حوض سانتوس

Coordinates: 26°6′22″S 43°43′45″W / 26.10611°S 43.72917°W / -26.10611; -43.72917
(تم التحويل من Santos Basin)
حوض سانتوس
Bacia de Santos
Map showing the location of حوض سانتوس
Map showing the location of حوض سانتوس
Santos basin map.png
موقع حوض سانتوس قبالة ساحل البرازيل.
الإحداثيات26°6′22″S 43°43′45″W / 26.10611°S 43.72917°W / -26.10611; -43.72917
أصل التسميةسانتوس
الموقعأمريكا الجنوبية
المنطقةالاقليم الجنوبي الشرقي، الاقليم الجنوبي
البلدFlag of Brazil.svg البرازيل
الولاياتريو دي جانيرو، ساو پاولو، پارانا، سانتا كاتارينا
المدنكابو فريو، ريو دي جانيرو، گواروجا، سانتوس، إيتاجاي، بالنياريو كامبوريو، فلوريانوپوليس
Characteristics
بري/بحريكلاهما، معظمه بحري
الحدودكابو فريو، مرتفعات فلوريانوپوليس، سـِرا دو مار
جزء منالأحواض البرازيلية على حافة الأطلسي
المساحة~352000 كم²
الهيدرولوجيا
البحارجنوب المحيط الأطلسي
الأنهارريبيرا دى إگواپى
Geology
نوع الحوضحافة مستقرة على حوض الصدع
الصفيحةالصفيحة الأمريكية الجنوبية
التجبلمنبثق من گوندوانا
العمرالباريمي-الحاضر
علم طبقات الأرضطبقات الأرض
الحقولتوپي، ليبرا، جوپيتر، أخرى
تتكون الحافة الشمالية للحوض من مرتفع كابو فريو، الممتد باتجاه الجنوب الشرقي من كابو فريو على الساحل.
إيتاجاي (يسار) وبالنياريو كامبوريو (يمين) على الحافة الجنوبية لحوض سانتوس البري.

حوض سانتوس (برتغالية: Bacia de Santos، إنگليزية: Santos Basin)، هو حوض رسوبي بحري في معظمه، تبلغ مساحته نحو 352.000 كم²، ويقع في جنوب المحيط الأطلسي على بعد نحو 300 كم جنوب شرق سانتوس، البرازيل. يُعد سانتوس أحد الأحواض البرازيلية التي تشكّلت نتيجة تفكك الگندوانا منذ أوائل العصر الطباشيري، حين نشأت سلسلة من الأحواض الصدعية على جانبي جنوب المحيط الأطلسي، وتشمل في البرازيل أحواض پلوتاس، سانتوس، كامپوس، وإسپيريتو سانتو، وفي جنوب غرب أفريقيا أحواض ناميبيا، كوانزا والكونغو.

ينفصل حوض سانتوس عن حوض كامپوس شمالاً بمرتفع كابو فريو، وعن حوض پلوتاس جنوباً بمرتفع فلوريانوپوليس، بينما تشكّل سلسلة جبال سـِرا دو مار الساحلية حدوده الشمالية الغربية على اليابسة. ويشتهر الحوض بوجود طبقات سميكة من الملح التي كوّنت هياكل تحت السطح بفعل التكتونيات الملحية. بدأ الحوض في التشكّل خلال أوائل العصر الطباشيري فوق راسخ الكونغو كحوض صدعي. وقد أدت مرحلة التصدّع في تطور الحوض، إلى جانب مناخ الأپتيان الجاف في خطوط العرض الجنوبية، إلى ترسّب المتبخرات في أواخر الأپتيان، قبل نحو 112 مليون سنة. تلت مرحلة التصدّع مرحلة ترهل حراري، ثم مرحلة انجراف مع اتساع جنوب المحيط الأطلسي، ما أدى إلى ترسّب سلسلة من الرواسب الفتاتية والكربونات بسمك يتجاوز 20 كم.


