Structure and tectonic evolution of the transitional region between the central Appalachian foreland and interior cratonic basins

Root, Samuel; Onasch, Charles M.

doi:10.1016/s0040-1951(99)00022-0

Cited by 28 publications

(26 citation statements)

References 25 publications

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“…These arches essentially parallel the strike of the Appalachian Orogen and partly separated the Appalachian Basin from the contemporaneously subsiding intracratonic Illinois and Michigan sag basin ( Fig. 12) (Quinlan and Beaumont, 1984;Tankard, 1986;Beaumont et al, 1987;Root and Onasch, 1999;Howell and van der Pluijm, 1999).…”

Section: Appalachian Forelandmentioning

confidence: 97%

“…the Rome Trough. Moreover, the location of the Cincinnati Arch appears to be preconditioned by basement discontinuities, partly related to the Grenvillian front and partly to Precambrian rifted basins (Root and Onasch, 1999;Gao et al, 2000). This suggests that during the Taconic, Acadian and Alleghanian orogenies compressional stresses were transmitted from the Appalachian collision zone into the foreland.…”

Section: Appalachian Forelandmentioning

confidence: 99%

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Dynamic processes controlling foreland development – the role of mechanical (de)coupling of orogenic wedges and forelands

Ziegler¹,

Bertotti²,

Cloetingh³

2002

Stephan Mueller Spec. Publ. Ser.

104

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Abstract. Depending on the polarity of the subduction system controlling the evolution of an orogenic wedge, we distinguish between pro-wedge (fore-arc, foreland) and retrowedge (retro-arc, hinterland) forelands. Flexural foreland basins and/or intraplate compressional structures can develop in retro-wedge domains of Andean-type and in pro-and retro-wedge domains of Himalayan-type orogens.Whereas the subsidence of retro-wedge foreland basins is exclusively controlled by the topographic load exerted by the orogenic wedge on the foreland lithosphere, the additional load of the subducted lithospheric slab contributes towards the subsidence of pro-wedge foreland basins. Flexural forebulges develop only if the orogenic wedge and the foreland lithosphere are mechanically decoupled at lithospheric levels.Under conditions of mechanical coupling between an orogenic wedge and its foreland at crustal and/or mantlelithospheric levels, compressional stresses are transmitted into the latter, inducing reactivation of pre-existing crustal discontinuities and broad crustal and lithosphere scale folding at distances up to 1700 km from the collision front. Such stresses can accentuate potential pre-existing flexural forebulges or impede their development. Depending on the thickness and rheological structure of the crust and its sedimentary cover, thick-and/or thin-skinned thrusts can propagate far into forelands, either disrupting pre-existing flexural foreland basins or impeding their development.Collision-related compressional stresses can be transmitted into pro-wedge forelands during 1) initiation of subduction zones, 2) periods of subduction impediment caused by the arrival of more buoyant crust at a subduction zone, 3) initial collision of an orogenic wedge with a passive margin, and 4) post-collisional over-thickening and uplift of an orogenic wedge and the development of a mantle-back-stop.Development of intraplate compressional/transpressional structures in forelands is indicative for the build-up of collision-related compressional stresses, and thus for strong Correspondence to: P. A. Ziegler (fax +41-061-421.55.35) mechanical coupling of a foreland with the associated orogenic wedge, either at crustal and/or mantle-lithospheric levels. The absence of syn-orogenic intraplate compressional structures suggests that the respective orogenic wedge and its foreland(s) were mechanically decoupled. The level of mechanical coupling between an orogenic wedge and its foreland is temporally and spatially variable.Mechanical coupling and uncoupling of orogenic wedges and their forelands probably depends on the geometry and frictional shear strength of their common boundary zone. Subduction resistance of the foreland, as well as the buildup of high fluid pressures in subducted sediments, presumably play an important role. Pro-wedge continental crust and mantle-lithosphere can be subducted to depths of 100-150 km at which it can no longer support the weight of the attached oceanic slab and fails. Slab-detachment results in uplift of th...

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Section: Appalachian Forelandmentioning

confidence: 97%

Section: Appalachian Forelandmentioning

confidence: 99%

Dynamic processes controlling foreland development – the role of mechanical (de)coupling of orogenic wedges and forelands

Ziegler¹,

Bertotti²,

Cloetingh³

2002

Stephan Mueller Spec. Publ. Ser.

