| Santos Basin | |
| Other Name: | Bacia de Santos |
| Named For: | Santos |
| Pushpin Map: | Brazil |
| Pushpin Relief: | 1 |
| Coordinates: | -26.1061°N -43.7292°W |
| Location: | South America |
| Region: | Southeast, South |
| State: | Rio de Janeiro, São Paulo, Paraná, Santa Catarina |
| Cities: | Cabo Frio, Rio de Janeiro, Guarujá, Santos, Itajaí, Balneário Camboriú, Florianópolis |
| Onoffshore: | Both, mostly offshore |
| Boundaries: | Cabo Frio, Florianópolis Highs, Serra do Mar |
| Partof: | Brazilian Atlantic margin basins |
| Seas: | South Atlantic Ocean |
| Rivers: | Ribeira de Iguape |
| Area: | ~352000km2 |
| Basin Type: | Passive margin on rift basin |
| Plate: | South American |
| Orogeny: | Break-up of Gondwana |
| Age: | Barremian-recent |
| Stratigraphy: | Stratigraphy |
| Fields: | Tupi, Libra, Júpiter, others |
The Santos Basin (Portuguese: Bacia de Santos) is an approximately 352000km2 large mostly offshore sedimentary basin. It is located in the south Atlantic Ocean, some southeast of Santos, Brazil. The basin is one of the Brazilian basins to have resulted from the break-up of Gondwana since the Early Cretaceous, where a sequence of rift basins formed on both sides of the South Atlantic; the Pelotas, Santos, Campos and Espírito Santo Basins in Brazil, and the Namibia, Kwanza and Congo Basins in southwestern Africa.
Santos Basin is separated from the Campos Basin to the north by the Cabo Frio High and the Pelotas Basin in the south by the Florianópolis High and the northwestern boundary onshore is formed by the Serra Do Mar coastal range. The basin is known for its thick layers of salt that have formed structures in the subsurface due to halokinesis. The basin started forming in the Early Cretaceous on top of the Congo Craton as a rift basin. The rift stage of the basin evolution combined with the arid Aptian climate of the southern latitudes resulted in the deposition of evaporites in the Late Aptian, approximately 112 million years ago. The phase of rifting was followed by a thermal sag phase and drift stage in the widening of the South Atlantic Ocean. This process led to the deposition of a more than 20km (10miles) thick succession of clastic and carbonate sediments.
One of the largest Brazilian sedimentary basins, it is the site of several recently (2007 and later) discovered giant oil and gas fields, including the first large pre-salt discovery Tupi (8 billion barrels), Júpiter (1.6 billion barrels and 17 tcf of gas), and Libra, with an estimated 8 to 12 billion barrels of recoverable oil. Main source rocks are the lacustrine shales and carbonates of the pre-salt Guaratiba Group and the marine shales of the post-salt Itajaí-Açu Formation. Reservoir rocks are formed by the pre-salt Guaratiba sandstones, limestones and microbialites, the Albian limestones of the Guarujá Formation and the Late Cretaceous to Paleogene turbiditic sandstones of the Itanhaém, Juréia, Itajaí-Açu, Florianópolis and Marambaia Formations. The mobile salt of the Ariri Formation forms regional seals, as well as the shales of the post-salt sedimentary infill. In 2014, the total production of only the sub-salt reservoirs accumulated to more than . In 2017, the Santos Basin accounted for 35% of Brazil's oil, with the northern neighbour Campos Basin at 55%.
The Santos Basin is named after the coastal city of Santos in the state of São Paulo.