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 250 thousand barrels per day (40×10^3 m3/d). In 2017, the Santos Basin accounted for 35% of Brazil's oil, with the northern neighbour Campos Basin at 55%.

التسمية

The Santos Basin is named after the coastal city of Santos in the state of São Paulo.[بحاجة لمصدر]

الوصف

Outline of the Serra do Mar coastal forest ecoregion, bordering the Santos Basin

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 352،000 متر كيلومربع (136،000 sq mi),[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 12،000 متر كيلومربع (4،600 sq mi). 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.[بحاجة لمصدر]

التاريخ التكتوني

The break-up of Pangaea characterised the start of formation of the Santos Basin in the South Atlantic, forming at the same time the Kwanza Basin in Africa.[5]
The Santos Basin formed with the rifting of Brazil and Africa splitting the Congo Craton from the Araçuaí Belt, shown as a thin brown strip.
Schematic diagram of the formation of a passive margin on a rift basin

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.[6] 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.[7] Basalts similar to the Paraná and Etendeka traps, exposed to the west in the Paraná Basin, have been found underlying the Santos Basin.[8] The Tristan da Cunha hotspot, known as the Tristan hotspot, is considered the driver behind the formation of these flood basalts.[9]

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.[بحاجة لمصدر]

Five tectonic stages have been identified in the Brazilian basins:[10]

  1. Pre-rift stage – Jurassic to Valanginian
  2. Syn-rift stage – Hauterivian to Late Barremian
  3. Sag stage – Late Barremian to Late Aptian
  4. Post-rift stage – Early to Middle Albian
  5. Drift stage – Late Albian to Holocene

The sag phase in the Santos Basin was characterised by thermal subsidence and generated restricted depocentres with relatively uniform water depths, ranging from 600 إلى 950 متر (1،970 إلى 3،120 ft). 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.[11] The deposition of the lowermost 600 متر (2،000 ft) of salt in the Aptian would have taken approximately 20,000 to 30,000 years.[12] 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.[11]

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.[13]

طبقات الأرض

Sugarloaf Mountain and the other inselbergs of Rio de Janeiro are the onshore representatives of the basement of the Santos Basin.

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.[بحاجة لمصدر]

The total stratigraphic thickness of the sediments in the Santos Basin has been estimated at 23،170 متر (76،020 ft) and has been described in detail by Clemente in 2013.[14]

مجموعة گواراتيبا 1

The Guaratiba Group is characterised by the presence of microbialites, like this present-day example in Pavilion Lake, Canada. These organic build-up structures are the reservoir of the giant pre-salt Tupi field, holding 8000 million barrels of oil.

The Guaratiba Group is 4،200 متر (13،800 ft) 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.[14]

Camboriú Formation

The Camboriú Formation is 40 متر (130 ft) thick and includes the basaltic rocks with a basin–wide distribution. The basalts are dark green to dark grey, holocrystalline, medium grained, with an ophiolitic texture. The main components are plagioclase and augite, usually fresh, non-altered.[14]

The syn-rift stage of the Santos Basin was characterised by the formation of half-grabens where rift shoulders were exposed and eroded, providing various sediment sources for the deposition in the lacustrine to shallow marine parts.
Piçarras Formation

The Piçarras Formation is 990 متر (3،250 ft) thick and consists of clastic and carbonate rocks. The formation includes reddish polymictic conglomerates, with clasts of basalt and quartz in a clay-sandy matrix. It also includes white, reddish lacustrine coquinas (shelly limestones) and sandstones, siltstones and shales of stevensite composition. Its age, based on the ostracod assemblages, is Hauterivian to Aptian.[14]

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.[15]

