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25-829: The Ebro Basin was a foreland basin that formed to the south of the Pyrenees during the Paleogene . It was also limited to the southeast by the Catalan Coastal Ranges . It began as a fully marine basin with connections to both the Atlantic Ocean and the Mediterranean Sea, before becoming an endorheic basin during the Late Eocene . In the Miocene

50-607: A regime's tectonic origin and development as well as the lithospheric mechanics. Migrating fluids originate from the sediments of the foreland basin and migrate in response to deformation. As a result, brine can migrate over great distances. Evidence of long-range migration includes: 1) correlation of petroleum to distant source rocks , 2) ore bodies deposited from metal-bearing brines, 3) anomalous thermal histories for shallow sediments, 4) regional potassium metasomatism and 5) epigenetic dolomite cements in ore bodies and deep aquifers. Fluids carrying heat, minerals, and petroleum, have

75-510: A thorough definition of the foreland basin system. Foreland basin systems comprise three characteristic properties: The wedge-top sits on top of the moving thrust sheets and contains all the sediments charging from the active tectonic thrust wedge. This is where piggyback basins form. The foredeep is the thickest sedimentary zone and thickens toward the orogen. Sediments are deposited via distal fluvial, lacustrine, deltaic, and marine depositional systems. The forebulge and backbulge are

100-454: A vast impact on the tectonic regime within the foreland basin. Before deformation, sediment layers are porous and full of fluids, such as water and hydrated minerals. Once these sediments are buried and compacted, the pores become smaller and some of the fluids, about ⁠ 1 / 3 ⁠ , leave the pores. This fluid has to go somewhere. Within the foreland basin, these fluids potentially can heat and mineralize materials, as well as mix with

125-410: Is a factor of temperature and time and occurs at shallower depths due to past heat redistribution of migrating brines. Vitrinite reflectance, which typically demonstrates an exponential evolution of organic matter as a function of time, is the best organic indicator for thermal maturation. Studies have shown that present day thermal measurements of heat flow and geothermal gradients closely correspond to

150-426: Is a function of topographic relief. For the loading model, the lithosphere is initially stiff, with the basin broad and shallow. Relaxation of the lithosphere allows subsidence near the thrust, narrowing of basin, forebulge toward thrust. During times of thrusting, the lithosphere is stiff and the forebulge broadens. The timing of the thrust deformation is opposite that of the relaxing of the lithosphere. The bending of

175-585: Is found closer to the orogen and oil is found further away. Geology of Svalbard The geology of Svalbard encompasses the geological description of rock types found in Svalbard , and the associated tectonics and sedimentological history of soils and rocks. The geological exploration of Svalbard is an ongoing activity, and recent understandings may differ from earlier interpretations. Geological basement dated from Precambrian , Cambrian , Ordovician and Silurian , originally termed Hecla Hoek ,

200-774: Is found in three different provinces. The southwestern terrain comprises Prins Karls Forland , Oscar II Land , Nordenskiöld Land west of Grønfjorden and Wedel Jarlsberg Land . The northwestern terrain includes Haakon VII Land and Albert I Land . The northeastern terrain comprises Nordaustlandet and the northeastern parts of Spitsbergen . Devonian age sediments are exposed in Andrée Land , James I Land and Dickson Land . Orogeny took place in late Devon. During Carboniferous and Permian , rift basins were formed. Carboniferous strata are found along Billefjorden , and Permian formations dominate Billefjorden, Tempelfjorden and Lomfjorden . Triassic rocks are found at

225-402: The active deformation zone with which it is connected. Today GPS measurements provide the rate at which one plate is moving relative to another. It is also important to consider that present day kinematics are unlikely to be the same as when deformation began. Thus, it is crucial to consider non-GPS models to determine the long-term evolution of continental collisions and in how it helped develop

250-399: The adjacent foreland basins. Comparing both modern GPS (Sella et al. 2002) and non-GPS models allows deformation rates to be calculated. Comparing these numbers to the geologic regime helps constrain the number of probable models as well as which model is more geologically accurate within a specific region. Seismicity determines where active zones of seismic activity occur as well as measure

275-436: The basin becomes completely filled. At this point, the basin enters the overfilled stage and deposition of terrestrial clastic sediments occurs. These are known as molasse . Sediment fill within the foredeep acts as an additional load on the continental lithosphere. Although the degree to which the lithosphere relaxes over time is still controversial, most workers accept an elastic or visco-elastic rheology to describe