The Santos Basin is a mostly offshore sedimentary basin across the Tropic of Capricorn, bordering from north to south the Brazilian states of Rio de Janeiro, Sáo Paulo, Paraná and Santa Catarina.[1] The basin covers an area of approximately 352000km2,[2] and is bounded in the north by the Cabo Frio High, separating the basin from the Campos Basin and the Florianópolis High and Fracture Zone, separating the Santos Basin from the Pelotas Basin.[3]
Along the Brazilian coast, the basin is bounded by the Serra do Mar and stretches from Cabo Frio in the northeast to Florianópolis in the southwest. The city of Rio de Janeiro is located at the coastal edge of the Santos Basin in the northern portion, Santos, Guarujá and the islands of Ilhabela in the central area and Itajaí and Balneário Camboriú in the south of the basin. Within the basin, several highs are located. The Outer High, in the distal part of the Santos Basin, is the most prominent and extensive intra-basinal high with an approximate area of 12000km2. The Outer High is likely a segmented series of rift fault-block shoulders which were uplifted and eroded during the Late Barremian.[4]
The climate of the onshore stretch of the basin ranges from tropical savanna climate (Aw), tropical monsoon climate (Am) and tropical rainforest climate (Af) to a humid subtropical climate (Cfa). The onshore portion of the Santos Basin is in the Serra do Mar coastal forests ecoregion of the Atlantic Forest biome. On the islands of the Superagüi National Park in the Santos Basin, the endemic critically endangered Superagüi lion tamarin (Leontopithecus caissara) has its restricted habitat.
The South Atlantic margin developed on Archean stable cratons consisting of hard and resistant rocks and partly on the Neoproterozoic mobile belts composed of less resistant metamorphic rocks.[5] The Precambrian basement of the Santos Basin is exposed as the Araçuaí Belt along the Brazilian coast, most notably in the inselbergs of Rio de Janeiro, of which Sugarloaf Mountain is the most iconic. The ancient rocks consist of a Neoproterozoic to Cambrian high-grade metamorphic core of granites and gneisses, formed during the collision of Gondwana in the Pan-African-Brasiliano orogeny.[6] Basalts similar to the Paraná and Etendeka traps, exposed to the west in the Paraná Basin, have been found underlying the Santos Basin.[7] The Tristan da Cunha hotspot, known as the Tristan hotspot, is considered the driver behind the formation of these flood basalts.[8]
During the Early Cretaceous, the former continent Gondwana, as southern part of Pangea, starting to break-up, resulting in a sequence of rift basins bordering the present-day South Atlantic. The Pelotas-Namibia spreading commenced in the Hauterivian, around 133 million years ago and reached the Santos Basin to the north in the Barremian. Seafloor spreading continued northwards to the Campos Basin in the Early Albian, at approximately 112 Ma.
Five tectonic stages have been identified in the Brazilian basins:[9]
The sag phase in the Santos Basin was characterised by thermal subsidence and generated restricted depocentres with relatively uniform water depths, ranging from 600mto950mm (2,000feetto3,120feetm). The Late Aptian climate was arid with high evaporation rates which triggered hypersaline conditions in these marginal sag basins. This resulted in the accumulation of thick layers of evaporites along the Brazilian and southwestern African continental margins, a process continuing towards the north later in the Cretaceous.[10] The deposition of the lowermost 600m (2,000feet) of salt in the Aptian would have taken approximately 20,000 to 30,000 years.[11] With the continental break-up of the Santos and Campos Basins from the opposite Namibia and Kwanza Basins, oceanic circulation returned during the post-rift stage. The drift phase since the Late Cretaceous produced a thick sequence of clastic and carbonate deposits. Differential thermal regimes and sediment loading of these units produced halokinesis; salt movement in the subsurface. The resulting salt diapirs, listric and thrust faults and various salt-related structures produced several stratigraphic and combined stratigraphic-structural traps for hydrocarbon accumulation in the Brazilian and southwest African offshore.[10]
During the phases of halokinesis, dated to the Albian to Paleocene, several areas of the now deep water distal part of the Santos Basin were exposed to subaerial conditions and suffered erosion. The distal parts of the basin were affected by E-W to NW-SE oriented shortening, sub-perpendicular to the Brazilian margin.[12]
The basement of the Santos Basin is composed of granites and gneisses of the Araçuarí Belt that formed at the western boundary of the Congo Craton. The erosion resistant metamorphic and magmatic rocks are exposed in the Serra do Mar, forming the edge of the Santos Basin along the Brazilian coast.