Itapema Formation

The Itapema Formation is several hundreds of metres thick and consists of calcirudites (limestones) and dark shales. The calcirudite limestones consist of fragmented bivalve shells, frequently dolomitized and silicified. In more distal sections, the formation consists of dark organic matter rich shales. In the well 1-RSJ-625, the formation includes 110 متر (360 ft) of radioactive shales interbedded with carbonates. These facies are thought to represent a lacustrine environment. The organic matter-rich shales are one of the main source rocks of the Santos Basin. This formation is correlative with the Coqueiros Formation in the Campos Basin. The age of the Itapema Formation is Barremian to Aptian.[15]

Barra Velha Formation

The Barra Velha Formation is approximately 300 إلى 350 متر (980 إلى 1،150 ft) thick. In the proximal sections, the formation comprises limestones of stromatolites and laminated microbialites. In the distal sections, it is composed of shales. Interbedded with the laminated microbialites there are limestones with packstone and grainstone textures made up of algal clasts and bioclasts (fragmented ostracods). The carbonates frequently are partly or completely dolomitized. These facies represent a transitional continental and shallow marine environment. The age of this formation has been estimated to be Late Barremian to Aptian. It is correlative with the Macabu Formation in the Campos Basin, as both are typified by laminated microbialites and stromatolites. These limestones are one of the sub-salt reservoirs in the Santos Basin.[15]

تشكيل أريري 2

The Ariri Formation, originally deposited as flat evaporite layers, has undergone extensive diapirism and canpoy formation during the Albian to Paleocene.

The Ariri Formation is in the type oil well[clarify] 581 متر (1،906 ft) thick and may be up to 4،000 متر (13،000 ft) 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).[15]

مجموعة كامبوري 3

The Camburi Group is up to 6،100 متر (20،000 ft) thick and includes three formations, Florianópolis, Guarujá and Itanhaém.[16]

Florianópolis Formation

The Florianópolis Formation is 343 متر (1،125 ft) thick in the type oil well, and consists of reddish, fine to coarse-grained sandstones with a clay matrix, reddish micaceous shales and siltstones. These clastic units are thought to represent alluvial environments distributed along the western Brazilian basin margin, along the Santos Hinge Line. These alluvial environments were gradational towards the east, with the shallow marine carbonates of the Guarujá Formation, and further to the open basin with the siltstones of the Itanhaém Formation. Biostratigraphical data and its relations with the Guarujá Formation point towards an Albian age.[16]

The depositional environment of the Guarujá Formation has been interpreted as a tidal flat, like this present-day example in Oregon, United States.
Guarujá Formation

The Guarujá Formation is 832 متر (2،730 ft) thick and consists of oolitic calcarenites, which laterally grade to greyish ochre and brownish grey calcilutites and grey marls. These facies are interbedded with the alluvial clastics of the Florianópolis Formation. The Guarujá name is restricted to the lowest limestone intercalation, previously named Lower Guarujá by Ojeda and Ahranha in Pereira and Feijó (1994). The microfacies indicate a tidal flat to shallow lagoon and open carbonate platform depositional environment. The age based on planktonic foraminifera and pollen is Early Albian.[16]

Itanhaém Formation

The Itanhaém Formation is 517 متر (1،696 ft) thick and consists of dark grey shales, silts and light grey marls, ochre-brown calcisilts and subordinated sandstones. These facies change laterally into the coarse clastics of the Florianópolis Formation. Facies analysis indicates a marine environment ranging from sub-littoral (inner neritic) and more rarely to pelagic (outer bathyal) conditions. The age based on planktonic foraminifera and pollen is Early Albian.[16]

مجموعة فرادى 4

The Itajaí-Açu and Juréia Formations consist mainly of turbidites, formed at the base of the Brazilian marginal continental slopes. The sands of these formations have proven to be excellent reservoirs worldwide.

