Late Jurassic-Early Cretaceous Central Atlantic Sea-Floor Spreading, Closure of Neo-Tethys, and Opening of Canada Basin

1988 ◽  
Keyword(s):  
Early Cretaceous ◽  
Late Jurassic ◽  
Canada Basin ◽  
Sea Floor ◽  
Sea Floor Spreading ◽  
Central Atlantic

Mesozoic sequence of Fuerteventura (Canary Islands): Witness of Early Jurassic sea-floor spreading in the central Atlantic

1998 ◽  
Vol 110 (10) ◽  
pp. 1304-1317 ◽  
Author(s):  
Christian Steiner ◽  
Alice Hobson ◽  
Philippe Favre ◽  
Gérard M. Stampfli ◽  
Jean Hernandez
Keyword(s):  
Canary Islands ◽  
Early Jurassic ◽  
Sea Floor ◽  
Sea Floor Spreading ◽  
Central Atlantic

COMPRESSIONAL GROWTH OF THE MINERVA ANTICLINE, OTWAY BASIN, SOUTHEAST AUSTRALIA—EVIDENCE OF OBLIQUE RIFTING

2004 ◽  
Vol 44 (1) ◽  
pp. 463 ◽  
Author(s):  
C.L. Schneider ◽  
K.C. Hill ◽  
N. Hoffman
Keyword(s):  
Early Cretaceous ◽  
Normal Faults ◽  
Sediment Distribution ◽  
East Central ◽  
Sea Floor ◽  
Structural Style ◽  
Isopach Maps ◽  
Structural Growth ◽  
Oblique Rifting ◽  
Sea Floor Spreading

Shipwreck Trough, east-central Otway Basin, evolved through Early Cretaceous to Santonian extension, followed by Campanian–Paleocene and Miocene to Recent pulses of compression.Onshore to offshore correlation of seismic sequences combined with 3D seismic mapping reveals that the Minerva anticline is located above an Early Cretaceous, northeast trending, basement-involved, graben. The graben-forming, northeast and north–south trending faults became largely inactive prior to the end of the Early Cretaceous. During the Turonian to Santonian, the northeast trending Point Ronald anticline and newly formed east–west trending normal faults controlled sediment distribution. The structural style changed in the Campanian as the northeast trending Minerva anticline began to form with a coeval, northwest-trending, axial-perpendicular fault array located along the crest of the fold. The location and orientation of this fault set is consistent with a compressional mechanism for fold growth. Similar compressional folding events during the Miocene–Recent modified and tightened the fold. Isopach maps show that during the Campanian to Maastrichtian, sediment thinned onto the nascent Minerva anticline, but accommodation rate outpaced structural growth, preserving a continuous sedimentary sequence.The timing of compressional fold growth is enigmatic. Campanian–Maastrichtian compression at the Minerva anticline was synchronous with over 10 km of extension accommodated by the Tartwaup–Mussel hingeline, 50 km to the south. Although the compression may be far-field effects associated with Tasman Basin sea floor spreading, we speculate that the Minerva anticline grew by transpression within a larger left-lateral transtensional Shipwreck Trough.

Cretaceous

1992 ◽  
Vol 13 (1) ◽  
pp. 131-139 ◽  
Author(s):  
J. M. Hancock ◽  
P. F. Rawson
Keyword(s):  
Early Cretaceous ◽  
Sedimentary Basins ◽  
Major Change ◽  
The Arctic ◽  
Sea Floor ◽  
The North ◽  
Marine Sedimentation ◽  
History Of ◽  
Sea Floor Spreading ◽  
Sea Area

AbstractEarly CretaceousThe Cretaceous Period lasted for about 70 million years. During this time there was a major change in the sedimentary history of the area as tectonism died down and deposition started of an extensive blanket of coccolith ooze: the Chalk. The change took place mainly over a brief interval across the Albian/Cenomanian (Lower/Upper Cretaceous) boundary, at about 95 Ma. Until that time crustal extension along the Arctic-North Atlantic megarifts continued to influence the tectonic evolution of northwest Europe (Ziegler 1982, 1988). This tensional régime caused rifting and block faulting, particularly across the Jurassic-Cretaceous boundary (Late Cimmerian movements) and in the mid Aptian (Austrian phase). During the latter phase, sea-floor spreading commenced in the Biscay and central Rockall Rifts. The northern part of the Rockall Rift began to widen too, possibly by crustal stretching rather than sea-floor spreading (Ziegler 1988, p. 75). During the Albian the regional pattern began to change and by the beginning of the Cenomanian rifting had effectively ceased away from the Rockall/Faeroe area.Most of the Jurassic sedimentary basins continued as depositional areas during the Early Cretaceous, but the more extensive preservation of Lower Cretaceous sediments provides firmer constraints on some of the geographical reconstructions. The marked sea-level fall across the Jurassic-Cretaceous boundary isolated the more southerly basins as areas of non-marine sedimentation, and it was not until the beginning of the Aptian that they became substantially marine.The extent of emergence of highs in the North Sea area is difficult to assess, especially where

