Placas das zonas convergentes
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Transcript of Placas das zonas convergentes
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Limites ConvergentesLimites Convergentes
Três tipos:
oceano–oceanoPhilippines
oceano–continente Andes
continente–continente Himalaya
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Limites ConvergentesLimites Convergentes• Nova crosta criada no MOR—antiga
crosta destruida (reciclada) em zonas de subducção
• 2 tipos : subducção & colissãosubducção & colissão• Importância Relativa da densidade :
Crosta continental ≈ 2.8 g/cm3
Crosta oceânica ≈ 3.2 g/cm3
asthenosfera ≈ 3.3 g/cm3
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Oceano–OceanoOceano–OceanoArcos de Ihas Arcos de Ihas : Cadeia de ilhas
vulcânicas
• Cinturão de alta sismicidade de terremotos rasos a profundos
• Alto fluxo de calor em arcos de vulcões andesiticos
• Borderjados por uma trincheira submarine
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Zonas de subducção
• Terremotos rasos e profundos, dispostos em uma superfície
• Vulcanismo e plutonismo
• Destruição da crosta oceânica
• Formação da crosta continental – deformação e metamorfismo
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Duas placas se movem uma em direção a outra :
1. Duas placas oceânicas
2. Uma placa continental plate e outra oceânica
3. Duas placas continentais
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• Quando duas placas colidem, a mais densa DESCE (mergulha) em direção ao manto
• Este processo é chamado SUBDUCÇÃO
• Como a placa mais densa mergula, são criados focos de terremos rasos, intermédiarios e profundos
• Este padrão de terremotos definem a ZONA de BENIOFF ZONE
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• Quando uma placa oceânica colide com outra placa oceânica, a mais ANTIGA subducta
• O topo da placa subductante forma um TRINCHEIRA no oceano profundo.
• Sedimentos da placa subductante é jogado para for a para formar um prisma acrecionário
Convergência Oceano-oceano
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• Água liberada da placa subductante causa a fusão da astenosfera
• Este magma move-se para cima para formar um ARCO DE ILHAS VULCÂNICO
• Parte do oceano entre o arco de ilha vulcânico e o prisma acrescionário é chamado de bacia de FOREARC (pós-arco)
• O oceano atrás do arco de ilhas é chamado de bacia de retro-arco (BACKARC )
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• Quando a placa oceânica colide com uma placa continental, a placa oceânica mais densa subducta
• Zone de Benioff zone, trincheira, prisma acrescionário e vulcões são formados devido a subducção.
• A jovem CINTURÃO DE MONTANHAS se forma na placa continental e
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• Duas placas continentais colidem quando o oceano inteiro entra em subducção.
• Placa Continental NÃO PODE subductar
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SEM subducção:
NÃO zona de Benioff
NÃO trincheira oceânica
NÃO prisma acrescionário
NÃO vulcões ativos
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• As placas continentais se juntam ao longo de uma ZONA DE SUTURA
• A crosta continental torna-se espessada e forma um CINTURÂO DE MONTANHAS (example: The Himalayas)
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Zona de Subducção Oceano–Oceano
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Oceano–ContinenteOceano–ContinenteArco Continental Arco Continental :
• Cinturão Magmatico de vulcões ativos (andesitos a riolitos)
• Frequentemente acompanhado de compressão de crosta superior na construção de montanhas
Bordejados por trincheira submarina
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Zona de Subducção Oceano-Continente
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Limites convergentes: zonas de subducción
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La zona de acoplamiento sísmico
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Figure 6. Uplift measured across central Vancouver Island compared with predictions from a simple elastic dislocation model of a locked fault. Curves for several fault geometries are given; parameters are fault dip, and widths of the locked zone and a transition zone where inter-seismic slip varies from zero to the full plate rate (derived from Hyndman and Wang, 1995; curves from model of Thatcher and Rundle, 1984).
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Zonas de subducción “frias” y “calientes”
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Caracteres geoquímicos del volcanismo de subducción
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Margenes accrecionales y no acrecionales
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Adakitas y fusión de la placa
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Geometría de la zona de subducción del Pacifico occidental: Kamtchatka, Japón, Izu-Bonin
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Cuencas trasarco: Zona de subducción Izu-Bonin
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Zona de subducción Izu-Bonin
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Estructura de la zona de subducción del Pacifico occidental: Tonga-Kermadec
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Sismicidad de la zona de subducción centroamericana
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Sismicidad estructura térmica de la zona de subducción en México central (Manea et al., 2004, Geophysical Journal International)
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Tomografía de ondas P en Centroamérica
(Rogers, Karason & Van der Hilst, 2002, Geology)
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Sismicidad de la zona de subducción de la placa Juan de Fuca
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Continente–ContinenteContinente–Continente• Limites Continente–continente,
convergência é acompanhada de :• Dobramento (encurtamento
“shortening” e espessamento “thickening”)
• falhamento transcorrente “Strike-slip
faulting”
• Empurrões reversos “Underthrusting” (subducção intracontinental)
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Continente–Continente
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Colissão Continente-Continente
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Himalayas and Tibetan PlateauHimalayas and Tibetan Plateau
• Produto da colisão entre India e Asia.
