Parnaíba Basin
The Parnaíba Basin (Portuguese: Bacia do Parnaíba) is a large cratonic sedimentary basin located in the North and Northeast portion of Brazil. About 50% of its areal distribution occurs in the state of Maranhão, and the other 50% occurring in the state of Pará, Piauí, Tocantins, and Ceará. It is one of the largest Paleozoic basins in the South American Platform. The basin has a roughly ellipsoidal shape, occupies over 600,000 km2, and is composed of ~3.4 km of mainly Paleozoic sedimentary rock that overlies localized rifts.[1]
| Parnaíba Basin | |
|---|---|
Map view of the Parnaíba Basin in Brazil | |
| Coordinates | 06°28′00″S 45°35′00″W / 6.46667°S 45.58333°W |
| Region | North Region, Brazil, Northeast Region, Brazil |
| Country | Brazil |
| State(s) | Pará, Maranhão, Piauí, Ceará, Tocantins |
| Cities | Teresina, Palmas, Araguaína, Parnaíba |
| Characteristics | |
| On/Offshore | Onshore |
| Boundaries | São Luís Craton (N), São Francisco Craton (SE), Borboremo Province (E), Amazonian Craton (W) |
| Part of | Brazilian onshore basins |
| Area | 665,888 km2 (257,101 sq mi) |
| Hydrology | |
| River(s) | Parnaiba River, Tocantins River |
| Geology | |
| Basin type | Cratonic basin |
| Plate | South American |
| Orogeny | Brasiliano orogeny |
| Age | Paleozoic to recent |
| Stratigraphy | Stratigraphy |
| Field(s) | Gavião Real field, Gavião Branoc field, Gavião Vermelho field, Gavião Caboclo field, and the Gavião Azul field |
The basin as named after the Parnaíba River, which is approximately 1,400 km (870 mi) long, and runs relatively parallel to the major axis of the basin.
Regional Setting edit
It is located between the Amazonian Craton to the west and the São Francisco Craton to the south east. The São Luís Craton sits north of the basin and the Borborema Province is the east. The basin currently covers a Precambrian basement composed of Archean–Early Proterozoic cratonic blocks, Late Proterozoic Brasiliano/Pan-African fold belts and basement inliers.[2]
The existence of a Parnaíba block was hypothesized from geophysical evidence, petrography, geochronology of the basement rocks,[3] and from collisional tectonic models.[4][5][6]
It was regarded as one of the continental fragments inherited by the South American platform after the dispersal of the Rodinia supercontinent to form the Gondwana supercontinent.[8] The São Francisco Craton and São Luis Craton existed before the opening of the Atlantic Ocean in Mesozoic times, were part of larger cratonic landmasses, and probably surrounded a central Parnaíba block presently concealed under the basin's sediments.[9] To the west, the Araguaia suture zone represents the final Neoproterozoic collision between the Amazonian craton and the Parnaíba block and, to the east, the Transbrasiliano Lineament marks the border with the Borborema Province.[8][10]
Depositional History edit
Stratigraphy of the Parnaíba basin contains depositional sequences, varying in age from Silurian to Cretaceous, marked by a progressive change in depositional environment from marine to continental.[11] Like many other cratonic basins, the Parnaíba Basin displays a polyphase sedimentary history.[12] There are five distinct and recognizable tectonostratigraphic (TS) units that are separated by basin-wide unconformities that make up the area. These TS units include: the Riachão unit (TS-1), the Jaibaras unit (TS-2), the Parnaíba unit (TS-3), the Mearim unit (TS-4), and the Grajau unit (TS-5). The sedimentary rocks vary greatly throughout the stratigraphy of the basin and depsostional enciroment changes, and includes shale, siltstone, mudstone, sandstone, conglomerate, breccia, limestone, and more. Two magmatic pulses can be seen in the rock record, and are known as the Mosquito Formation and the Sardinha Formation. Most of the magmatic rocks are sub-alkaline tholeiitic basalts, and occur as dykes and sills mainly within the Silurian to Carboniferous and as magmatic flows in the Jurassic and, less commonly, in the Cretaceous[13]
Grajau Unit (TS-5) edit
- Cretaceous (deposition between ~120 and 95 million years ago)
- Comprises the Corda, Grajau, Codo, and Itapecuru Formations