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300-5214: The basin was captured by a precursor to the Ebro river and the new drainage system that developed eroded away much of the basin fill, except for resistant lithologies, such as the conglomerates at Montserrat . References [ edit ] ^ Guerrero J.; Gutiérrez F.; Gutiérrez M. (2014). Gutiérrez F.; Gutiérrez M. (eds.). Conglomerate Monoliths and Karst in the Ebro Cenozoic Basin, NE Spain . Springer. ISBN   978-94-017-8627-0 . {{ cite book }} : |work= ignored ( help ) v t e Geology of Europe Countries Albania Andorra Armenia Austria Azerbaijan Belarus Belgium Bosnia and Herzegovina Bulgaria Croatia Cyprus Czech Republic Denmark Faroe Islands Estonia Finland Åland Islands France Georgia Germany Greece Hungary Iceland Ireland Italy ( Sicily ) Kazakhstan Kosovo Latvia Liechtenstein Lithuania Luxembourg Malta Moldova Monaco Montenegro Netherlands North Macedonia Norway Jan Mayen Svalbard Poland Portugal Romania Russia San Marino Serbia Slovakia Slovenia Spain Sweden Switzerland Turkey Ukraine United Kingdom England Northern Ireland Scotland Wales Gibraltar Alderney Guernsey Jersey Isle of Man [REDACTED] Geologic regions Orogens Acadian Alpine Belomorian Cadomian Caledonian Carpathian Dalslandian Gothian Grampian Hallandian-Danopolonian Hellenic Laxfordian Lopian Saamian Scandian Scourian Timanide Svecofennian Sveconorwegian Uralian Variscan Mountain ranges Alps Apennines Caucasus Dinaric Alps Harz Massif Central Ore Mountains Pyrenees Scandinavian Mountains Sudetes Urals Western Carpathians Oceanic basins Atlantic Ocean Arctic Ocean Bay of Biscay Black Sea Mediterranean Sea Norwegian Sea Intracontinental basins and grabens Aquitaine Basin Barents Basin Baltic Sea Basin Central Lowlands Dnieper–Donets Rift Ebro Basin European Cenozoic Rift System Hellenic Trench Limagne Graben Mezen Basin Molasse Basin Moscow Basin North Sea Basin Oslo Rift Pannonian Basin Paris Basin Peri-Caspian Depression Timan-Pechora Basin White Sea Rift System Tectonic plates and microcontinents Adriatic plate Aegean Sea plate Anatolian plate Eurasian plate Iberian plate Jan Mayen Microcontinent Moesian plate Pelso plate Tisza plate Terranes Armorican terrane Avalonia Baltica Cimmeria East European Craton Fennoscandian Craton Sarmatian Craton Volgo–Uralia UNESCO World Heritage Sites Aeolian Islands Aggtelek Calanques de Piana Curonian Spit Dolomites Durmitor Geirangerfjord Giant's Causeway Glarus High Coast Jungfrau-Aletsch Jurassic Coast Komi Kvarken Laponia Messel Pit Meteora Monte Perdido Monte San Giorgio Mount Etna Nærøyfjord Pirin Plitvice Rhine Gorge Scandola Škocjan St Kilda Stevns Klint Surtsey Thingvellir Retrieved from " https://en.wikipedia.org/w/index.php?title=Ebro_Basin&oldid=1258921976 " Categories : Foreland basins Geology of Spain Geology of Catalonia Hidden category: CS1 errors: periodical ignored Foreland basin Foreland basins can be divided into two categories: DeCelles & Giles (1996) provide

325-497: The lithosphere under the orogenic load controls the drainage pattern of the foreland basin. The flexural tilting of the basin and the sediment supply from the orogen. Strength envelopes indicate that the rheological structure of the lithosphere underneath the foreland and the orogen are very different. The foreland basin typically shows a thermal and rheological structure similar to a rifted continental margin with three brittle layers above three ductile layers. The temperature underneath

