Basin Analysis Análise de Bacias Part 2 Basin Classification Basins and Sequence Stratigraphy Summary Basin Analysis • Introduction • Mechanisms of Basin Formation • Basin Classification • Basins and Sequence Stratigraphy • Summary Basin Classification Many different classification systems have been proposed (3 parâmetros mais usados para classsificar as bacias): Principal factors 1. Position of the basin in relation to plate margins 2. Crustal/lithospheric substratum Oceanic, continental crust 3. Type of plate boundary Basin Classification Ingersoll and Busby (1995): 26 different types of basin Divided into various settings • Divergent • Intraplate • Convergent • Transform • Hybrid 1983 Basin Classification Alternate approach (Allen and Allen, 2005): focus on basin- forming processes What causes subsidence? Basin Classification This course – hybrid approach: What causes subsidence? What is tectonic setting? We do not have time to cover all types of basins Focus on selected basin types Basin Classification Basins can be related to tectonic setting • Position with respect to plate boundary • Nature of plate boundary “Wilson Cycle” Basin Classification Divergent Plate Boundaries Divergent Plate Boundaries Continental rifting (a) may lead to opening of an ocean with a mid-ocean ridge (b, c) Rift basin evolves into passive margin Basin Classification Rift Basins • Elongate, valleys bounded by normal faults Few km -> 10s of km wide Length – up to 1000s of km • Occur in many plate settings, but most common in divergent settings RIFTES CONTINENTAIS Os riftes continentais são vales definidos por falhas tectónicas com larguras entre 30 a 75 km e comprimento variável, desde as dezenas até às centenas de quilómetros. Mostram-se aqui quatro exemplos de sistemas de rifte recentes. Vale do rifte na parte leste do Nevada no Parque Nacional da Great Basin – vista do Wheeler Peak A Província Basin and Range do Nevada prolonga-se desde Wasatch no Utah até à Sierra Nevada na Caifórnia Os riftes têm pequena espessura crustal (20-30 km) À medida que o rifte vai abrindo a crusta inferior sofre adelgaçamento CRATÃO RIFTE CONTINENTAL O adelgaçamento da crusta durante a formação do rifte deve-se principalmente ao adelgaçamento dúctil das camadas crustais média e inferior Riftes Continentais Riftes Continentais Riftes Continentais Riftes Continentais Basin Classification Rift Basins Seismic studies indicate rifts overlie thinned crust Evidence for thermal anomalies at depth: Negative Bouguer gravity anomalies High heat flow Bimodal volcanic activity À medida que a Terra arrefece, o calor é transferido por convexão do interior do manto para a litosfera, sendo depois conduzido através da litosfera para a superfície. O fluxo de calor que se observa à superfície da Terra pode ser estimado com base na medição do gradiente térmico e na condutividade das rochas. Nas áreas oceânicas, o fluxo de calor (q0) diminui e a profundidade aumenta (d) com a idade (t) da litosfera - ver expressões indicadas acima Basin Classification Rift Basins Active rifting: Mantle upwelling causes crustal thinning (heating) Thinning leads to uplift Uplift leads to tension and rifting Passive rifting: Regional extension causes failure Hot mantle rocks rise and penetrate lithosphere Passive Rifting – regional extension causes rifting, upwelling of hot mantle follows. Example: Rio Grande Active Rifting – Upwelling of hot mantle leads to uplift and extension. Example: East African Rift Como a crosta inferior e a litosfera apresentam comportamento dúctil com a deformação, a área de ascensão astenosférica é maior que a de distensão crustal. Assim, a subsidência termal (sag basin) afeta uma área maior que a subsidência mecânica por ela responsável. Basin Classification Rift Basins Rift fill commonly consists of “continental” deposits Fluvial, lacustrine, alluvial fans Evaporites may form if rift valley/basin is located in a hot, dry area Invasion of the sea Closed drainage basins Volcanic rocks, and associated intrusions, may be present Early Mesozoic Evaporites Evaporites accumulated in shallow basins • As Pangaea broke apart during the Early Mesozoic • Water from the Tethys Sea flowed into the Central Atlantic Ocean Basin Classification Continued rifting can lead to formation of oceanic crust – opening of ocean basin E.g., Red Sea “Rift-Drift” transition Rift-drift transition may be marked by a “breakup unconformity” If rift associated with subaerial relief at onset of drifting Basin Classification Passive Margins Basin Classification Passive Margins • Strongly attenuated continental crust • Stretched over distances of 50-500 km • Overlain by seaward-thickening sediment prisms Typically shallow-marine deposits • Sometimes referred to as “Atlantic- type margins” or “continental