104

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“…The transitional region between the central Appalachian foreland basin, and the Michigan and Illinois interior cratonic basins, is characterized by first and second order structures related to plate convergent processes at the Laurentian plate margin (Root and Onasch, 1999). The Illinois Basin formed primarily during the Paleozoic Era, but its structural controls are related to older events.…”

Section: Structural Geologic Settingmentioning

confidence: 99%

“…Central and western Ohio is the transitional area between foreland and cratonic basins that is characterized by structures directly related to plate convergent processes (Root and Onasch, 1999). The Rome Trough is one of the major structural elements in the region and is part of the Eastern Interior (Iapetian) system of grabens (Root and Onasch, 1999) (Fig. 1).…”

Section: Structural Geologic Settingmentioning

confidence: 99%

“…Locations of Pennsylvanian age anticline axes in Illinois are from Schwalb (1982) and Nelson (1998). Compare sample locations to Table 1. with the highly faulted Rough Creek graben (Moorman syncline of Illinois), and extends over 800 km east-northeast across Kentucky and West Virginia, and northeast into northern Pennsylvania (Root and Onasch, 1999). The Reelfoot Rift, which extends from east-central Arkansas into southernmost Illinois and lies beneath the Gulf coastal plain strata of the Mississippi Embayment, and its extension, the Rough Creek graben, was related to the formation of the Illinois Basin (Kolata and Nelson, 1990) (Fig.…”

Section: Structural Geologic Settingmentioning

confidence: 99%

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Effects of late Paleozoic foreland deformation on underground coal mine ground instability, Illinois and Appalachian Basins

Phillipson

2005

International Journal of Coal Geology

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Tectonics of Sedimentary Basins, with Revised Nomenclature

Ingersoll

2011

Tectonics of Sedimentary Basins

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Actualistic plate-tectonic models are the best framework within which to understand the tectonics of sedimentary basins. Sedimentary basins develop in divergent, intraplate, convergent, transform, hybrid, and miscellaneous settings. Within each setting are several variants, dependent on type(s) of underlying crust, structural position, sediment supply, and inheritance. Subsidence of sedimentary basins results from (1) thinning of crust (2) thickening of mantle lithosphere (3) sedimentary and volcanic loading (4) tectonic loading (5) subcrustal loading (6) asthenospheric flow, and (7) crustal densification. Basins vary greatly in size, life span, and preservation potential, with short-lived basins formed in active tectonic settings, especially on oceanic crust, having low preservation potential, and long-lived basins formed in intraplate settings having the highest preservation potential.Continental rifts may evolve into nascent ocean basins, which commonly evolve into active ocean basins bordered by intraplate continental margins with three types of configurations: shelf-slope-rise, transform, and embankment. Continental rifts that do not evolve into oceans become fossil rifts, which later become sites for development of intracratonic basins and aulacogens. If all plate boundaries within and around an ocean basin become inactive, a dormant ocean basin develops, underlain by oceanic crust and surrounded by continental crust.Sites for sedimentary basins in convergent settings include trenches, trench slopes, forearcs, intra-arcs, backarcs, and retroarcs. Complex dynamic behavior of arc-trench systems results in diverse configurations for arc-related basins. Most notable is the overall stress regime of the arc-trench system, with resulting response along and behind the magmatic arc. Intra-arc rifting in highly extensional arcs commonly evolves into backarc spreading to form new oceanic crust. Backarcs of neutral arcs can contain any type of preexisting crust that was trapped there at the time of initiation of the related subduction zone. Highly compressional arcs develop retroarc foldthrust belts and related retroforeland basins, and may develop hinterland basins; in extreme cases, broken retroforelands may develop in former cratonal areas.As nonsubductable continental or arc crust is carried toward a subduction zone, collision generally initiates at one point and the resulting suture propagates away from this point of initial impact. Remnant ocean basins form on both sides of the initial impact point, and rapidly fill with sediment derived from the suture zone. As collision continues, the flux of sediment into the remnant ocean basin(s) increases concurrently with shrinkage of the basin until final suturing and obduction of the accreted sediment occur. Concurrently with collision, proforeland basins form on continental crust of the subducting plate and collisional retroforeland basins form on the overriding plate. Impactogens, broken forelands, and hinterland basins also may result.In transform settings and along c...

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Structure and tectonic evolution of the transitional region between the central Appalachian foreland and interior cratonic basins

Cited by 28 publications

References 25 publications

Dynamic processes controlling foreland development – the role of mechanical (de)coupling of orogenic wedges and forelands

Dynamic processes controlling foreland development – the role of mechanical (de)coupling of orogenic wedges and forelands

Effects of late Paleozoic foreland deformation on underground coal mine ground instability, Illinois and Appalachian Basins

Tectonics of Sedimentary Basins, with Revised Nomenclature

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Structure and tectonic evolution of the transitional region between the central Appalachian foreland and interior cratonic basins

Cited by 28 publications

References 25 publications

Dynamic processes controlling foreland development &#8211; the role of mechanical (de)coupling of orogenic wedges and forelands

Dynamic processes controlling foreland development &#8211; the role of mechanical (de)coupling of orogenic wedges and forelands

Effects of late Paleozoic foreland deformation on underground coal mine ground instability, Illinois and Appalachian Basins

Tectonics of Sedimentary Basins, with Revised Nomenclature

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Product

Resources

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Dynamic processes controlling foreland development – the role of mechanical (de)coupling of orogenic wedges and forelands

Dynamic processes controlling foreland development – the role of mechanical (de)coupling of orogenic wedges and forelands