The Frade Group is 4،000 متر (13،000 ft) thick and includes three formations: Santos, Itajaí-Açu and Juréia. They predominantly comprise turbidites.[17]

Santos Formation

The Santos Formation is 1،275 متر (4،183 ft) thick and consists of reddish lithic conglomerates and sandstones, interbedded with grey shales and reddish clays. These facies are interbedded and change laterally into the Itajai-Açu and Juréia Formations. The sedimentary environment is thought to be transitional continental to marginal marine, ranging from alluvial to braided rivers and deltas. Biostratigraphic data indicate a Late Cretaceous age (Cenomanian-Maastrichtian).[17]

Itajaí-Açu Formation

The Itajaí-Açu Formation is 1،545 متر (5،069 ft) thick and comprises a thick interval of dark grey clayey rocks, interbedded with the clastics of the Santos and Juréia Formations. Within this formation, the Ilhabela Member includes the turbiditic sandstones occurring along the section. The sedimentary environment is thought to be marine talus to open basin. Biostratigraphic data from palynomorphs, calcareous nannofossils and planktonic foraminifera indicate a Late Cretaceous age (Cenomanian-Maastrichtian).[17]

Ostracods are small crustaceans commonly used to identify paleo-environments and for age dating formations
Juréia Formation

The Juréia Formation is 952 متر (3،123 ft) thick and includes a succession of clastics between the coarse facies of the Santos Formation in the west and the fine-grained clastics of the Itajai-Açu Formation in the east. The formation is characterized by dark grey to greenish and brown shales, dark grey siltstones, fine-very fine sandstones and light ochre calcisilts. The depositional environment is thought to be of a marine platform setting. The age based on palynomorphs and calcareous nanofossils is Late Cretaceous (Santonian-Maastrichtian).[17] Two new ostracod species were identified in the drilling cuttings of wells drilled into the Santonian-Campanian section, ?Afrocytheridea cretacea and Pelecocythere dinglei.[18]

مجموعة إيتامامبوكا 5

Itamambuca Group is 4،200 متر (13،800 ft) thick and includes four formations, Ponta Aguda, Marambaia, Iguape and Sepetiba.[17]

Ponta Aguda Formation

The Ponta Aguda Formation is up to 2،200 متر (7،200 ft) thick and consists of conglomerates, coarse to fine-grained sandstones interbedded with siltstones and shales. The dominant facies are coarse to fine-grained quartzitic sandstones. They range from reddish to grey, usually with calcite cements. Intercalated are reddish to light grey claystones and siltstones. They represent a fluvial to shallow marine environment.[19]

Iguape Formation

The Iguape Formation is 1،103 متر (3،619 ft) thick and consists of bioclastic calcarenites and calcirudites, containing bryozoa, echinoids, corals, foraminifera, fragmented shells, and algae remains. They are interbedded with grey-greenish clays, siltstones, marls and variegated grey fine-to-medium grained conglomerates. These facies are interbedded with and change laterally to the Marambaia Formation. The depositional environment is thought to be a marine carbonate platform, influenced by the arrival of alluvial clastics in the most proximal areas. Biostratigraphic data from planktonic foraminifera, calcareous nanofossils and palynomorphs indicate a Tertiary age.[19]

The uppermost sedimentary layer is formed by coquinas (similar to this sample from Crimea in Europe); carbonitic sandstones composed of broken shells
Marambaia Formation

The Marambaia Formation is 261 متر (856 ft) thick and consists of grey shales and light grey marls interbedded with fine-grained turbiditic sandstones. This formation in places can be found cropping out at sea bottom. The depositional environment is thought to be talus and open marine basin. Biostratigraphic data indicate a Tertiary age.[19]

Sepetiba Formation (Pleistocene)

The Sepetiba Formation is the uppermost formation in the Santos Basin. It has a variable thickness due to the proximal erosion of the uppermost part. The formation consists of whitish grey fine to coarse grained carbonitic sands. They are feldspar-rich, glauconitic coquinas consisting of bivalve fragments and foraminifera. The depositional environment is thought to be coastal.[19]

The stratigraphy following the classifications by Vieira 2007, Kiang Chang 2008 and Contreras 2011 is:

