlain by gravel, silts, marls, and sands, and consequently no solutional caves are known to exist in this region of Maryland. Piedmont Plateau – an area of gently rolling hills and flatlands, the Piedmont is home to only a few of Maryland's caves, as most of its members are unsuitable for their development or are largely hidden from view beneath surface settlement.
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We can affirm that the parietal levels of the studied structures show in general a low influence of the human activity, though we have documented an increase of the slimy fraction to the levels of the structure 10 and to the top level of the structure 14, which it might mean that the substratum was affected by the human activities throughout the period of occupation. Inside the perceived uniformity, there are two remarkable associations: on the one hand there are two types of substratum for the levels, and on the other hand, the samples of the structures 14 and 10 come from calcareous tertiary marls. The structures 19 and 1 come on the other hand from sediments few carbohydrate of gray color and with more organic matter, that we might associate with a substratum Miocene different from the typical calcareous marl or from holocene edaphic formations. On the other hand, the top units seem to possess characteristics that indicate a light worsening in the environmental conditions, though they all in general reflect a few conditions similar to the current ones, result of an evolution from previous moments with more favorable conditions (homestead edaphics levels ).
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