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NARROW
GeoRef Subject
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all geography including DSDP/ODP Sites and Legs
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Atlantic Ocean
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Primary terms
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Atlantic Ocean
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North Atlantic
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Bay of Fundy (2)
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North Sea (1)
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Scotian Shelf (2)
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Atlantic region (1)
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Australasia
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Australia (1)
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New Zealand (1)
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Canada
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lower Mesozoic (3)
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rock formations
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sandstone (1)
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sedimentary structures
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sedimentary structures
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soft sediment deformation
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Three-dimensional fault geometries and interactions within experimental models of multiphase extension
Analogue benchmarks of shortening and extension experiments
Abstract We report a direct comparison of scaled analogue experiments to test the reproducibility of model results among ten different experimental modelling laboratories. We present results for two experiments: a brittle thrust wedge experiment and a brittle-viscous extension experiment. The experimental set-up, the model construction technique, the viscous material and the base and wall properties were prescribed. However, each laboratory used its own frictional analogue material and experimental apparatus. Comparison of results for the shortening experiment highlights large differences in model evolution that may have resulted from (1) differences in boundary conditions (indenter or basal-pull models), (2) differences in model widths, (3) location of observation (for example, sidewall versus centre of model), (4) material properties, (5) base and sidewall frictional properties, and (6) differences in set-up technique of individual experimenters. Six laboratories carried out the shortening experiment with a mobile wall. The overall evolution of their models is broadly similar, with the development of a thrust wedge characterized by forward thrust propagation and by back thrusting. However, significant variations are observed in spacing between thrusts, their dip angles, number of forward thrusts and back thrusts, and surface slopes. The structural evolution of the brittle-viscous extension experiments is similar to a high degree. Faulting initiates in the brittle layers above the viscous layer in close vicinity to the basal velocity discontinuity. Measurements of fault dip angles and fault spacing vary among laboratories. Comparison of experimental results indicates an encouraging overall agreement in model evolution, but also highlights important variations in the geometry and evolution of the resulting structures that may be induced by differences in modelling materials, model dimensions, experimental set-ups and observation location.
Abstract We use geometric and experimental models to study the development of extensional fault-bend folds. The geometric models show that fault shape, fault displacement, and patterns of aggradation/erosion profoundly affect the distribution of growth beds, the magnitude and direction of dip of pregrowth and growth beds, and the location and dip of the outer limit of folding in pregrowth and growth beds. Complex structural and stratigraphic patterns develop if the rate of aggradation/erosion relative to the rate of fault displacement changes through time. The experimental models (with dry sand and wet clay) show that several deformational styles can accommodate extensional fault-bend folding. In sand models, a few, relatively major, secondary antithetic normal faults accommodate most hanging wall deformation. Pregrowth layers, although faulted, remain flat. The effective shear direction parallels the antithetic normal faults, and the shear angle is about 60°-65°. In clay models, numerous, relatively minor, secondary normal faults (antithetic and synthetic) and cataclastic flow accommodate most hanging wall deformation. The deformed pregrowth and growth layers dip gently toward the main fault. The effective shear angle (35 Q -50°) is considerably less than the dip of the antithetic normal faults. In the sand models and geometric models with a large shear angle (60°), more displacement occurs on the main normal fault and the hanging wall collapses in a relatively narrow zone. In the clay models and geometric models with a small shear angle (35°), less displacement occurs on the main normal fault. Instead, the hanging wall stretches substantially and collapses in a relatively wide zone.
Abstract Field, seismic, and drill-hole data provide a wealth of information about the tectonic processes associated with rifting, breakup, and the early stages of seafloor spreading for the passive margin of eastern North America. The onset of rifting, from Florida to the Canadian Grand Banks, was approximately synchronous, occurring by Late Triassic time. The cessation of rifting (and presumably the onset of drifting) was diachronous, occurring first in the southeastern United States (latest Triassic), then in the northeastern United States and southeastern Canada (Early Jurassic), and finally in the Grand Banks (Early Cretaceous). The Central Atlantic Magmatic Province developed simultaneously (earliest Jurassic, ~200 Ma) throughout eastern North America. This magmatic activity occurred after rifting in the southeastern United States, and during rifting in the northeastern United States and maritime Canada. The passive margin, from Florida to southern Nova Scotia, is volcanic, characterized by seaward-dipping reflectors ( SDRs ) near the continent-ocean boundary. The remainder of the passive margin lacks SDRs and is, thus, non-volcanic. In the continental crust, most rift-related structures parallel preexisting zones of weakness created by Paleozoic and older orogenies. Few transfer zones exist, and these also parallel the pre-existing fabric. In the oceanic crust, fracture zones parallel the direction of relative plate motion. Thus, the trends of the fracture zones in the oceanic crust differ from the trends of the rift-related structures in the continental crust. The deformational regime changed substantially after rifting throughout eastern North America: post-rift shortening (inversion) replaced syn-rift extension. Detached structures associated with salt movement also developed after rifting, especially on the Scotian shelf and Grand Banks.
The early Mesozoic Birdsboro central Atlantic margin basin in the Mid-Atlantic region, eastern United States: Discussion
An Experimental Study of the Secondary Deformation Produced by Oblique-Slip Normal Faulting
Abstract Rift basins are complex features defined by several large-scale structural components including faulted margins, the border faults of the faulted margins, the uplifted flanks of the faulted margins, hinged margins, deep troughs, surrounding platforms, and large-scale transfer zones. Moderate- to small-scale structures also develop within rift basins. These include: basement-involved and detached normal faults; strike-slip and reverse faults; and extensional fault-displacement, fault-propagation, forced, and fault-bend folds. Four factors strongly influence the structural styles of rift basins: the mechanical behavior of the prerift and synrift packages, the tectonic activity before rifting, the obliquity of rifting, and the tectonic activity after rifting. On the basis of these factors, we have defined a standard rift basin and four end-member variations. Most rift basins have attributes of the standard rift basin and/or one or more of the end-member variations. The standard rift basin is characterized by moderately to steeply dipping basement-involved normal faults that strike roughly perpendicular to the direction of maximum extension. Type 1 rift basins, with salt or thick shale in the prerift and/or synrift packages, are characterized by extensional forced folds above basement-involved normal faults and detached normal faults with associated fault-bend folds. In Type 2 rift basins, contractional activity before rifting produced low-angle thrust faults in the prerift strata and/or crystalline basement. The reactivation of these contractional structures during rifting created the low-angle normal faults characteristic of Type 2 rift basins. In Type 3 rift basins, preexisting zones of weakness in the prerift strata and/or crystalline basement strike obliquely to the direction of maximum extension, leading to oblique rifting. Type 3 rift basins are characterized by faults with strike-slip, normal, and oblique-slip displacement and with multiple trends. Contractional activity followed rifting in Type 4 rift basins. These inverted rift basins are affected by late-formed contractional structures including normal faults reactivated with reverse displacement, newly formed reverse faults, and contractional fault-bend and fault-propagation folds. Structures within rift basins affect depositional patterns by creating sites of uplift and erosion, by controlling pathways of sediment transport, and by defining the accommodation space for sediment deposition and preservation. The relationships among basin capacity (structurally controlled), sediment supply, and water supply determine the primary depositional regime in nonmarine rift basins, fluvial or lacustrine. Changes in basin capacity resulting from the growth of a rift basin may yield a tripartite stratigraphy (fluvial, deep lacustrine, and shallow lacustrine-fluvial) common to many nonmarine rift basins.