| Lusitanian Basin | |
| Named For: | Lusitania |
| Coordinates: | 39.4361°N -8.9372°W |
| Region: | Iberian Peninsula |
| Cities: | Lisbon, Aveiro, Leiria, Figueira da Foz |
| Onoffshore: | Both |
| Partof: | Iberian Mesozoic Sedimentary Basins |
| Seas: | North Atlantic |
| Lakes: | Lagoa de Óbidos |
| Area: | 22000km2 |
| Basin Type: | Rift |
| Plate: | Eurasian |
| Orogeny: | Opening of the North Atlantic Ocean |
| Age: | Late Triassic-Late Cretaceous |
| Stratigraphy: | Stratigraphy |
| Faults: | Nazaré Fault |
The Lusitanian Basin is a rift basin remnant located on both the mainland and continental shelf off the west-central coast of Portugal. It covers an area measuring [1] and extends north-south from Porto to Lisbon.[2] The basin varies between approximately and in width and belongs to a family of periatlantic basins such as the Jeanne d'Arc Basin. To the east of the Lusitanian Basin lies the Central Plateau of the Iberian Peninsula. A marginal horst system lies to the west. The Alentejo and Algarve Basins connect to the southern end of the Lusitanian Basin. In the north, it connects to the Porto and Galicia Basins via an undersea ridge.[3]
The Lusitanian Basin results from the opening of the North Atlantic Ocean due to Mesozoic extension. Throughout the complete formation of the basin, from the Late Triassic to the Cretaceous, five distinct phases can be defined, with four stages of rifting activity:
The most significant faults and salt structures throughout the Lusitanian Basin trend north-northeast, parallel to the elongation of the shoreline. The faults that trend northeast to east-northeast are fewer in number. However, they are fairly substantial—for example, the Nazare Fault. The north-trending faults are concentrated mainly in the central part of the Lusitanian Basin. These faults are a part of in important structural trend within the Estremadura Trough which highlights the Oxfordian extension within the basin. West-northwest trending faults are scattered throughout the basin.[4] Both thrust faults and normal faults are observed. The thrusting observed is resultant of the basement-attached inversion movements of the pre-existing normal faults during the Miocene. Most of the faults within the basin are fairly high-angle, with some shallowing with depth observed. There is always faulting beneath salt structures and it is speculated that the movement of the salt structures is caused by basement-influenced faulting.
Resultant of diapirism leading to the formation of salt pillows, the Lusitanian Basin can be divided into seven different sub-basins:
The Lusitanian basin Triassic to Cretaceous rocks provided thousands of fossils, from plants, microfossils, invertebrates and vertebrates. The most productive formations are the Late Jurassic Lourinhã Formation, Alcobaça Formation, and Montejunto Formation and the Cretaceous Papo Seco Formation. This includes an outstanding abundance of Jurassic mammals, and dinosaur fossils and trackways.[6] [7]
The Lusitanian Basin is a late Triassic rift basin is filled with synrift siliciclastics and capped by post-rift evaporites. In the late Triassic, there was deposition of fluvial sand and clay that eventually evolved into deposition of shallow marine dolomites during the lower and middle Jurassic. These sediments are known as the Silves, Dagorda, and Coimbra Formations. Deposition of Carbonates of the Brenha and Candieros Formations are in shelf, ramp, and sub-marine fan environments and filled the basin during the early and middle Jurassic. The carbonate formations are commonly interbedded with shale and there are local turbidite beds also present. Below the halite-bearing evaporites that compose the Dagorda formation are the synrift continental siliciclastics of the Silves formation. Above the Dagorda formation is the post-rift carbonate shelf environment—the Coimbra dolomite, Brenha limestone, and Cardieros carbonate grainstone. A substantial unconformity, associated with significant tectonic activity, characterizes the top of the sequence. The carbonate shelf environment is still present in the Upper Jurassic—characterized by the Montejunto grainstone and reef facies, Cabacos organic-rich limestone (capped by anhydrite). Above this sequence, deposition is dominated by the siliciclastics from the Meseta highlands. The Abadia formation is composed of shale, marl, siltstone, and minimal sandstone. The rest of the Upper Jurassic and Cretaceous is dominated by westward-prograding continental clastics.
In the basin, all Jurassic source-rocks could possibly be within the hydrocarbon generation window. However, this is not the case throughout the entire basin. This is due to the highly heterogeneous nature of basin subsidence, especially in the Late Jurassic. Around 100 exploratory wells have been drilled in the basin. 80% of these wells, from Triassic, Jurassic, and Cretaceous strata, had oil and gas shows while drilling and 27% recovered live oil or gas at surface. While there is substantial hydrocarbon potential in this basin alone, Portugal imports 100% of its fossil fuel. There are two major petroleum systems at work within the basin—Subsalt and Suprasalt. In the subsalt petroleum system, there are Paleozoic source rocks and synrift Triassic sandstone reservoirs that are sealed by Dagorda evaporites. In the suprasalt system, the oldest source rock is the Lower Brenha formation. The best reservoirs to mention include the Coimbra dolomite and Upper Dagorda carbonates, Candieiros oolitic and bioclastic grainstones, and the fractured carbonates of the Brenha formation. Seals are tight or marly carbonates of the Brenha and overlying basal Upper Jurassic.
N. Pimentel1 and R. Pena dos Reis (2016) - PETROLEUM SYSTEMS OF THE WEST IBERIAN MARGIN: A REVIEW OF THE LUSITANIAN BASIN AND THE DEEP OFFSHORE PENICHE BASIN. Journal of Petroleum Geology, Vol. 39(3), July 2016, pp 305-326. [8]