- Deposition of near-shore, shallow marine, and fluviolacustrine clastic sediments has been attributed to subsidence associated with early opening of the South Atlantic[14]
Sardinha Formation edit
- Middle Cretaceous (emergence between ~130 and 125 million years ago)
- Occur mainly as diabase dykes and sills and as minor basaltic flows with higher alkali content when compared to the other magmatic pulse in the basin, the Mosquito Formation[13]
- Interpreted as a second phase of basaltic magmatism manifesting itself as extensive sills interlocking basin strata that is attributed to the early opening of the South Atlantic Ocean[12]
Mearim Unit (TS-4) edit
- Late Jurassic (deposition between ~165 and 155 million years ago)
- Comprises the Pastos Bons Formation
- Deposition of sandstone in a sabkha environment that is restricted to the center of the basin and undergoes of central "sag"[15][16]
Mosquito Formation edit
- Early Jurassic (emergence between ~205 and 185 million years ago)
- Formed mainly by lava flows that are occasionally interbedded with sandstones with lower alkali content when compared to the other magmatic pulse in the basin, the Sardinha Formation[13]
- Interpreted as a phase of extrusive volcanism with the deposition of basaltic lava flows[15][17] resulting from the Central Atlantic magmatic province and the opening of the central Atlantic Ocean[18]
Parnaíba Unit (TS-3) edit
- Late Ordovician/Silurian to Early Triassic (deposition between ~445 and 220 million years ago)
- Interpreted as the product of basinal "sag" or cratonic basin subsidence
- Consists of three megasequences, separated by regional unconformities and comprising shallow marine, fluviolacustrine, and terrestrial siliciclastic sediments[12]
Balsas megasequence
- Late Carboniferous to Middle Triassic (deposition between ~310 and 220 million years ago)
- Comprises the Piaui, Pedra de fogo, Motuca, and Sambaiba Formations
- Consists of clastic sandstone and evaporites deposited in subaerial environments[15]
Caninde megaseqeuence
- Lower Devonian to Carboniferous (deposition between ~400 and 330 million years ago)
- Comprises the Itaim, Pimenteiras, Cabecas, Longa, and Poti Formations
- Consists of interbedded shallow marine and deltaic depositional environments[12]
Serra Grande megasequence
- Early Silurian to Lower Devonian (deposition between ~440 and 405 million years ago)
- Comprises the Ipu, Tiangua, and Jaicos Formations
- Consists of quartz arenites of fluvioglacial, glacial marine, and shallow marine sediments that account for a complete transgressive/regressive cycle[12]
Jaibaras Unit (TS-2) edit
- Cambrian (deposition between ~530 and 485 million years ago)
- Comprises the Jaibras Group, which is the Massapé, Pacujá, Parapuí and Aprazível Formations[19]
- Interpreted as a rift infill resulting from a prevalent Cambro-Ordovician rifting event[20] or pull-apart infill resulting from dextral strike-slip motion on the Transbrasiliano shear zone during the Cambrian/Early Ordovician[12]
Riachão Unit (TS-1) edit
- Late Neoproterozoic to Cambrian (deposition between ~570 and 515 million years ago)
- Comprises the Riachão Package, which is Riachão I, II and III Sequences
- Interpreted as a Neoproterozoic rift,[7][21] or a remnant foreland basin, bounded by thick skinned thrust faults of Cambro-Ordovician age[22]
Tectonic Evolution edit
The Parnaíba basin is located above a complex basement comprising several Archaean and Proterozoic terranes that stabilized during the Brasiliano orogeny.[12] Seismic reflection data reveal a remnant basin beneath the major pre-Silurian unconformity and the base of the sediments of the Parnaíba cratonic basin. This pre-Silurian basin, known as the Riachão basin, covers an area of at least 35,000 km2 along a north–south trend.[11] The remnant basin is thought to have originated as a foreland basin, and is poorly constrained between 574 and 500 million years ago.[11]
The Riachão basin edit
The Riachão basin has sedimentation that reaches a thickness of 4 km at its maximum, and is composed of three seismostratigraphic sequences (Riachão I, II and III). These sequences are defined by onlaps and erosive unconformities.