Age Formations Lithologies Maximum thickness Petroleum geology Notes
Pleistocene Sepetiba Fm. Coquinas
570 m (1،870 ft)
 Overburden
[20][21]
Pliocene Iguape Fm. Marambaia Fm. Shales, limestones, sandstones Shales, sandstones
2،200 m (7،200 ft)
2،700 m (8،900 ft)
 SEAL
(Marambaia)
RES
(Marambaia)
[20][22]
[23][24]
Miocene
Oligocene
Eocene
Paleocene
Maastrichtian Santos Fm. Juréia Fm. Itajaí-Açu Fm. Shales, sandstones Sandstones Shales, sandstones
2،700 m (8،900 ft)
2،000 m (6،600 ft)
2،000 m (6،600 ft)
 SEAL
(Itajaí-Açu)
RES
(Itajaí-Açu, Juréia)
SR
(Itajaí-Açu)
[20][22][23]
[24][25]
Campanian
Santonian
Coniacian
Turonian
Cenomanian
Late Albian Florianópolis Fm. Itanhaém Fm. Sandstones Shales
1،500 m (4،900 ft)
 RES
[20][22][23]
Early Albian Guarujá Fm. Limestones
2،500 m (8،200 ft)
 RES
[20][22][23]
Ariri Fm. Evaporites
2،500 m (8،200 ft)
 SEAL
[20][22][24]
Late Aptian
Early Aptian Guaratiba Gp. Carbonates, sandstones, shales, volcanics
~1،500 m (4،900 ft)
 SEAL, RES, SR
[20][22]
[25][26]
Barremian
Hauterivian Camboriú Fm. Basalt
[20][22]
Valanginian
Jurassic
Triassic
Paleozoic
Precambrian Araçuarí Belt Granites and gneisses Basement
[7][20]

تحليل الحوض

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.[27]

التنقيب عن النفط والغاز

موقع مقل توپي المحتمل.

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.[28] From 1988 to 1998, 45 wells were drilled in the basin providing small discoveries, with the 30 million برميل (4.8 million متر مكعب) 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 1،871 متر (6،138 ft) and a true vertical depth of 6،150 متر (20،180 ft).[29]

In 2014, the pre-salt reservoirs of the Santos Basin produced more than 250 thousand barrels per day (40×10^3 m3/d).[30] Thanks to the pre-salt production, compensating for the declining post-salt production, the total oil production of Brazil rose above 2،500 thousand barrels per day (400×10^3 m3/d) in April 2016.[31] The Lapa Field, originally named Carioca, was taken in production in December 2016.[32] In 2017, the Santos Basin accounted for 35% of Brazil's oil, with the Campos Basin at 55%.[33] In the same year, 76 blocks were open for bidding in the Santos Basin.[34]

في 4 أغسطس 2025، أعلنت شركة ب پ عن حفرها البئر الاستكشافي 1-BP-13-SPS في بلوك بومرانگي، الواقعة في حوض سانتوس، على عمق 2.372 متر تحت سطح الماء. وحُفر البئر إلى عمق إجمالي يبلغ 5.855 متراً. وقد قطع البئر الخزان على عمق نحو 500 متر أسفل قمة الهيكل واخترق عموداً هيدروكربونياً إجمالياً يبلغ طوله 500 متر تقريباً في خزان كربونات ما قبل الملح عالي الجودة بمساحة تزيد عن 300 كم². تشير نتائج تحليل موقع الحفر إلى ارتفاع مستويات ثاني أكسيد الكربون. ستبدأ شركة ب پ الآن تحليلاتٍ مختبريةً لتوصيف الخزان والسوائل المكتشفة بشكلٍ أعمق، مما سيوفر فهماً أعمق لإمكانات بلوك بومرانگي. ومن المقرر إجراء المزيد من أنشطة التقييم، رهناً بموافقة الجهات التنظيمية.[35]

تمتلك شركة ب پ حصة 100% في بلوك بومرانگي مع شركة Pré-Sal Petróleo. ب پ على ترخيص البلوك في ديسمبر 2022.