350-458: The lithosphere. Thus, the thrust belt is mobile and the foreland basin system becomes deformed over time. Syntectonic unconformities demonstrate simultaneous subsidence and tectonic activity. Foreland basins are filled with sediments which erode from the adjacent mountain belt. In the early stages, the foreland basin is said to be underfilled . During this stage, deep water and commonly marine sediments, known as flysch , are deposited. Eventually,

375-425: The lithospheric deformation of the foreland basin. Allen & Allen (2005) describe a moving load system, one in which the deflection moves as a wave through the foreland plate before the load system. The deflection shape is commonly described as an asymmetrical low close to the load along the foreland and a broader uplifted deflection along the forebulge. The transport rate or flux of erosion, as well as sedimentation,

400-457: The local hydrostatic head. Orogen topography is the major driving force of fluid migration. The heat from the lower crust moves via conduction and groundwater advection . Local hydrothermal areas occur when deep fluid flow moves very quickly. This can also explain very high temperatures at shallow depths. Other minor constraints include tectonic compression, thrusting, and sediment compaction. These are considered minor because they are limited by

425-411: The orogen is much higher and thus greatly weakens the lithosphere. According to Zhou et al. (2003), "under compressional stress the lithosphere beneath the mountain range becomes ductile almost entirely, except a thin (about 6 km in the center) brittle layer near the surface and perhaps a thin brittle layer in the uppermost mantle." This lithospheric weakening underneath the orogenic belt may in part cause

450-404: The passive margin stage with orogenic loading of previously stretched continental margin during the early stages of convergence. Second, the "early convergence stage defined by deep water conditions", and lastly a "later convergent stage during which a subaerial wedge is flanked with terrestrial or shallow marine foreland basins". The temperature underneath the orogen is much higher and weakens

475-498: The regional lithospheric flexure behavior. Foreland basins are considered to be hypothermal basins (cooler than normal), with low geothermal gradient and heat flow . Heat flow values average between 1 and 2 HFU (40–90 mWm . Rapid subsidence may be responsible for these low values. Over time sedimentary layers become buried and lose porosity. This can be due to sediment compaction or the physical or chemical changes, such as pressure or cementation . Thermal maturation of sediments

500-401: The slow rates of tectonic deformation, lithology and depositional rates, on the order of 0–10 cm yr , but more likely closer to 1 or less than 1 cm yr . Overpressured zones might allow for faster migration, when 1 kilometer or more of shaley sediments accumulate per 1 million years. Bethke & Marshak (1990) state that "groundwater that recharges at high elevation migrates through

525-528: The southern part of Spitsbergen , at Edgeøya , Barentsøya and Kong Karls Land . It is particularly visible at Edgeøya, Barentsøya and in eastern part of Olav V Land . Triassic outcrops are exposed in a long and narrow belt between pre-Triassic sediments along the west coast and the post-Triassic sediments of the central basin. The Triassic rock units are divided into the Sassendalen Group , dating from Early Triassic to Late Middle Triassic, and

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550-441: The subsurface in response to its high potential energy toward areas where the water table is lower." Bethke & Marshak (1990) explain that petroleum migrates not only in response to the hydrodynamic forces that drive groundwater flow, but to the buoyancy and capillary effects of the petroleum moving through microscopic pores. Migration patterns flow away from the orogenic belt and into the cratonic interior. Frequently, natural gas

575-487: The succeeding Kapp Toscana Group . Jurassic , Cretaceous and Cenozoic rocks are exposed in the middle southern part of Spitsbergen. Coal deposits from Paleogene are exploited in Longyearbyen (including Svea ) and Barentsburg . The post-glacial rebound is estimated to be up to three kilometers in central Spitsbergen, while only a few hundred meters at Kong Karls Land . This geology article

600-429: The thinnest and most distal zones and are not always present. When present, they are defined by regional unconformities as well as aeolian and shallow-marine deposits. Sedimentation is most rapid near the moving thrust sheet. Sediment transport within the foredeep is generally parallel to the strike of the thrust fault and basin axis. The motion of the adjacent plates of the foreland basin can be determined by studying

625-501: The total fault displacements and the timing of the onset of deformation. Foreland basins form because as the mountain belt grows, it exerts a significant mass on the Earth's crust, which causes it to bend, or flex, downwards. This occurs so that the weight of the mountain belt can be compensated by isostasy at the upflex of the forebulge. The plate tectonic evolution of a peripheral foreland basin involves three general stages. First,

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