The Riachão III sequence is a wedge-shaped package of low amplitude continuous reflectors that onlap the top of the Riachão II sequence to the west. These clastic sediments were deposited in the second foreland phase to the east.[11]
The Riachão II sequence is a wedge-shaped package of very low amplitude discontinuous reflectors that onlap the top of the Riachão I sequence to the east. These sediments were deposited in the first foreland phase, centered in the west.[11]
The Riachão I sequence is a thin, banded package of high-amplitude reflections that extend across most of the basin area and define a broad arch. This is interpreted as a carbonate marine platform sequence that took place before any foreland subsidence or clastic sediment input.[11]
The Phanerozic Parnaíba basin sits on top of the remnant Riachão basin sequences, and shows no signs of deformation from thrust faulting. An intense erosional event took place after the deposition of the Riachão basin sequences that ultimately created a profound pre-Silurian unconformity. The subsidence and deposition of the Parnaíba basin sediments occurred after this event and have little to do with the previous development and deformation of the Riachão basin.[11]
Modern Parnaíba basin edit
The current Parnaíba basin has maximum thickness of 3.5 km in its center,[11] covers a Precambrian basin composed of Archean-Early Proterozoic cratonic blocks,[2] consists of phanerozoic sediment, and is termed a cratonic sag basin. Low to moderate thermal subsidence caused the tectonostratigraphic units to become increasingly thicker in the central portion of the basin, which produces a saucer shape typical of cratonic sag basins.[2] Tectonic subsidence curves through the Parnaíba Unit, done by backstripping data from 21 different wells, show an exponentially decreasing subsidence profile over 300 million years.[23] Thermal time constraints of this subsidence range from 70 to 90 million years ago.[23] The underlying subsidence appears largely continuous throughout the basin's history, there are minor deviations associated with regional disconformities. These variations in subsidence can be interpreted as brief uplift events from epeirogenic movement caused by changing patterns of dynamic topography.[24]
References edit
- ^ Daly, Michael C.; Andrade, Vander; Barousse, Chuck A.; Costa, Rafaela; McDowell, Kenneth; Piggott, Neil; Poole, Alan J. (2014). "Brasiliano crustal structure and the tectonic setting of the Parnaíba basin of NE Brazil: Results of a deep seismic reflection profile". Tectonics. 33 (11): 2102–2120. doi:10.1002/2014TC003632 ISSN 1944-9194
- ^ a b c d de Castro, D.L., Oliveira, D.C. & Hollanda, M.H.B.M. Geostatistical Interplay Between Geophysical and Geochemical Data: Mapping Litho-Structural Assemblages of Mesozoic Igneous Activities in the Parnaíba Basin (NE Brazil). Surv Geophys 39, 683–713 (2018). doi:10.1007/s10712-018-9463-5
- ^ CordaniI, U.G., Brito Neves, B.B., Fuck, R.A., Porto, R., Thomaz Filho, A. & Cunha, F.M.B. 1984. Estudo preliminar de integração do Pré-Cambriano com os eventos tectônicos das bacias sedimentares brasileiras. Paper presented at Ciência Técnica Petróleo, Seção Exploração de Petróleo. Petrobras, Rio de Janeiro, Brazil, internal report.
- ^ Brito Neves, B.B., Fuck, R.A., Cordani, U.G. & Thomas, A. 1984. Influence of basement structures on the evolution of the major sedimentary basins of Brazil: a case of tectonic heritage. Journal of Geodynamics, 1, 495–510.
- ^ Nunes, K.C. 1993. Interpretação integrada da Bacia do Parnaíba com ênfase nos dados aeromagnéticos. Proceedings of the 3rd International Congress of the Brazilian Geophysical Society, 1, 152–157, Rio de Janeiro, Brazil.
- ^ Klein, E.L., Luzardo, R., Moura, C.A.V. & Armstrong, R. 2008. Geochemistry and zircon geochronology of Paleoproterozoic granitoids: further evidence on the magmatic and crustal evolution of the São Luís cratonic fragment, Brazil. Precambrian Research, 165, 221–242
- ^ a b de Castro, D. L., Bezerra, F. H., Fuck, R. A., & Vidotti, R. M. (2016). Geophysical evidence of pre-sag rifting and post-rifting fault reactivation in the Parnaíba basin, Brazil. Solid Earth, 7(2), 529-548.
- ^ a b Reinhardt A. Fuck, Benjamim Bley Brito Neves, Carlos Schobbenhaus, Rodinia descendants in South America, Precambrian Research, Volume 160, Issues 1–2, 2008, Pages 108-126, ISSN 0301-9268, doi:10.1016/j.precamres.2007.04.018.