حقول النفط والغاز

الحقل
الخط العريض يشير إلى ما قبل الملحي 		الخزان السنة المشغل الاحتياطيات (في الموقع ما لم يُذكر غير ذلك)
ملاحظات
إتشيدا "الپليوسيني-الماستريشتياني" 2015 كارون إنرجي أستراليا 11.9 مليون م³
[36]
ساگيتاريو مجموعة گواراتيبا 2013 پتروبراس
[37]
ليبرا مجموعة گواراتيبا 2011 پتروبراس 1.300–1.900 مليون م³ (قابلة للاسترداد)
[38][39]
بوزيوس مجموعة گواراتيبا 2010 پتروبراس 486 مليون م³
[40]
إراكما سول 2009 پتروبراس
[41]
پانوراميكس تكوين إيتاجاي-أتشو 2009 رپسول 28.0 مليون م³
[28]
پيراكوكا تكوين إيتاجاي-أتشو 2009 پتروبراس 51.1 مليون م³
[28][42]
ڤامپيرا 2009 رپسول
[43]
إيارا مجموعة گواراتيبا 2008 پتروبراس 480–640 مليون م³
[44]
إراكما مجموعة گواراتيبا 2008 پتروبراس
[45]
جوپيتر مجموعة گواراتيبا 2008 پتروبراس 250 مليون م³
480 بليون م³
[37]
ساپينهوا مجموعة گواراتيبا 2008 پتروبراس 320 مليون م³
[46]
باونا 2008 پتروبراس 18.0 مليون م³
[47]
پيراكابا 2008 پتروبراس 13.2 مليون م³
[47]
لاپا مجموعة گواراتيبا 2007 پتروبراس 73.0 مليون م³
[32]
توپي مجموعة گواراتيبا 2006 پتروبراس 1.300 م³
[48]
بلمونتى 2005 إني 25.2 مليون م³
[28]
سدرو تكوين إيتاجاي-أتشو 2005 پتروبراس 15.2 مليون م³
[28][49]
تامباو تكوين إيتاجاي-أتشو 2005 پتروبراس 45 مليون م³
[50]
لاگوستا تكوين إيتاجاي-أتشو 2003 إل پاسو 4.9 مليون م³
[28][50]
أوروگوا تكوين إيتاجاي-أتشو 2003 پتروبراس 27.7 مليون م³
28 بليون م³
[28][50]
كاراپيا تكوين إيتاجاي-أتشو 2002 پتروبراس 10.1 مليون م³
[28][50]
أطلنطا تكوين مرامبايا 2001 QGEP 36.8 مليون م³
[28][50][51]
كاڤالو مارينهو تكوين گواروجا 2001 پتروبراس 3.98 مليون م³
[28][52]
مكسيلهاو تكوين إيتاجاي-أتشو 2001 پتروبراس {84.6 مليون م³
96 بليون م³
[28][52][53]
پيراپيتانگا تكوين فلوريانوپوليس 2001 پتروبراس 8.62 مليون م³
71 بليون م³
[28][50]
تامبواتا تكوين إيتاجاي-أتشو 1999 پتروبراس 212.8 million bbl (33.83 million m3)
[28][52]
أوليڤا تكوين مرامبايا 1993 شل 92.64 million bbl (14.7 million m3)
[28][50][51]
كاراڤلا تكوين گواروجا 1992 پتروبراس 7.76 مليون م³
[28][54]
كاراڤلا سول تكوين گواروجا 1991 پتروبراس 0.79 مليون م³
[28]
كورال تكوين گواروجا 1990 پتروبراس 3.59 مليون م³
[28][55]
إسترلا دو مار تكوين گواروجا 1990 پتروبراس 2.41 مليون م³
[28][56]
توباراو تكوين گواروجا 1988 پتروبراس 4.8 مليون م³
[57]
مرلوزا تكوين جوريا 1979 پكتن 2.1 بليون م³
[28][58]

