Basin Analysis Análise de Bacias Part 1 - geomuseu.ist.utl.ptgeomuseu.ist.utl.pt/GSP2012/Basin...
Transcript of Basin Analysis Análise de Bacias Part 1 - geomuseu.ist.utl.ptgeomuseu.ist.utl.pt/GSP2012/Basin...
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Basin Analysis Análise de Bacias
Part 1
Introduction Mechanisms of Basin Formation
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Basin Analysis
• Introduction • Mechanisms of Basin Formation • Basin Classification • Basins and Sequence Stratigraphy • Summary
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Introduction
Basin analysis - Study of sedimentary rocks to determine: • Subsidence history • Stratigraphic architecture • Paleogeographic evolution Tools: Geology (outcrops, wireline logs, core) Geophysics (seismic, gravity, aeromag) Computers (modeling, data analysis)
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FORÇAS E ORDENS DE RELEVO Shaping the world
FORÇAS QUE MODELAM A TERRA
ENDÓGENAS EXÓGENAS
TERRA UM PLANETA DINÂMICO
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FORÇAS E ORDENS DE RELEVO
ORDENS DE RELEVO
CONTINENTES BACIAS OCEÂNICAS
PLACAS TECTÓNICAS
MODELADOS /bacias sedimentares
1
2
3
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PRIMEIRA ORDEM DE RELEVO First approach
CONTINENTES E BACIAS OCEÂNICAS
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Morfologia submarina no Atlântico
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Planície abissal Ibérica Depocentros actuais Actual depocenters
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Planície abissal Portuguesa ( Perfil Sísmico LUSIGAL)
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PRIMEIRA ORDEM DE RELEVO
CONTINENTES E BACIAS OCEÂNICAS
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Morfologia Submarina
Vida no meio marinho
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SEGUNDA ORDEM DE RELEVO Second approach
PLACAS TECTÓNICAS Rever o
Tem
a 5
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TERCEIRA ORDEM DE RELEVO
MODELADOS
Quais são os agentes modeladores? Agents ? Energy?
• Gravidade • Águas pluviais e de escorrência • Cursos de água • Lagos • Glaciares • Vento • Mar • Águas subterrâneas • Seres Vivos (incluindo o Homem)
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Factores intervenientes no ciclo evolutivo das rochas External Geodinamics
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Introduction
What is a basin? • Repository for sediment • Formed by crustal subsidence relative to surrounding areas • Surrounding areas sometimes uplifted • Many different shapes, sizes and •mechanisms of formation
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Introduction
Zonation of the Earth-Composition
• Crust • Mantle • Core
See other revision presentation on this subject!
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PRINCIPAIS TIPOS DE CRUSTA
A crusta ou crosta terrestre constitui a parte rígida superior da litosfera, na base da qual se define uma descontinuidade sísmica de primeira ordem – Descontinuidade de Mohorovicic ou Moho (linha vermelha). Consideram-se três tipos principais de crusta:
Oceânica Transicional Continental
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PRINCIPAIS TIPOS E SUBTIPOS DE CRUSTA
Os 3 tipos principais de crosta são habitualmente divididos em 13 subtipos
Cada subtipo representa uma porção de crusta com características geológicas e geofísicas próprias
Área aflorante (inclui domínio oceânico)
Volume da crosta
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Escudos e Plataformas Orógeno de colisão
Arco vulcânico insular
Arco de margem continental
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Rifte continental Plateau oceânico
Bacia oceânica
Cordilheira oceânica
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Introduction
Zonation of the Upper Earth –Rheology Lithosphere Rigid outer shell Crust and upper mantle Asthenosphere Weaker than lithosphere Flows (plastic deformation)
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COMPORTAMENTOS MECÂNICOS DA CROSTA
Mechanical behaviour of
the crust
Comportamento frágil ou rígido
Comportamento plástico
O comportamento da crusta continental sujeita a esforços está dependente da temperatura e da duração de aplicação dessas tensões. Quanto mais quente estiver a crusta mais esta se comportará como um sólido dúctil que se deforma plasticamente; por outro lado crustas frias tendem a ter um comportamento mais elástico, observando-se frequentemente fracturas e deslizamentos por fricção.
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TRANSIÇÃO FRÁGIL – DÚCTIL (TFD)
Como a temperatura da crosta aumenta com a profundidade, observa-se uma mudança de comportamento, relativamente à deformação, de frágil para dúctil, uma vez ultrapassado um determinado limite. Esta transição frágil-dúctil ocorre apenas a cerca de 20 km de profundidade nos riftes pois aí o fluxo de calor é muito grande.
Mais aspectos desta transição em
“Deformação e Orogénese”
Tensões máxima (σ1) e mínima (σ3)
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Nos escudos pré-câmbricos, relativamente frios, a transição frágil-dúctil ocorre a uma profundidade superior a cerca de 30 km.
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A base reológica da litosfera, correspondente ao valor estipulado de cerca de 1MPa = log(σ1-σ3) de resistência à rotura, ocorre a 55 km nas zonas de rifte e a 115 km nas zonas dos escudos pré-câmbricos.
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Introduction
Zonation of the Upper Earth –Rheology VERTICAL MOTIONS (subsidence, uplift)
in sedimentary basins are primarily in response to deformation of lithosphere and asthenosphere
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Introduction
Plate motions Plate-plate interactions can generate vertical crustal movements We will examine basins according to their positions with respect to plate boundaries and plate-plate interactions “Wilson Cycle” – opening and closing of ocean basins (See revision presentation)
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Introduction
Three types of plate boundaries: Divergent – plates moving apart Mid- ocean
ridges, rifts
Convergent – plates moving towards each
other Subduction zones
Conservative – plates move parallel to each
other Strike-slip systems
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Mechanisms of Basin Formation Como se formam as bacias?
Major mechanisms for regional subsidence(subsidência)/uplift(soerguimento): Isostatic – changes in crustal or lithospheric thickness Loading (sobrecarga) – by thrust sheets, volcanic piles, sediment Dynamic effects – asthenospheric flow, mantle convection, plumes
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Mechanisms of Basin Formation
Isostatic Processes: Crustal thinning
Extensional stretching, erosion during
uplift, magmatic withdrawal
Mantle-Lithosphere Thickening
Cooling of lithosphere, following cessation
of stretching or cessation of heating
Pesquisar ISOSTASIA
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Mechanisms of Basin Formation
Isostatic Processes: Crustal densification Density increase due to changing pressure/temperature conditions and/or emplacement of higher density melts into lower density crust
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Mechanisms of Basin Formation
Loading (sobrecarga):
• Local isostatic compensation of crust and regional lithospheric flexure • Dependent on flexural rigidity of lithosphere
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Mechanisms of Basin Formation
Loading: Sedimentary or Volcanic Loading Tectonic loading During overthrusting and/or underpulling
Subcrustal loading Lithospheric flexure during underthrusting of dense lithosphere
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Mechanisms of Basin Formation
Dynamic effects: Asthenospheric flow
Descent or delamination of subducted
lithosphere
Mantle convection Plumes
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