The total stratigraphic thickness of the sediments in the Santos Basin has been estimated at 23170m (76,020feet) and has been described in detail by Clemente in 2013.[13]
The Guaratiba Group is 4200m (13,800feet) thick and includes four formations, from old to young the Camboriú, Piçarras, Itapema and Barra Velha Formations. The group is equivalent to the Lagoa Feia Group of the Campos Basin.[13]
The conglomerates and sandstones of the formation are representative of an alluvial environment. The coquinas represent a shallow lacustrine environment. Similar to the Atafona Formation of the Campos Basin, the sandstones, stevensite-bearing siltstones and shales represent an alkaline lacustrine environment affected by volcanic activity. The shales represent deeper lacustrine waters in more distal areas. The alternation of the two facies implies a series of alluvial progradation-retractions into the Cretaceous carbonate lakes. The low textural and compositional maturity of conglomerates and sandstones implies the basin was supplied from areas close to the basin margins.[14]
The Ariri Formation is in the 581m (1,906feet) thick and may be up to 4000m (13,000feet) thick in other areas of the basin. It is predominantly composed of evaporites. The formation is characterized by thick intervals of white halite, associated with white anhydrite, ochre greyish calcilutites, shales and marls. The sedimentary environment probably was restricted marine including mudflat sabkhas, evolving under an arid climate. The ostracod assemblages of this formation indicate a neo-Algoas age (local time scale).[14]
The Camburi Group is up to 6100m (20,000feet) thick and includes three formations, Florianópolis, Guarujá and Itanhaém.[15]
The Frade Group is 4000m (13,000feet) thick and includes three formations: Santos, Itajaí-Açu and Juréia. They predominantly comprise turbidites.[16]
Itamambuca Group is 4200m (13,800feet) thick and includes four formations, Ponta Aguda, Marambaia, Iguape and Sepetiba.[16]
The stratigraphy following the classifications by Vieira 2007, Kiang Chang 2008 and Contreras 2011 is:
| Age | Formations | Lithologies | Maximum thickness | Petroleum geology | class=unsortable | Notes | ||||||
|---|---|---|---|---|---|---|---|---|---|---|---|---|
| Coquinas | ||||||||||||
| Shales, limestones, sandstones | Shales, sandstones | SEAL (Marambaia) RES (Marambaia) | ||||||||||
| Miocene | ||||||||||||
| Oligocene | ||||||||||||
| Eocene | ||||||||||||
| Paleocene | ||||||||||||
| Shales, sandstones | Sandstones | Shales, sandstones | SEAL (Itajaí-Açu) RES (Itajaí-Açu, Juréia) SR (Itajaí-Açu) | |||||||||
| Sandstones | Shales | |||||||||||
| Limestones | ||||||||||||
| Evaporites | ||||||||||||
| Carbonates, sandstones, shales, volcanics | ||||||||||||
| Barremian | ||||||||||||
| Granites and gneisses | ||||||||||||
4D Basin analysis of the Santos Basin has revealed insights about the interplay among the elements and processes of the petroleum system to assess source rock potential (vertical and horizontal distribution), thermal evolution of the source rocks, transformation ratio, hydrocarbon generation and charge, timing of migration, oil origin, quality, and volume of petroleum in the main reservoirs. In a basin modeling study performed in 2008 and 2009, a detailed facies model from the pre-salt section was built based on well data and conceptual models from seismic interpretation associated with previous knowledge of the tectono-sedimentary