انظر أيضاً


المصادر

  1. ^ Constantino et el., 2016, p.200
  2. ^ Clemente, 2013, p.18
  3. ^ Contreras, 2011, p.1
  4. ^ Gomes et al., 2009, p.3
  5. ^ Love, 2015, 16:16
  6. ^ Clemente, 2013, p.3
  7. ^ أ ب Owen, 2014, p.36
  8. ^ Peate, 1997, p.220
  9. ^ Beasley et al., 2010, p.31
  10. ^ Contreras, 2011, p.7
  11. ^ أ ب Contreras, 2011, p.8
  12. ^ Bryant et al., 2012, p.51
  13. ^ Alves et al, 2017, p.319
  14. ^ أ ب ت ث Clemente, 2013, p.20
  15. ^ أ ب ت ث Clemente, 2013, p.21
  16. ^ أ ب ت ث Clemente, 2013, p.22
  17. ^ أ ب ت ث ج Clemente, 2013, p.23
  18. ^ Piovesan, 2010, p.177
  19. ^ أ ب ت ث Clemente, 2013, p.24
  20. ^ أ ب ت ث ج ح خ د ذ Kiang Chang et al., 2008, p.32
  21. ^ Kiang Chang et al., 2008, p.34
  22. ^ أ ب ت ث ج ح خ Contreras, 2011, p.22
  23. ^ أ ب ت ث Vieira, 2007, p.19
  24. ^ أ ب ت Contreras, 2011, p.77
  25. ^ أ ب Vieira, 2007, p.18
  26. ^ Vieira, 2007, p.24
  27. ^ Mello et al., 2009, p.47
  28. ^ أ ب ت ث ج ح خ د ذ ر ز س ش ص ض ط ظ ع غ "Santos Basin Fields". Archived from the original on 2017-09-07. Retrieved 2017-09-07.
  29. ^ Juarez, 2013, p.1
  30. ^ Moczydlower, 2014, p.34
  31. ^ Oddone, 2017, p.5
  32. ^ أ ب Ribeiro da Silva & Pereira, 2017, p.136
  33. ^ Brazil Draws Auctions Calendar, Confirms Santos Basin Most Attractive Area
  34. ^ Petersohn, 2017, p.18
  35. ^ "bp announces hydrocarbon discovery at Bumerangue exploration well, offshore Brazil". bp. 2025-08-04. Retrieved 2025-08-13.
  36. ^ Echidna Field
  37. ^ أ ب Juarez, 2013, p.44
  38. ^ Moczydlower, 2014, p.42
  39. ^ Moczydlower, 2014, p.52
  40. ^ Búzios Field
  41. ^ Iracema Sul Field
  42. ^ Piracucá Field
  43. ^ Vampira Field
  44. ^ Iara Field
  45. ^ Brazil Confirms Massive Offshore Oil Field
  46. ^ Sapinhoá Field
  47. ^ أ ب Baúna and Piracaba Fields
  48. ^ Juarez, 2013, p.24
  49. ^ Petrobras BS-400 gas find confirms E&P expansion plans
  50. ^ أ ب ت ث ج ح خ Vieira, 2007, p.9
  51. ^ أ ب Atlanta Field
  52. ^ أ ب ت Juarez, 2013, p.14
  53. ^ Vieira, 2007, p.8
  54. ^ ANP Yearbook, 2014, p.30
  55. ^ Coral Field: Case History in Oil Producing Albian Carbonates in Santos Basin, Brazil
  56. ^ Estrela do Mar, Cavalo Marinho oil output by 2007
  57. ^ Juarez, 2013, p.11
  58. ^ Juarez, 2013, p.7

المراجع

عامة عن البرازيل

جيولوجيا حوض سانتوس

استكشاف حوض سانتوس

وصلات خارجية

قالب:Sedimentary basins of Brazil

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