Tromsø - Bjørnøya Composite Tectono-Sedimentary Element

2021 ◽  
pp. M57-2018-19
Author(s):  
Alf Eivind Ryseth ◽  
Dominique Similox-Tohon ◽  
Olaf Thieβen
Keyword(s):  
Early Cretaceous ◽  
Middle Jurassic ◽  
Late Jurassic ◽  
Barents Sea ◽  
Structural Evolution ◽  
Primary Source ◽  
Source Rocks ◽  
Late Paleozoic ◽  
The North ◽  
Sea Floor Spreading

AbstractThe Tromsø - Bjørnøya composite tectono-sedimentary element in the southwestern Barents Sea comprises strata of Late Paleozoic - Paleocene age. Since the Paleozoic Caledonian orogeny, the structural evolution of the CTSE is mainly related to extension, culminating in Late Jurassic - Early Cretaceous hyperextension. Some compressive deformation observed during Late Cretaceous - Paleogene times may relate to activity in the North Atlantic prior to the Early Eocene onset of sea floor spreading between Norway and Greenland.The sedimentary succession may be up to 14 km thick. It comprises Late Paleozoic continental facies, followed by carbonates, evaporites and eventually cherts and marine clastic material. The overlying Triassic - Paleocene succession is entirely siliciclastic, reflecting Triassic - Middle Jurassic deltaic and shallow marine conditions followed by deeper marine conditions during Late Jurassic - Paleocene times.Primary reservoirs are encountered in the latest Triassic - Middle Jurassic succession, with secondary reservoirs found in Late Jurassic - Early Cretaceous syn-rift succession, and in Paleocene strata. The primary source rock for petroleum is of Late Jurassic - Early Cretaceous age. Other source rocks include strata of Triassic and Barremian age, and a recently observed unit of Cenomanian - Early Turonian age.

A revised magnetic polarity timescale for the Cretaceous and Cainozoic

1982 ◽  
Vol 306 (1492) ◽  
pp. 129-136 ◽  
Keyword(s):  
Magnetic Polarity ◽  
Geomagnetic Reversal ◽  
Sea Floor ◽  
Marine Magnetic Anomalies ◽  
Increasing Trend ◽  
Reversal Frequency ◽  
Spreading Rates ◽  
Sea Floor Spreading ◽  
Central Atlantic ◽  
Stage Boundaries

Magnetostratigraphic correlations of biostratigraphic stage boundaries have established calibration points for dating the polarity reversal sequence derived from marine magnetic anomalies. Interpolation between the best-estimate ages for these tie points gives a revised magnetic polarity timescale for the Cainozoic and Cretaceous. Recomputed sea-floor spreading rates for this time prove to be high during the Cretaceous quiet interval at several plate margins, but remained remarkably constant in the central Atlantic. The geomagnetic reversal frequency, when averaged over intervals of several megayears duration, has exhibited a steadily increasing trend since the late Cretaceous.

scholarly journals Late Jurassic−Early Cretaceous horizontal tectonics drives the Jbel Amsittene Anticline in the Haha Basin, Morocco

2019 ◽  
Author(s):  
David Fernández-Blanco ◽  
Jop Klaver ◽  
Kirsten Brautigam
Keyword(s):  
Early Cretaceous ◽  
Late Jurassic ◽  
Field Data ◽  
Fault Propagation ◽  
Kinematic Indicators ◽  
Fault Propagation Fold ◽  
Central Atlantic

The western Moroccan basins are considered to have acted as stable regions during the postrift phase of the Central Atlantic rifting. Field data, however, show a period of Late Jurassic to Early Cretaceous exhumation. N−S shortening led to the formation of the Jbel Amsittene, located at the northwest most of Haha basin. This anticline was formed in the Late Jurassic to Early Cretaceous, as indicated by syn-tectonic wedges for this period. It is a salt-cored fault propagation fold verging north, with a Triassic salt acting as a detachment plane. Regional kinematic indicators and structures show NNW−SSE to NNE−SSW shortening during the postrift phase. These facts discard the ”salt-drives-tectonics” theory to let ”tectonic-drives-salt” one to rise.