sequences of the Santos Basin. The predicted vitrinite map, integrated with all data, indicates that the Coquinas source rock in most of the eastern half area is in the main oil window, whereas the western half is in the late oil/wet gas generation window. In terms of transformation ratio, the Barremian and Aptian source rock systems in the area reached 70% to 80% today where the main depocentres are. The charge and accumulation simulation model for the pre-salt province suggests a potential reserve in the Cluster area of Santos Basin much larger than that reported, getting numbers to 60 billion barrels of oil reserves.[19]
Exploration in the Santos Basin started in the 1970s. Between 1970 and 1987, 59 dry wells were drilled, with one discovery in Santonian turbidites in 1979, Merluza Field.[20] From 1988 to 1998, 45 wells were drilled in the basin providing small discoveries, with the 30e6oilbbl of oil equivalent Tubarão Field discovered in 1988. Eighty-one wells were drilled from 1999 to 2005, leading to the discovery of the Mexilhão Field. Exploration boomed between 2006 and 2012, with 166 wells and the giant Tupi field (8 BBOE), discovered at the Tupi prospect in 2006. In 2013, the Sagitário Field was discovered in the sub-salt carbonates at a water depth of 1871m (6,138feet) and a true vertical depth of 6150m (20,180feet).[21]
In 2014, the pre-salt reservoirs of the Santos Basin produced more than .[22] Thanks to the pre-salt production, compensating for the declining post-salt production, the total oil production of Brazil rose above in April 2016.[23] The Lapa Field, originally named Carioca, was taken in production in December 2016.[24] In 2017, the Santos Basin accounted for 35% of Brazil's oil, with the Campos Basin at 55%.[25] In the same year, 76 blocks were open for bidding in the Santos Basin.[26]
| Field | Reservoir | Year | Operator | Reserves (in place unless otherwise noted) | class=unsortable | Notes |
|---|---|---|---|---|---|---|
| Echidna | "Paleocene-Maastrichtian" | 2015 | 75abbr=offNaNabbr=off | |||
| Sagitário | 2013 | |||||
| Libra | 2011 | 8000- (recoverable) | ||||
| Búzios | 2010 | 3058abbr=unitNaNabbr=unit | ||||
| Iracema Sul | 2009 | |||||
| Panoramix | 2009 | 176e6oilbbl | ||||
| Piracucá | 2009 | 321.4abbr=unitNaNabbr=unit | ||||
| Vampira | 2009 | |||||
| Iara | 2008 | 3000- | ||||
| Iracema | 2008 | |||||
| Júpiter | 2008 | 1600e6oilbbl 17e12cuft | ||||
| Sapinhoá | 2008 | 1100- | ||||
| Baúna | 2008 | 113e6oilbbl | ||||
| Piracaba | 2008 | 83e6oilbbl | ||||
| Lapa | 2007 | 459e6oilbbl | ||||
| Tupi | 2006 | 8000e6oilbbl | ||||
| Belmonte | 2005 | 158.4abbr=unitNaNabbr=unit | ||||
| Cedro | 2005 | 95.76abbr=unitNaNabbr=unit | ||||
| Tambaú | 2005 | 1.6e12cuft | ||||
| 2003 | 0.173e12cuft | |||||
| Uruguá | 2003 | 174.27abbr=unitNaNabbr=unit 1e12cuft | ||||
| Carapiá | 2002 | 63.52abbr=unitNaNabbr=unit | ||||
| Atlanta | 2001 | 231.16abbr=unitNaNabbr=unit | ||||
| Cavalo Marinho | 2001 | 25.04abbr=unitNaNabbr=unit | ||||
| 2001 | 532.23abbr=unitNaNabbr=unit 3.4e12cuft | |||||
| Pirapitanga | 2001 | 54.24abbr=unitNaNabbr=unit 2.5e12cuft | ||||
| Tambuatá | 1999 | 212.8e6oilbbl | ||||
| Oliva | 1993 | 92.64abbr=unitNaNabbr=unit | ||||
| Caravela | 1992 | 48.81abbr=unitNaNabbr=unit | ||||
| Caravela Sul | 1991 | 5e6oilbbl | ||||
| Coral | 1990 | 22.57abbr=unitNaNabbr=unit | ||||
| Estrela do Mar | 1990 | 15.16abbr=unitNaNabbr=unit | ||||
| Tubarão | 1988 | 30e6oilbbl | ||||
| 1979 | 0.074e12cuft | |||||