rises and terraces” (Boggs) Basin Classification Scotian Shelf Beaumont et al. 1992 – cited in Allen and Allen 2005 Basin Classification Passive Margins Various subsidence mechanisms: Cooling (thermal contraction) following lithospheric thinning [Main mechanism] Phase changes in lower crust/mantle (gabbro to eclogite) Not known if this process can be widespread enough Sediment loading Adds to other effects Basin Classification Passive Margins Subsidence variable in space and time Subsidence rate increases in offshore direction Subsidence rate decreases with time for all parts of the profile Basin Classification Basin Classification Basin Classification Passive Margins Morphology characterized by shelf, slope and continental rise Shelf margin builds out with time Shelf sediments can be clastic or carbonate Water depth stays relatively constant on shelf Abundant sediment supply Basin Classification Passive Margins Slope/rise – material shed from continental shelf during lowstands (clastic systems) Aprons/fans deposited along slope/rise Also pelagic sediments, contourites, etc. Basin Classification Gravity-driven deformation common in drift-phase sediments Listric growth faults, salt tectonics, mud diapirs, etc. Basin Classification Basin Classification Basin Classification Basin Classification Aulacogens •“Failed rifts” •Occur at high angle to continental margin •Fill: non-marine to deep marine Example: Reelfoot Rift (Mississippi valley) Basin Classification Convergent Plate Boundaries Subduction of oceanic plate(d) may lead to closing of ocean basin (e) and ultimately to continental collision (f) Basin Classification Convergent Plate Boundaries Age of oceanic crust affects angle at which it is subducted Young crust (top) – shallow angle subduction, compression behind arc Old crust (bottom) – steep angle subduction, “rollback”, extension behind arc Basin Classification BACIAS ANTE-ARCO FOREARC BASIN Arcos vulcânicos oceânicos Arcos vulcânicos de margem continental BACIA PÓS-ARCO BACK-ARC BASIN ARCO REMANESCENTE Bacia pós-arco Continental Foreland Basin Sedimentação e estruturas cavalgantes Basin Classification Arc-related basins • Forearc and backarc basins dominated by sediment derived from arc Immature clastics Backarc basin may also have component derived from continent • Deep-sea trench has sediments derived from arc and sediments scraped off subducting oceanic crust “Melange” FOSSAS PRISMAS DE ACREÇÃO Basin Classification foreland promontório A natural elevation (especially a rocky one that juts out into the sea) Basin Classification Foreland basins (Bacias de antepaís) • Crustal loading of thrust sheets causes subsidence • May face towards or away from continental interior • Ocean-continent or continent-continent collision • Rate of subsidence greatest adjacent to thrust loading Basin Classification Carreamento(Thrust) Falha geológica inversa muito pouco inclinada, que resulta de um campo de tensões compressivo. Normalmente tem uma grande amplitude (pode ser quilométrica), com grande quantidade de transporte. Basin Classification Basin Classification Underthrusting of continental crust and Compressive shortening and lithosfere, which buoyanty elevates the plateau thickening of both the crust and the lithosfere, folloed by isostatic rebound to form the plateau Basin Classification Basin Classification Depth to basement(km; outcrop=0) Turcotte and Schubert, 1982 Basin Classification Basin Classification Basin Classification Basin Classification Foreland basins Generally clastic – high sediment input from adjacent uplifts “Clastic wedges” Date thrusting Carbonates in some settings Marine or non-marine fill Turbidites, pelagic, deltaic, shoreface/shelf, fluvial Basin Classification Foreland basins Basin fill adjacent to thrusting typically gets caught up in deformation Basin Classification Basin Classification Bacias intracratónicas Riftes Continentais Riftes Continentais Riftes Continentais Riftes Continentais Basin Classification Intracratonic Basins “Interior Basins” Semi-circular to ovate downwarps Within continental interiors Otherwise stable cratonic areas Away from plate boundaries Basin Classification Intracratonic Basins Causes of subsidence •Underlying rifts, large-scale fault blocks •Cooling after intrusion of dense material •Mantle “cold” spots (downwelling) •Phase changes Subsidence greatest towards center of basin Basin Classification Subsidência e levantamento Basin Classification Basin Classification Intracratonic Basins Sedimentary fill terrestrial or marine Carbonates, clastics, evaporites Basin Classification Other basins, e.g. basis associated with wrench faulting, not discussed here (time constaints) Some basins have had multiple-phase history •Sometimes related to reactivation because