- ^ Coelho, D. L., Julià, J., Rodríguez-Tribaldos, V., & White, N. (2018). Deep crustal architecture of the Parnaíba basin of NE Brazil from receiver function analysis: implications for basin subsidence. Geological Society, London, Special Publications, 472(1), 83-100.
- ^ Brito Neves, B.B. & Fuck, R.A. 2013. Neoproterozoic evolution of the basement of the South American Platform. Journal of South American Earth Sciences, 47, 72–89
- ^ a b c d e f g h i Porto, A., Daly, M. C., La Terra, E., & Fontes, S. (2018). The pre-Silurian Riachão basin: a new perspective on the basement of the Parnaíba basin, NE Brazil. Geological Society, London, Special Publications, 472(1), 127-145.
- ^ a b c d e f g Tozer, B., A. B. Watts, and M. C. Daly (2017), Crustal structure, gravity anomalies, and subsidence history of the Parnaíba cratonic basin, Northeast Brazil, J. Geophys. Res. Solid Earth, 122, 5591–5621, doi:10.1002/2017JB014348
- ^ a b c Oliveira, A. L. (2017). Geologia e Petrologia dos basaltos das formações Mosquito e Sardinha, Bacia do Parnaíba.
- ^ Rossetti, D. F., J. D. S. Paz, and A. M. Góes (2004), Facies analysis of the Codó formation (late Aptian) in the Grajaú area, southern São Luís-Grajaú Basin, An. Acad. Bras. Cienc., 76, 791–806, doi:10.1590/S0001-37652004000400012
- ^ a b c d Góes, A. M. O., W. A. S. Travassos, and K. C. Nunes (1993), Projeto Parnaiba: Reavaliacao e perspectivas exploratorias, paper presented at Relatorio Petrobras, DEXNOR-DINTER.
- ^ Araujo, R. N., A. C. R. Nogueira, J. Bandeira, and R. S. Angelica (2016), Shallow lacustrine system of the Permian Pedra de Fogo Formation, western Gondwana, Parnaíba Basin, Brazil, J. S. Am. Earth Sci., 67, 57–70, doi:10.1016/j.jsames.2016.01.009
- ^ Merle, R., A. Marzoli, H. Bertrand, L. Reisberg, C. Verati, C. Zimmermann, M. Chiaradia, G. Bellieni, and M. Ernesto (2011), 40Ar/39Ar ages and Sr-Nd-Pb-Os geochemistry of CAMP tholeiites from western Maranhão basin (NE Brazil), Lithos, 122, 137–151, doi:10.1016/ j.lithos.2010.12.010.
- ^ Baksi, A. K., and D. A. Archibald (1997), Mesozoic igneous activity in the Maranhao province, northern Brazil: 40Ar/39Ar evidence for separate episodes of basaltic magmatism, Earth Planet. Sci. Lett., 15, 139–153.
- ^ Pedrosa Jr, N. C., Vidotti, R. M., Fuck, R. A., Oliveira, K. M. L., & Branco, R. M. G. C. (2015). Structural framework of the Jaibaras Rift, Brazil, based on geophysical data. Journal of South American Earth Sciences, 58, 318-334.
- ^ de Oliveira, D. C., and W. U. Mohriak (2003), Jaibaras trough: An important element in the early tectonic evolution of the Parnaíba interior sag basin, Northern Brazil, Mar. Pet. Geol., 20, 351–383.
- ^ de Castro, D. L., Fuck, R. A., Phillips, J. D., Vidotti, R. M., Bezerra, F. H., & Dantas, E. L. (2014). Crustal structure beneath the Paleozoic Parnaíba Basin revealed by airborne gravity and magnetic data, Brazil. Tectonophysics, 614, 128-145.
- ^ Porto, A. L., M. C. Daly, and S. L. Fontes (2016), The pre-Silurian Riachao basin, a new perspective into basement configuration of the cratonic Parnaíba Basin, NE Brazil, paper presented at 48th Congresso Brasileiro de Geologia, Sociedade Brasileira de Geologia, Porto Alegre.
- ^ a b Tribaldos, V. R., & White, N. (2018). Implications of preliminary subsidence analyses for the Parnaíba cratonic basin. Geological Society, London, Special Publications, 472(1), 147-156.
- ^ Daly, M. C., Fuck, R. A., Julià, J., Macdonald, D. I., & Watts, A. B. (2018). Cratonic basin formation: a case study of the Parnaíba Basin of Brazil. Geological Society, London, Special Publications, 472(1), 1-15.