RSS Cientifico geral Geodynamics and sea-level changes in the Meso-Cenozoic: : from the global evolution to the Lisbon Metropolitan Area

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Breve resumo:
This article presents an evolution of geodynamics and eustatic sea-level changes in theMeso-Cenozoic and relates global events to the formation of Iberia and the Lisbon MetropolitanArea (LMA). The distensive tectonic regime resulted in the breakup of Pangea, the separationbetween the North American and Eurasian plates and the individualization of the Iberianmicroplate in the Lower Cretaceous. Rift basins were developed until the formation of oceaniccrust in the Atlantic. The Lusitanian Basin is linked to the genesis of the Meso-Cenozoic WesternPortuguese Border, where a large part of the Northern LMA is included. The compressiveregime from the end of Cretaceous gave rise to mountain ranges in the Iberian Peninsula andto the reactivation of late-hercinian faults responsible for the formation and subsidence of atectonic depression (Cenozoic Basin of the Tagus-Sado), where most of the Southern LMA isincluded. It was in this tectonic framework that the subvolcanic massif of Sintra was formed atthe end of the Upper Cretaceous or the Arr谩bida chain during the Miocene. The transition tothe compressive regime marked the maximum sea-level in the Meso-Cenozoic (170 to 250mabove the current level). The variations in sea-level explain the LMA鈥檚 lithological diversity. Theformations of the Northern LMA date mostly from Cretaceous (prevalence of limestones andmarls), while more recent formations are prevailing in the Southern LMA (Pliocene and Pleistocene),which justifies its detrital character.​



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This article presents an evolution of geodynamics and eustatic sea-level changes in theMeso-Cenozoic and relates global events to the formation of Iberia and the Lisbon MetropolitanArea (LMA). The distensive tectonic regime resulted in the breakup of Pangea, the separationbetween the North American and Eurasian plates and the individualization of the Iberianmicroplate in the Lower Cretaceous. Rift basins were developed until the formation of oceaniccrust in the Atlantic. The Lusitanian Basin is linked to the genesis of the Meso-Cenozoic WesternPortuguese Border, where a large part of the Northern LMA is included. The compressiveregime from the end of Cretaceous gave rise to mountain ranges in the Iberian Peninsula andto the reactivation of late-hercinian faults responsible for the formation and subsidence of atectonic depression (Cenozoic Basin of the Tagus-Sado), where most of the Southern LMA isincluded. It was in this tectonic framework that the subvolcanic massif of Sintra was formed atthe end of the Upper Cretaceous or the Arr谩bida chain during the Miocene. The transition tothe compressive regime marked the maximum sea-level in the Meso-Cenozoic (170 to 250mabove the current level). The variations in sea-level explain the LMA鈥檚 lithological diversity. Theformations of the Northern LMA date mostly from Cretaceous (prevalence of limestones andmarls), while more recent formations are prevailing in the Southern LMA (Pliocene and Pleistocene),which justifies its detrital character.



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