Stratigraphy and tectonic significance of Cretaceous volcanism in the Queen Elizabeth Islands, Canadian Arctic Archipelago

1988 ◽  
Vol 25 (8) ◽  
pp. 1209-1219 ◽  
Author(s):  
Ashton F. Embry ◽  
Kirk G. Osadetz
Keyword(s):  
Hot Spot ◽  
Volcanic Rocks ◽  
Ellesmere Island ◽  
Canada Basin ◽  
Southern Limit ◽  
Sea Floor ◽  
Sverdrup Basin ◽  
Cretaceous Volcanism ◽  
Volcanic Succession ◽  
Sea Floor Spreading

Cretaceous volcanic rocks, which consist mainly of basalt flows and pyroclastic rocks, occur on northern Ellesmere Island, Axel Heiberg Island, and northernmost Amund Ringnes Island as part of the Sverdrup Basin succession. Volcanic rocks are associated with each of four regional transgressive–regressive (T–R) cycles that constitute the Cretaceous clastic succession of Sverdrup Basin and are of Valanginian – early Barremian, late Barremian – Aptian, latest Aptian – early Cenomanian, and late Cenomanian – Maastrichtian age; the volcanic component of each increases northward. The centre of volcanism appears to have been north of Ellesmere Island and is interpreted as the site of a mantle plume that was active throughout the Cretaceous.Most of the volcanic activity took place from Hauterivian to early Cenomanian (T–R cycles 1–3) and was accompanied by widespread sill and dyke intrusion. This activity coincided with the main rifting phase of the adjacent oceanic Canada Basin and with minor crustal extension in the Sverdrup Basin. From late Cenomanian to Campanian, volcanism was restricted to the extreme northeast, and trachytes and rhyolites were extruded along with basalts. This volcanic succession is interpreted as being the southern limit of Alpha Ridge, a major volcanic edifice that formed as a hot-spot track across Canada Basin during sea-floor spreading in Late Cretaceous.

The Canadian Cordillera, the Hellenides, and the Sea-Floor Spreading Theory

1972 ◽  
Vol 9 (6) ◽  
pp. 709-743 ◽  
Author(s):  
Jean Dercourt
Keyword(s):  
Pacific Ocean ◽  
Oceanic Crust ◽  
Continental Margin ◽  
Middle Jurassic ◽  
Late Jurassic ◽  
Late Triassic ◽  
Canadian Cordillera ◽  
Transform Faults ◽  
Sea Floor ◽  
Sea Floor Spreading

The theory of plate tectonics is applied to the tectonic evolution of the Hellenides and the Canadian Cordillera. In the Hellenides a Tethyan zone of sea-floor spreading developed within the continental crust during Triassic time and functioned until the end of the Middle Jurassic. It led to the formation of two plates, each with continental and oceanic segments, that were separated in some places by accreting plate margins and in others by transform faults. In Late Jurassic time the mid-Tethyan ridge became inactive as new ridges developed in the Atlantic Ocean. From Late Jurassic to Recent time, Tethyan oceanic crust largely disappeared under one of the cratons. The chronology of tectonic events in the Hellenides corresponds well with that of sea-floor spreading in the Atlantic.Four periods of sea-floor spreading were involved in the formation of the Canadian Cordillera: (1) a Silurian? to Early Devonian period when an Archeo-Pacific Ocean separated the Canadian craton with a stable sedimentary margin from a volcanic archipelago; (2) a Middle Devonian to Permian period when the extinct volcanic archipelago was bounded to the west by a spreading Paleo-Pacific Ocean, and to the east by a tectonic contact which was consuming Archeo-Pacific oceanic crust; part of this crust was obducted over the continental margin; (3) a Late Triassic to Middle Jurassic period when a second volcanic archipelago separated a spreading Neo-Pacific Ocean from the continental margin; and (4) a Late Jurassic to Recent period where spreading occurred in both the Atlantic and Pacific Oceans, subjecting the second volcanic archipelago and the continental margin to major tectonism; since the Paleocene, the Cordillera has slid towards the NNW along transform faults.

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