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Serravallian
Tectono-stratigraphic evolution of a deep-water foreland basin: a case study from the Marnoso-arenacea basin, central Italy
Middle Miocene (Serravallian; upper Badenian–lower Sarmatian) dinoflagellate cysts from Bad Deutsch-Altenburg, Vienna Basin, Austria
Neodymium isotopes of central Mediterranean phosphatic hardgrounds reveal Miocene paleoceanography
Middle and Upper Miocene Deposits and Facies of Northern Ustyurt (Western Kazakhstan)
The origin of large gypsum crystals in the Geode of Pulpí (Almería, Spain)
Depositional history of the western Nile Delta, Egypt: Late Rupelian to Pleistocene
Basin-scale, high-resolution three-dimensional facies modeling of tectonically confined turbidites: An example from the Firenzuola system (Marnoso-arenacea Formation, northern Apennines, Italy)
Source areas evolution in the Neogene Agost Basin (Betic Cordillera): implications for regional reconstructions
Mid-Miocene (post 12 Ma) Displacement along the Central Karakoram Fault Zone in the Nubra Valley, Ladakh, India from Spot LA-ICPMS U/Pb Zircon Ages of Granites
The Neogene Mediterranean origin of Cyprideis torosa (Jones, 1850)
The tectonically confined Firenzuola turbidite system (Marnoso-arenacea Formation, northern Apennines, Italy)
The Paleogene/Neogene boundary in continental deposits of the West Siberian Plain
Palaeoenvironment, palaeoclimate and age of the Brassington Formation (Miocene) of Derbyshire, UK
Rift and supradetachment basins during extension: insight from the Tyrrhenian rift
The Numidian Flysch: a guide formation for the reconstruction of the paleogeography and tectono-sedimentary evolution of southern Apennines
The Effect of Drainage Reorganization and Climate On the Sedimentologic Evolution of Intermontane Lake Systems: The Final Fill Stage of the Tertiary Ebro Basin (Spain)
Fault growth as a key control on the sedimentary architecture and depositional environments of extensional basins: the case study of the Tablate area (Granada Basin, Spain)
Abstract Reservoirs at Pony-Knotty Head Field consist of stacked, middle Miocene (Serravallian) turbidites deposited as high-frequency low-stand successions within an increasingly ponded basin. Depositional elements include: (1) high to moderate permeability channel axes, channel margins, channelized lobes, and amalgamated lobes; and (2) those having low-permeability, such as marginal to distal lobes, levee-overbank debrites, slumped mudsheterolithics, and pelagic/hemipelagic muds. Fluid pressure data demonstrate that the Pony-Knotty Head Field is segmented into pressure compartments at multiple scales. Although the field is a low-dip, faulted, four-way turtle structure, interpreted faults are neither long enough nor have sufficient throw to segment reservoirs into observed pressure cells. Analyses of individual reservoir units indicate that variations in fluid potential are often greater vertically within wells than laterally between wells. This pattern indicates that at least some segmentation at this scale is due to low-dip stratigraphic barriers between depositional elements rather than to steeply dipping barriers, such as faults. At the field scale, both fluid pressures and depositional elements change vertically. Excess pressure was used to help define compartments at Pony-Knotty Head Field. (“Excess pressure” is the difference between pressure measured in a well and pressure calculated using a datum with an expected fluid gradient.) The deepest reservoirs have the lowest excess pressures. They are dominated by laterally continuous, unconfined depositional elements that bled excess pressure laterally. Progressively shallower reservoirs have progressively higher excess pressures in progressively more confined depositional elements. Between reservoirs of different depths and ages, stratigraphic complexity increased with time as increasing structural confinement of the depocenter above mobile salt drove stratigraphic evolution from a lobe-dominated system to a channelized lobe and levee-channel complex system. We propose that compartmentalization at this scale results directly from stratigraphic responses to the structural evolution of depocenters.