• Colissão iniciou-se a 45 M yr., continua hoje.
• Antes da colisão, sudeste da Asia parecia como o Andes de hoje.
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Estagios na
colissão da
India com Asia
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Limite Transformante recobrimento de centros de expansão
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Razões de movimento de placasRazões de movimento de placas
Maioria obtida de anomalias magnéticas no fundo oceânico
Espalhamento lento Espalhamento lento 3 cm/ano
Espalhamento rápido Espalhamento rápido : 10 cm/ano
Espalhamento muito rápido Espalhamento muito rápido : 17cm/ano
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Velocidade Relativa e Direção do movimento da placa
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Assembleia de Rochas Assembleia de Rochas
e placas tectônicase placas tectônicas• Cada ambiente na placa tectônica
porduz um distinto grupo de rochas.
• Para estudar o registro de rochas na área, pode-se estudar a história tectônica de uma região.
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Camadas de suite de ofiolitos
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Precambrian Ophiolite Suite
Pillow basalt
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Terrenos Exóticos ou Microplacas
• Grandes blocos cuja forma contrasta com áreas vizinhas
• Diferentes tipos de falhas, dobras, fosseis, tipo de rochas, metamorfismo, magnatismo
• Devem representar fragmentos de continentes, fundo oceânico, platôs oceânicos, arcos de ilhas que se separaram e foram agrupados em um novo lugar
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Aproximação de Arco ou Microcontinente
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Colissão
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Terreno e microplaca Accrescido
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Terrenos de Microplacas
adicionados ao Oeste da America
nos últimos 200 Milhões de anos
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Mecanismos de forças
de placas tectonicas• Pode ser a convecção do manto.
• Fricção na base da litosfera e transferência de energia da astenosfera para a litosfera.
• Convecção pode remover a astenosfera 4–6 vezes.
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Outros fatores
• Empurrão da Trincheira
Descida da Placa
• Abertura da cadeia
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Three possible driving factors
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Three possible
mechanisms for the
movement of lithosphere
over the asthenospher
e
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Reconstruções TectônicasReconstruções Tectônicas A variedade de evidências traça o
movimento dos continentes no decorrer do tempo :
• Paleomagnetismo
• Estruturas Deformacionais Ambientes de deposição
• Fosseis
• Distribuição de vulcões
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Assembleia of Pangaea
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(Breakup) Quebra do Pangaea
200 million years ago
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Breakup of Pangaea
140 million years ago
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Breakup of Pangaea
65 million years ago
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Breakup of Pangaea
Today
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Examinando Furos de mar profundo
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Questões sobre placas tectônicas
• O que realmente sabemos sobre as células de convecção do manto?
• Por que existem alguns continentes completamente circundados por centos de espalhamento?
• Por que tectônica na crosta continental crust e oceânica são tão diferentes?
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Cross Section of Western Canada
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Formação de
anomalias Magnéticas
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HimalayasHimalayas and Tibetan Plateau and Tibetan Plateau
Modelos
• Underthrusting
• Encurtamento Distribuido
•Falhamento Strike-slip
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Ciclo de WilsonCiclo de WilsonPlate tectonics repeats itself: rifting, sea-
floor spreading, subduction, collision,
rifting, …
Plate tectonics (or something like it)
seems to have been active since the
beginning of Earth’s history.
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After Hutchinson, 1992-1993
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Examples of Plate Boundaries
O-Oconvergent
O-Odivergent
O-Cconvergent
O-Cconvergent
O-Odivergent
C-Cdivergent
O-Odivergent
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Sedimentos Vulcânicos e Não-marinhos são depositados em rift
valleys
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Resfriamento e subsidência da margem do rift segue a
deposição de sedimentos
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Desenvolvimento de plataforma de Carbonatos
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Margem Continental continua a crescer suprida por erosão do continente
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Limites Oceano–Continente
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Opening of the
Atlantic by Plate Motion
After Phillips & Forsyth, 1972
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Partes de um limite de placa convergente Oceano–Oceano
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Partes de um limite Oceano–Continente
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Subducção Continuada
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Colissão Continente– Continente
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